PALEOBOTANY and PALEOZOOLOGY Cc D 9 LIBRARY OF RETURN TO SMITHSONIAN INSTITUTION R. D. LACOE. i ee » Z 0 Es C Z ie a) < 5 For the Promotion of Research in 7 J. W.RAEDER, Pa. lkes-Barre BINDER, (7 & 9 W. Market St... | i |W t oP an eg yibie: ” ® %, xe mF 3 @, «5: ® S x 2 a I EOLA. 5248 THE QUARTERLY JOURNAL GEOLOGICAL SOCIETY OF LONDON. EDITED BY THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY. Quod si cui mortalium cordi et cur sit non tantum inventis herere, atque iis uti, sed ad ulteriora penetrare ; atque non disputando adyersarium, sed opere naturam vincere; denique non belle et probabiliter opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant. —Novum Organum, Prefatio. VOLUME THE FORTY-FIRST,, TAN STS VIN LTT Os 1885. wee, D ZB43e7 | g £ eg 7 SS AATIONAL WE LONDON : ; LONGMANS, GREEN, AND CO. ’ PARIS: FRIED. KLINCKSIECK, 11 RUE DE LILLE; F. SAVY, 24 RUE HAUTEFEUILLE LEIPZIG: T.O. WEIGEL. SOLD ALSO AT THE APARTMENTS OF THE SOCIETY; MDCCCLXXXV. List OF THE OFFICERS OF THE GEOLOGICAL SOCIETY OF LONDON. PARADA EPA Elected February 20, 1885. Present, Prof. T. G. Bonney, D.Sc., LL.D., F.R.S. 1s «EERO Ses ciel een 30 Morean, Prof. C. Luoyp. On the S.W. Extension of the Clifton Palins os ce 6:2 See wey ceca ake: ca Pe aase on alae MEA TABLE OF CONTENTS. . Vv Page OweENn, Sir RicHarp. Note on the Resemblance of the Upper Molar _ Teeth of an Eocene Mammal (Neoplagiaulax, Lemoine) to those Oli RAEN AATG op 50) alpici oie SAGA dines he Hon digs senn ix Seley he ao 28 ——. Notes on Remains of Elephas primigenius from one of the Creswell ome emMe set cia seat (ate < aa Perse a as wie arcleverete a aie eye 31 Pennine, W. H., Esq. A Sketch of the Goldfields of the Trans- Voal,. OOUEMMeMmleamnr tate ah reels ya sveia Gage ctacniare'e wath a abel s oraves 569 Pipaeron, D., Esq. On some Recent Discoveries in the Submerged Worest, of) Torbay a ween en tate pais es chee enn, Sia e's) acoee «sis as ee READE, T. MELLARD, Esq. The Drift-deposits of Colwyn Bay.... 102 Evidence of the Action of Land-ice at Great Crosby, Baneashires cern ee ede cede he esas ate WEA eo) he 45 Ricketts, Dr.C. Onsome Erraties in the Boulder-clay of Cheshire, &c., and the Conditions of Climate they denote.............. 591 RoBeErts, T., Esq., and J. E. Marr, Esq. The Lower Paleozoic Rocks of the Neighbourhood of Haverfordwest. (Plate XV.).. 476 RuTLEY, Frank, Esq. On Fulgurite from Mont Blanc; with a Note on the Bouteillenstein or Pseudo-chrysolite of Moldauthein, ant bekiemiic.. o(ilate BEN sso ithe ac.g delete wichensjcreracatone. miso 3 152 =—————_ On breceiated, -orido-rosso Ameo .2....0.c.c sneer... 157 TEALL, J. J. H., Esq. The Metamorphosis of Dolerite into Horn- plemtesemist sc (CEAALOCID inti «Harve cies <- Bie ein nep ie eee TPR a - 9 baatrot Horeipn Members: .-).....2. 4, ses aoc eae meet a 18 lust ‘of, Moreien Correspondents. 200 ae eetacl ep cause ate 19 fast of Wollaston. Medallistse.s. (7. = coon. soe cies oe ee 20 Tastiotr Murchison Medalitstan 7: cc ae cere oan are eee 21 Lastiot Lyell Medallists <2. se .a.)-\cicle seu le cesie eee am ee Sime rmia ae duist- of, Bigsby Medallists”... oo. eae ete eee en ees Applications of the Barlow-Jameson Fund ..............05. Reet 23 Financial oe SEO Dane ae oO Se anne Enel esi 3 BEG oh 24. Award ofthe Medals-&e: 043606. .c 0002000 s be. ee eee 30 Anniversary Address Cae. ih s.. 3) 37 Donations to the Library (with Bibliography) .................. 113 Datton, W. H., Esq. On Specimens of Voluta Lamberti and 2 CUPPIRAIANGU AG. bs oo tel vistnin dias ciee so oe ee Davies, D.C., Esq. On the North-Wales and Shrewsbury Coalfields 107 GrestEy, W.S., Esq. On certain Fossiliferous Nodules and Frag- ments of Hematite (sometimes Magnetite), from the (so-called) Permian Breccias of Leicestershire and South Derbyshire .... 109 Page — a TABLE OF CONTENTS. _ oy Page Jounston-Lavis, Dr. H. J. On the Physical Conditions involved — _ in the Injection, Extrusion, and Cooling of Igneous Matter.... 103 Kinston, Ropert, Esq. On the Relationship of Ulodendron, Lindl. & Hutt., to Lepidodendron, Sterub., Bothrodendron, Lindl. & Hutt., Segillaria, Brongn., and Rhytidodendron, Boulay .... 98 LENDENFELD, Dr. R. von. On the Glacial Period in Australia .... 103 ReEAvDE, T. Metriarp, Esq. On Boulders wedged in the Falls of the Cynttehy Wiesgintope” Sor. arn ler. deoneler« ahct si ls's «is'sa eee % Tomes, R. F., Esq. On some imperfectly known Madreporaria from the Cretaceous Formation of England ................ II Ving, G. R., Esq. On the Polyzoa and Foraminifera of the Cam- Dadee Greencamd. oes vcanc cate teGmn ne Cece s Coe ere IOI ae ee ee SAC a A ee ee! Ck eo > Ee Wag mda ih Hah wet LIST OF THE FOSSILS FIGURED AND DESCRIBED IN THIS VOLUME. [In this list, those fossils the names of which are printed in Roman type have been previously described. ] Name of Species. Formation. Locality. Page. C@LENTERATA. ( Actinozoa.) Ale losteedy Sp. gnceesgnewondenecsensesss a (| 183 Barysmilia Etalloni. P1. v. fies. 179 Bathycoenia Slatteri ...............06 | 176 Comoseris irradians, Pl. v. f. 24 186 vermicularis, P]. v. f.25 ...... | 186 Dimorphastrea fungiformis. PI. v. BAe valde cndancceanasies ceils caste 185 Ennalloheitia socialis. Pl. v. f. 13, EE ere ete adeapiaiae cts asuadscsiace ieee 175 GaMlOGGKAy SPs cc cacucvecccceccsesleccacs 184 Hebstonin oolizien, .-PI.%. £1619 ee 181 Microsolena excelsa ..........00.s000 188 Montlivaltia, sp..........cecoeccscsceees | | 182 @hrasenis, Slattert 10550). cveds evanescence 187 Platastrea Conybeari................ “i 184 DEYMHOCUENIA, SPo ..<6-.2-secesecwenes 177 Stylosmilia excelsa. Pl. v. f. 9-12. 180 reptans. Pl. v. f. 18+21...... 179 Thamnocenia oolitica. Pl.v. f. 5-8 177 Waeycloseris limax............0s England ...... northamptonensis. Pl.i.f.4-7. |Lias .............-- PIAS eee ae eee eee at Great Oolite...... | | WSs Jac seceos teaeesda tac eee se ataas Great Oolite...... yj \ ANNULOSA. ( Crustacea.) Candona ansaia. PI. ix. f.9-12 ... | \ ( bononiensis. PI. ix. f. 7,8... Purbeck ......... H H Cypridea Dunkeri. PI. viii. f.9,10, |Wealden and tea loins sos ds a gaejyen see ARE Borbeck ‘50... —— granulosa. PI. viii. f. 18-21. ) a , var.fasciculata ......... —— —, var. paucigranulata. r England ...... 4 EDIE GT hed to | aS , var. gibbosa. PI. viii. f. 7. , var. posticalis. Pl. viii. RES Cee rn ee ) ) —— punctata. PI. viii. f. 1-8 } Purbeck .. ...... ——_——— | Page. 296 294 295 295 296 291 294 294 293 293 109 297 301 300 301 300 301 302 302 309 300 42 43 35 45 45 xii FOSSILS FIGURED AND DESCRIBED. Se a eee Name of Species. Formation. Locality. Page. SE EA EE an We LED VRE es ORNS eS ANNULOSA (continued). (Crustacea continued.) : Wealden and \ ( Cypridea tuberculata ..............200. | Purbedk fee 342 —_— , var. adjuncta. PI. Viii. | Ai Dd ieee Ct sate snack oe thcsas oe Purbéeke se ee || 342 WALAEHSIS vepees sce tea5cemceeorseei Wealden and —— ventrosa. PI. viii. f. 25,26... \ Purbeck™<..... | 336 — 9 WAN. GRUUOBE 1) ccs cectne Purbetle”. 2.3 | 340 Cyprione Bristovii. Pl. viii. f. 27— {Wealden and 340 7s Re ia aie et dS ae: Actidoaeere Purbeck ...... 344 Cypris purbeckensis. PI. ix. f. a) 347 Cythere retirugata. Pl. ix. f. 17- Be A Rape en een ens aint abate r England ......4 | 350 — —, var. rugulata. Pl. ix. eo eas RE VS ER | 350 —— ——,, var. fertilis. Pl. ix. ik £o 2A de Fete ones neerineey eae 350 transiens. Pl. ix. f. 13-16 ... } 349 Darwinula leguminella. Pl. viii. | Wealden and | fDO-SL see wce nano eecaieneie weneeies Purbeck’ .....- | 346 Metacypris Forbesii. PI. viii. f. 11- NG iii ic005- dacoesceeamenenearemssene= 345 —— ——,, var. verrucosa. PI. viii. Purbeck ...... .. | Pal Ze PAs spanseenes seeseey ) (| 345 VERTEBRATA. ( Pisces.) Onchus clintoni ...... EP Sy San Oe ari ( 61 pennsylvanicus ..... Acs haeeaeaee ee : 61 Pale@aspis americana .......6ce0.+-000- pe Selon AP series =. { 62 DELEUNCHLD 2 caaeneteeaecaeeeee Wh: ee62 (Reptilia.) Iguanodon. PI. xiv. ..........00-se00e {Wealden Pees va) Elastinies ca.2e | 473 (Mammaiia.) Elephas primigenius ......... ........ Pleistocene ...... Pritam. «cs... 31 Halitherium Schinzi ....... Be jana Miocene ......... Germany ...... 465 Microcheerus erinaceus ............. és BOGRBELe A. eae Britain, ..... eae 529 Neoplagiaulax eoccenus ............4 Hocene....... 5a 6 MECC oa siacd ois a 28 QyiOsitiosChatus <2 ...520..3s.c026.- Pleistocene ...... Ligi7) ee | 242 Prorastomus sirenoides ............... Tertiaty. >see Jamaica ...... 465 Rhytina gigas ..... ght ore bissvecssese |Pleistocétie :.i77-|0 sbenting’s Isl. 459 EXPLANATION OF THE PLATES. PLATE Pace I Triconix, to illustrate Mr. E. A. Walford’s paper on the Trigoniz of the Jurassic Beds of North Oxfordshire ...... 35 II Do.LeERITE AND HorNBLENDE Scuists, to illustrate Mr. Teall’s paper On those rOcks............s.ceececseeseeccscenccecscscessecees 133 rr { Fuucurite on HoRNBLENDE-GNEISS, to illustrate Mr. F.Rutley’s “| paper on Fulgurite from Mont Blane ............cscceeseeees 152 IV. Hoxtow Senervuirss, to illustrate Mr. Cole’s paper ......... 162 ~ Great OoritE MADREPORARIA, to illustrate Mr. R. F. Tomes’s , Paper on: Hose. TOSS: iss. ccc cukssasds cows dadkquneusece=+ccteenee 170 Map anv Section of the Rio-Tinto Mining District, to illus- VE { trate Mr. Collins’s paper on its geology ..........s.eeeeeeeee 245 VII SoutH-AvstrALIAN CHILosToMATous Bryozoa, to illustrate “| Mr. A. W. Waters’s paper on those fossils .................. 279 VIII. { Purseck Ostracopa, to illustrate Prof. T. Rupert Jones’s IX. Pit PieE Of bHG RS LU SSE eee cco ant aa oncecs . Yy (i, Y iy » Ss ~ een . SSNy WR SS sheet of no great thickness from Redcliffe Towers to Preston Lane, while its seaward edge, instead of extending beyond low-water mark, as in the neighbouring inlets of Goodrington, Torre Abbey, Paignton, and Broad Sands, has been truncated by the action of the sea and is now confined to the limits shown upon the plan. Inland the clay bed forms a flat basin, whose northern lip, rising with the flank of the valley, thins out to nothing at B, about seven feet above high-water mark, while its southern lip has been denuded, together with the Trias rock upon which it rests, to the level of the sea. Of the inland lip of this basin more hereafter. The clay reposes directly upon the Trias at A (figs. 1 & 2), while, further north, it lies upon a somewhat remarkable breccia or “ head ” (L, fig. 2), which caps the Trias conformably from about the point C for a considerable distance northwards of Preston Lane. This breccia, which, together with the forest-clay underlying Preston Sands, has been minutely described by Mr. Pengelly*, consists of unstratified, angular, and loosely aggregated stones, packed, without order or arrangement, in a clayey matrix. The stones have nearly all been derived from a neighbouring hill of Devonian sandstone, whence * Trans. Dev. Assoc. for 1878. IN THE SUBMERGED FOREST OF TORBAY. 13 they have travelled to their present position along slopes which are, for the most part, so slight that it is difficult to suppose existing natural agencies to have been concerned in their transportation. This breccia is, in all probability, an example of those deposits which, going by the name of “head” in the west of England, attain a great development in the maritime districts of Southern England and Northern France, and which Sir A. Ramsay and Prof. James Geikie have considered to be the equivalents of true glacial deposits, such as the till, but formed in districts which were not covered by the continental ice-sheets. That the clay bed, which thus rests either upon the Trias rock or the breccia which caps it, forms the soil in which a portion of the submerged forest of Torbay is rooted, there is no sort of doubt. It is crowded with roots of all sizes; while here and there, the trunks of trees, whose roots branch through the clay in all direc- tions, still stand erect and show themselves above the surface of the shingle whenever this is thinly strewn over the tidal strand. It is further covered, as shown on the map, with a mass of so-called . peat, D (fig. 2), which is nearly three feet thick in some places. Towards the end of December 1883, the sea exposed the area of clay and underlying ‘“‘ head” shown at E, fig. 2. E itself represents the trunk of a large tree about whose roots, which were partially denuded, the clay was several feet thick, and whence it thinned away to a feather-edge where it met the “head.” Here, resting immediately upon the breccia at G, two pavement-like aggregations of stones were observed, each about two feet across, and of irregular out- line, but both presenting the appearance of having once been united. These quasi floor-fragments consisted of well-rolled beach stones, the counterparts of certain trap pebbles, derived from the Trias, and very numerous on the present beach, but differing totally in character from the angular Devonian stones in the “head” on which they lay. That these were no heaps of pebbles shot down from a cart for some purpose, during a previous exposure of the breccia, as might well have seemed the case, was clear from the fact of. their being everywhere interpenetrated by fibrils of the forest roots. A close examination revealed the curious fact that these trap pebbles were all cracked and traversed in every direction by minute fissures, so that the stones, usually difficult to break, even with a heavy hammer, could be pulled apart by hand. The fractures were of such a kind as forcibly to suggest that the stones had been heated ; and some trap pebbles from the beach, upon being placed in the fire, soon exhibited similar fissures, and became cracked in exactly the same way as those forming the heaps in question. The interstices of the hearth, as the structure now began to be con- sidered, were crowded with fragments of charcoal, easily distinguish- able from the dark-coloured and decomposed. vegetable matter furnished by the adherent rootlets. But if the seeming floor were really a hearth, the question at once arose—Why should its builders have gone afield for materials when there was plenty of Devonian sandstones ready to hand in the 14 D. PIDGEON ON RECENT DISCOVERIES “head”? Why did they not light their fires upon it? On trial, however, it was found that such fragments of Devonian rock as the breccia contains fly to pieces with great violence on being heated, and were therefore quite unfit for the construction of fire- places. Finally, the floor-like structure, the heat-cracked stones, the presence of apparently true charcoal, and the proved unfitness of the breccia for hearth-building, suggested the conclusion that man had roamed in Torbay at some period subsequent to the depo- sition of the breccia capping the Trias, and prior to the deposition of the clay in which the submerged forest is rooted. The discovery of a presumptive hearth raised hopes that some utensils of human origin might ultimately be found ; nor was this anticipation disappointed. ‘Towards the end of February 1884, a heavy gale bared the strand very widely, the junction of the forest- clay with the underlying Trias being well displayed at the point marked A in figs. 1 and 2. A large area was here uncovered, and the clay soon yielded several trap pebbles, cracked as if by fire, and fissured in exactly the same way as others which formed a part of the presumed hearth. This suggestive find was carefully followed up and the forest-clay thoroughly searched from A to B, after every tide, so long as the exposure lasted. The following articles were discovered, and are all exhibited on the table :— 1. An ingot of copper, found lying on the surface of the forest- clay. Although not actually imbedded, its position and appearance left no room to doubt that 16 had been disinterred by the last tide. 2. A portion of a similar ingot, also found lying on the surface of the clay, but having a few minute rootlets clinging to one of its crevices. 3. Numerous pieces of rude pottery, made of dark-coloured, un- burned clay, mixed with small fragments of stone. 4, Three fragments of granite grinding-stones, originally of circular outline, and about ten inches in diameter. 5. A curiously shaped piece of whetstone. 6. A piece of glass. 7. A large number of angular stones consisting, according to assays made by Messrs. Henry Bath and Sons, the eminent tin- and — copper-brokers of Swansea, of tin slags containing a small quantity of that metal. 8. A quantity of triturated tin-slag, without metallic contents. 9. A number of angular flints, ame which are many having a decidedly artificial character. 10. Three or four flint implements, in some cases worn by use. All these objects, with the exception of the copper, were actually disinterred from the clay, and were found either interpenetrated or embraced, according as they had or had not fissures, by fine root- lets, such as everywhere crowd the clay itself. Everything, except the whetstone and one flint implement, which occurred near Preston Lane, was found closely associated within the space of a few square yards, and at the spot marked H on the plan (fig. 2), or just where the forest-clay makes a junction with the Trias. IN THE SUBMERGED FOREST OF TORBAY. 15 It is worthy of remark that the spot in question forms the natural point of discharge for water accumulating in the valley A B, and that water-rolled gravel occurs in the clay, quite close to the spot where the modern pipes F, which drain the low marshy land of the valley, have been laid down. A word must now be said with regard to the position of these various articles vertically in the clay. This, together with the Trias ridge upon which it rests, has been ereatly ‘denuded within the limits of the tidal strand. A number of truncated posts were observed at J, and several of these were drawn. They consisted of tree-stems, four or five inches in diameter, and roughly pointed ; but, in no case did more than five or six inches of their original length remain, proving that some feet of clay had been denuded since the posts were driven. The wood of these piles had its larger vessels threaded with the rootlets of other plants in exactly the same way as the forest-wood itself, which, whether prostrate or erect, is always ‘ interpenetrated by the roots of subsequent vegetation. The present tidal strand has therefore been a land surface since the posts were driven. The Trias ridge upon which the forest-clay rests has been pared down pari passu with the latter, above which it projects only a few inches. The clay thickens rapidly from its junction with the Trias outwards, and is from three to four feet thick under the drain- pipes F. Assuming that the piles were originally driven not less than two feet into the clay, and bearing in mind that the objects on the table were found nearer the junction than the drain-pipes, it is probable that they occupied a position about midway between the original surface and the bottom of the clay bed at this point. Reviewing the above facts, the conclusion seems inevitable that tin was smelted and bronze probably made on the spot in question at some time prior to the deposition of the forest-clays, and that the land surface supporting this early metallurgical establishment was the Trias rock. That the objects obtained from the clay were en- tombed during its deposition, is shown by the fact of their inter- penetration by the rootlets for which that clay subsequently formed a soil; and, unless work was carried on within a pile-dwelling, the bronze-makers must have been antecedent in time to the forest- clay. If the platform of cracked stones found seated upon the “head” be accepted as the remains of a neighbouring smelting- hearth, then there is no question but that the suggested sequence of events is correct. Not only, then, was man living in Torbay at some period prior to the deposition of the forest-clays, but he was already acquainted with the art of smelting and a worker in copper and tin—facts which allow no escape from the conclusion that the soils in which the submerged forests of Torbay flourished were deposited since the beginning of the bronze age in Britain. This, according to Dr. Evans, did not probably extend more than twelve or fourteen centuries backwards from the commencement of the Christian era, a period agreeing fairly well with M. Morlot’s well-known estimates, which give 3800 years as the present age of 16 D. PIDGEON ON RECENT DISCOVERIES the bronze period in Europe. Sir John Lubbock has, indeed, ad- vanced reasons {for believing that the Phoenicians traded with Britain for tin fully 1500 years before our era; and, if this be so, we must suppose that the inhabitants of Belertum had been acquainted with the art of. smelting for very many years before that date, there being nothing to suggest that the Britons were taught metallurgy by the Pheenicians. That the present coast-levels of England have persisted for at least two thousand years past seems to be fairly” established; and, this being so, it follows that the subsidence, if subsidence it were, that placed the primitive smelting-works lying under Redcliffe Towers beneath the tidal waters of Torbay, must have occurred at some period prior to the Roman occupation, or during the 12, 15, or more centuries which, according to Dr. Evans, M. Morlot, or Sir John Lubbock, elapsed between the beginning of the bronze age in Britain and the coming of Julius Cesar to our shores. This question may be left for a moment in order to inquire how _ far a comparison of the objects found in the clay with other early works of human art supports the conclusion that the soils of the Torbay forest are of comparatively recent date. It will be observed that the fragments of pottery are similar in character to both British and Swiss lake-dwelling pottery, of which the former may be of any age from 1500 to 3000 years. The copper ingots have their exact counterparts in others now in the Natural-History Museum which were found in the black mould, or uppermost layer of Kent’s Cavern ; while whetstones and querns, similar to those taken from the clay, are not uncommon in Romano-British finds. Granting that the flint implement found by Mr. Watson, lying on Torre-Abbey sands, is a true forest-fossil, this in no way militates against the conclusion which is sought to be established. Not only have such tools been found associated with bronze implements in the Swiss lake-dwellings and elsewhere, but there is evidence of such association on the table this evening. The horn implement found by Mr. Ardley in the peat of the Torbay forest supports the ideas which have been advanced ; for no one examining this tool with a critical eye can avoid coming to the conclusion that it has been shaped with something very much more effective for cutting-purposes than a stone hatchet. : It is well known that the Torbay forest is of later date than the cave-earth of the neighbouring Kent’s Cavern, and later than some portions, at least, of its stalagmitic covering; for both these deposits contain the bones of certain extinct mammals whose remains are not found in the forest. The fauna of the latter is, indeed, the fauna of to-day, consisting for the most part of the red deer, the ox, hog, sheep, and goat, creatures whose bones are also found in the black mould of Kent’s Cavern. There is some evidence, it is true, that the mammoth roamed in Torbay during the forest-era ; but it is not conclusive, and it will be time to believe that Elephas primigenius was a contemporary of bronze-making man in Devon- shire when its remains have been found in actual association with the works of the latter. This subject will be again referred to in the. sequel; it is needful now to pass on to the description of IN THE SUBMERGED FOREST OF TORBAY. another find recently made by the writer’s son on the tidal strand of Goodrington Bay (fig. 1). This inlet has much the same general character as that which has already been described, and consists of wide and gently sloping sands, crowned with a prominent ridge of beach, behind which the ground is low, flat, and marshy, having been reclaimed from swampy conditions only in recent years. Fig. 3 exhibits a section of the tidal strand taken through the spot where the “find” in question was made, and it will be observed that the forest-clay is here no- where visible. -At the bottom is a bed, E, consisting entirely of pro- strate trees and vegetable débris ; above that is another, A, com- posed of the stems of the water- bistort (Polygonum amphibium) standing as they grew; next, a stratum of silt and vegetable mat- ter, D; then a thin layer of red clay, F, and lastly a bed of much- abraded reedy débris, C, upon which the beach, B, appears to rest. The thickness of the lowest bed is unknown, while that of the others is altogether about eight feet. Borings made by the Great Western Railway Company have shown that there are at least seventy, and it may be many more, feet of vegetable débris in the marsh immediately behind the beach, where it is crossed by the line carried on a high embank- ment, On November 18th, 1883, the writer’s son disinterred from the Polygonum-bed, A, fig. 3, two large pewter vases, one of which is now on the table, while the other has been presented to the Museum of the Torquay Natural History Society. These vessels Q.d2G..5. No. Ler. ze) “1ajYVUI o[qvjos0A pure pug *q ‘royyeun Apaod JO stiqocy “pues “p rel “£vIO, poy P [[e ut 07¥1480ad Pal SuySIsuoo ‘poq-yseto,7 “OT Youd “g ‘qystadn sue}g ‘poq-uinuossjog “y "SUO1}O0.AT & SUIAT 80044 JO = ° Zz a in a 9° 2 im 0% 09 OS Ob OF Of oF Oo SQAgo oe og #2 itioo BIWOS WWOLYAA Mo Oi mn I ina JNM UaLVM HDIN 17 ‘sasp4 fo worrsod pun ‘unau ur Ysinyy paunipun buamoys ‘yonog uopburupooy fo wonooy ajnunxouddy—e “OUT 18 D. PIDGEON ON RECENT DISCOVERIES lay in contact, one above the other, were unmistakably imbedded, were full of fine vegetable débris, totally free from any admixture of marine deposits, and were crushed flat by long-continued gentle pressure. he metal of which they are composed has been found to con- sist of 10 parts of tin to 1 part of lead, and they have been pronounced by Mr. Franks of the British Museum to be almost certainly Roman. The bed in which they were found is about 10 feet. below high- tide line, and vertically lower than the point at which the relics of bronze-making man were discovered in the clay bed of the adjoining inlet. This fact alone suggests the necessity of caution in coming to conclusions on the general question of subsidence. _ Old maps of Torbay, such as those of Speed, dated 1610, Saxton, 1675, and Donne, 1765, demonstrate immense encroachments of the sea in this neighbourhood during comparatively recent times. The ordnance survey of 1809 shows that a road then traversed Goodrington Sands where the tide now flows; while the earlier surveyors whose names have been mentioned demonstrate a very considerable seaward prolongation of the land in Torbay within the last three centuries. There is little room to doubt that the Roman vases in question were lost in Goodrington Marsh at a time when the beach which dammed its waters was far seaward of its present position and of the spot where the vessels were found. Since that time, the beach, receding before the advancing sea, has passed over the vases, which the waves have, finally, disinterred from the foreshore. The vertical position of the vessels, 16 feet below high-water mark, may be explained by supposing that the fallen trees and vege- table detritus, filling the Goodrington valley to a depth of at least 70 feet, formed a very compressible mass, and as this became gra- dually consolidated, the reedy beds growing above the prostrate forest gradually settled and carried any enclosed objects down with them. The same bed of clay which underlies the forest on Preston Sands, is also present at the same levels at Goodrington, where, how- ever, it is generally covered with sand and shingle. In the centre of the bay there oceurs a reef of Devonian shale, C, fig. 1, which is covered at high, and exposed at low water. Upon either side of this reef the clay reposes, just as it does upon the Trias reef immediately below Redcliffe Towers in the neighbouring bay. Thence it dips rapidly on either hand, and is soon covered with a thick layer of peaty matter, as is also the case on Preston Sands. There is, however, nothing to show whether this bed of clay passes continuously from the reef under the great depth of forest- deposits which the Great-Western borings have shown to exist at the lowest part of the Goodrington valley. With regard to the character of the forest-clays Mr. Godwin- Austen*, writing in 1842, says that the submerged forest of Torbay rests on lacustrine mud, which at Broad Sands contains shells of Paludina impura in great abundance; while at Goodrington also * Trans. Geol. Soc. ser. 2, vol. vi. IN THE SUBMERGED FOREST OF TORBAY. 1y there are traces of lacustrine marl. The writer, on the other hand, while totally failing to find any freshwater shells in either of the inlets, has met with Scrobicularia, Hydrobia, Lnttorina, and Melampus, the three former abundantly, in a single but very limited exposure of the clay only a few hundred yards south of Redcliffe Towers. Of these shells, the Hydrobiw formed a bed several inches in thickness, and would have given the idea of their having lived and died during the accumulation of the clay, but for the fact that they occur at precisely the same horizon as living shells of the same species would do. It is quite impossible to suppose that an estuarine bed of clay which has been elevated io form the soil of a forest should, upon subsequent subsidence, sink to exactly the same horizon as it occupied before its elevation ; and it is probable, therefore, that the marine shells in question flourished where they were found during some recent but prolonged exposure of the clay, while the shifting of derived mud during that time might give them the appearance of being bedded. The clay itself, when not charged with vegetable matter (which gives it a blue tinge), or stained at its margins by the red rocks upon which it lies, is almost white and of an extremely fine, butter-like consistency. To this excessive fineness must probably be attributed the fact that the clay is white, while the surrounding drainage-area is composed chiefly of red rocks. Not the slighest evidence of marine action is exhibited by the lip which, as already stated, can be traced around portions of the shallow basin in which the clay accumulated; and, in view of this fact, of Mr. Godwin-Austen’s positive observation, and of the possibility of explaining away the rare presence of marine shells in the deposit, it is probable that the clay is of lacustrine origin. It is time to consider the question of the supposed subsidence of the area under consideration in the light of the following facts :— 1st. That the forest-clay of Preston Sands contains relies of bronze- making man. 2nd. That the upper, peaty beds of the submerged forest of Good- rington have yielded Roman remains. It has been suggested that the shores of Britain have probably remained at their present levels for at least 2000 years past; and if Dr. Evans’, M. Morlot’s, and Sir John Lubbock’s views may be relied upon, the bronze age in Britain is not older than 4000 years. But if, as Mr. Pengelly suggests, Torbay stood at least forty feet higher than now during the forest-era, it becomes necessary to believe that, at some time within the twenty centuries preceding Roman times in Britain, the Trias rocks of Preston Sands have been :— 1. Submerged for the deposition of the forest-clay. 2. Elevated to a height of at least 40 feet. 3. Depressed to their present level. That a coast which has remained stationary for the last 2000 years should have made such active use of the preceding twelve or twenty centuries for the purposes of oscillation, is rather hard of belief. Hither the bronze age must be of unsuspected antiquity, or the c2 20 (Scale 60 feet to 1 inch.) Fig, 4.—Section of the Exposure at Redcliffe Towers, April 22, 1884. D. PIDGEON ON RECENT DISCOVERIES | Sand,-------7--+ il =| a iu = <| “| =] oi) =| Tree stumps.------- Al BG ‘i Shingle._------ Blown sand._-_-_-- Blown sand..-----_\ Kass OoENe Sosua de Neen ew eT Gus Se SS ES SS SS on = SEE ee SSSSS SSSsss vee Seats Sw SS SS Ss SS SS SSS SSSA SESS FOREST CLAY FOREST CLAY objects to which attention has been directed this evening must have been lodged where they were found while the land stood at ex- isting levels. In attempting to answer this question attention will be strictly confined to the Paignton-Preston inlet, a section of which is shown in fig. 4. The clay-bed is here only just below high-water mark at that part of the marshy land most remote from the sea. It passes seaward with a very slight inclination to at least 750 feet from the shore, that being the length of the Paignton Pier, whose piles were all screwed into the clay. It is covered, inland, first with coarse sand, among which are found many large cockle-shells and occasional patches of shingle ; while, over all, is a layer of blown sand, the surface of which is some two feet above high-water mark. Its seaward margin, being un- protected by a beach, is in course of truncation and destruction by the waves; but behind the beach such plants as the water-bistort (Polygonum) are growing luxuri- antly, while willows are exten- sively cultivated in the swampy soil. It is noteworthy that most of the trees found prostrate in the forest-clay are also willows. The basin in which the clay lies has alip which is distinctly visible in the cliff near Preston Lane, and whose position on the slopes of the neighbouring hills is well known to the village builders. This stands about seven feet above high-water mark, and its margin (as already mentioned) gives no evidence of having ever been fring- ed by a marine beach, while the extreme fineness of the clay itself attests its deposition in still and scarcely turbid waters. IN THE SUBMERGED FOREST OF TORBAY. oF The evidence in favour of extensive encroachment of the sea in Torbay is conclusive. Large tracts of land, houses, and roads have disappeared within the memory of man; while maps less than 300 years old show, with more or less accuracy, a shore-line hundreds of feet in advance of the present one. It seems probable therefore that the Paignton-Preston inlet was once barred by a beach, distant at least 750, and probably very many more, feet from the present beach, behind which the land-water accumulated to a height of about seven feet above the high-tide level, and that in the lake, or mere, thus formed the forest-clay was laid down. By the breaking down of the dam, the sea was admitted, covering what is now Paignton Marsh with coarse sand, to be followed by blown-sand deposits, and in this way the sea was again expelled to the limits of the present coast-line. Meanwhile the willows and marsh-plants whose débris aud roots form the greater part of the so-called peat-beds overlying the clay took possession of the low-lying ground. Man, as we have seen, was present in the Paignton-Preston inlet either before the lake in question was formed, living on the “ head,” or inhabiting a pile-dwelling during the deposition of the clay, or even, if the lacustrine conditions were intermittent, settled on the clay itself; but, i any case, the suggested explanation makes it unnecessary to suppose that the bronze-makers of Redcliffe Towers were witnesses of those wide oscillations of level which have here- tofore been associated with the physical history of the submerged Torbay forests. The topmost beds of these deposits have been shown to be no older than the Roman occupation of Britain, while their base dates from the bronze age. If the molar of Hlephas primi- genius which has already been referred to was really derived from a seaward extension of the forest lying exposed between tide-marks in Torbay, then it must be concluded that the mammoth survived in Devonshire almost down to Roman times, and that he was certainly contemporary there with bronze-making man. But it is not necessary to suppose that the same bed of clay and the same forest were continuous for great distances seaward in Torbay. Buried forests are, elsewhere, almost always found in tiers, sometimes, as in the Fenland districts, four or more one above another. At Blackpool, only a few miles from Torbay, Mr. A. R. Hunt* has given reasons for believing that one submerged forest rests upon another; and these forests might, of course, differ vastly in age. Similarly there may be forest-beds beneath the waters of Torbay older than those which are visible on Torre-Abbey, Paignton, Preston, and Goodrington Sands, and the mammoth’s tooth may have come from one of these. In any case, the submerged Forest of Tor- bay, and possibly therefore other submerged forests fringing the English coast, are even more truly things of yesterday than has hitherto been supposed. _ * Trans. Dev. Assoc. A. R. Hunt, July 1881. 22 oN RECENT DISCOVERIES IN THE SUBMERGED FOREST OF TORBAY. Discussion. Dr. H. Woopwarp said that it was interesting to find that the copper ingots exhibited by the author closely resembled ingots of the same metal obtained by Mr. Pengelly from Kent’s Cavern. The pottery from the two localities was also similar. . Prof. T. Rupert Jones doubted the paleolithic age of the flint- flakes. Similar flakes have been found on the surface in many parts of southern England, and are by no means of paleolithic age. Prof. T. M‘K. Hveuus said that one of the most interesting points connected with the paper was the explanation of a “submerged forest ” without the necessity for any submergence. He quite agreed with the author that the damming back of the sea and the growth of trees below high-water mark behind the dam, furnished a probable explanation of the phenomena. The occurrence of the two clays described might indicate two different periods, and sub- mergence might have occurred between them. The evidence of the chips was not of much value, as they might be of any age. The pottery appeared to be British. Mr. Branrorp agreed with the author in his main views, but wished to point out one difficulty. The supposed tin-smelting hearths were some 10 feet below high-water mark, and the ground must have been too wet for smelting, if not actually below water. Mr. Torrzy expressed his general agreement with the author; but remarked that similar opinions, as to the recession of shingle- beaches and the formation of “submerged forests” without sub- sidence, had been put forward by Mr. Yates, Col. Greenwood, and others. Where the forest-growth, however, extended to or below low-water mark, he thought subsidence must have occurred. The AvurHor thanked Dr. Woodward for his remarks, and for the access he had given him to similar ingots in the Natural History Museum. He had used the term “ paleolithic” merely to indicate the type of the flint fragments. He stated that his paper answered Mr. Pengelly, who thought that there had been a submergence of 40 feet. With regard to the hearth he admitted the difficulty pointed out by Mr. Blanford, for there was no doubt that this was resting on head. ON THE CRETACEOUS BEDS AT BLACK VEN, NEAR LYME REGIS. 23 3. The Creraceous Beps at Buack Van, near Lyme Ruets, with some SUPPLEMENTARY Remarks on the Buackpown Bens. By Rev. W. Downss, F.G.8. (Read November 5, 1884.) Four visits, each of three or four hours’ duration, to the same section and upon almost consecutive days ought to afford the opportunity for recording somewhat, unless the section be either one that is void of interest, or already so worked-out as to leave nothing further to be recorded. In the present case, when among the previous workers are found the names of Etheridge, Meyer, De Rance, Price, and others, it may seem probable that the subject might have been exhausted. As, however, the writer’s experiences do not quite agree with all that has before been written, and as he found not a few fossils in a bed hitherto (as he believes) supposed to be non-fossiliferous, a brief memoir may be of service. The section in question is about halfway between Lyme Regis and Charmouth, in the sea-cliff. Four years ago there had been a landslip there, which necessitated a reconstruction of the high road. According to a local informant this landslip revealed for the first time the presence of a bed of Gault; but this statement was certainly erroneous, for fossils from the Gault bed seem to have been in the Jermyn-Street cases long ere that date. But the landslip seems to have done some service to geology in making the Gault bed in one place more accessible, and in causing a new and clean-cut section of the beds above it to be made in the course of the recon- struction of the road. The whole cliff-section may be roughly computed to be 300 ft., ot which the lower 200 ft. is Lias, and the upper 100 ft. is Cretaceous. The iatter may be subdivided again, as 25 ft. of black loamy clay at. the base, and above it 75 ft. of yellow non-calcareous sand, with a capping of chert gravel. Further westward the Greensand is calcareous, but not at this spot. The Gault is of very much the same colour as the Lias beneath; but as the former is pervious, and the latter impervious, it appeared to be more easy to trace the boundary with the eye than to traverse it with the feet; for in the few places where a ledge is accessible there is a quagmire of black ~ slush, the result of the outbreak of springs. Mr. De Rance, as quoted by Mr. Price (‘ The Gault’ &c. p. 27), tells us that, “‘at Black Ven, where it (¢. ¢. the Gault) is best seen, it is divided from the Cowstones above by a few feet of yellow sand. A comparison of the fossils from this place with those at Folkestone tends to correlate the Dorsetshire Gault with the Lower Gault of Folkestone, rather than with the Upper Gault; in which case, sup- posing the Whetstones in the Blackdown beds to represent the Cow- stones, they and other portions of the former may be equivalents, in time, of the Upper Gault.” 24 REV. W. DOWNES ON THE CRETACEOUS BEDS It is with reference to the above questions that the following observations are especially made. The fossils found in the Gault by the writer were 33 in number, and in the following proportions :— dima gparallelay Wo. esa Weis 10 Inoceramus concentricus ........ 6 HECTARES end meio ene teats 1 Miodiola? ssp: iiss esi... oe ee 1 Pinna tebrarona, |i). 2) aie 3 GTS BPs 222 6 Ce Oe ee 2 Cacullees cearinata.?:o.:o Eee 3 Panoprea?.; Yast +. eee eee furritella granulata ?\ 42.222. 4 Hemiaster ?, sp. (crushed specimens) 2 33 The chief point to be observed with regard to this list is the great preponderance of Lima parallela, a form unknown in the Blackdown beds. Inoceramus concentricus, which comes next in point of numbers, is useless for marking an horizon, as it occurs everywhere in Cretaceous beds. Negatively the absence of Belemnites and of Inoceramus sulcatus is noticeable in comparing this bed with that at Folkestone. Of Ammonites, I believe that A. splendens is the only form hitherto found. This black bed passes upwards into yellow sand of the ordinary Greensand type. No fossils from the latter have, so far as I am aware, been yet recorded. I searched long without finding any. After a while, however, a careful examination of the roadside section revealed the fact that organic remains had been abundant there, though the traces of them had in the large majority of cases been obliterated. In some cases a spiral univalve, ¢.g., would be trace- able only by a spiral line of discoloration, which fell to pieces on being touched with the penknife. Elsewhere, by very carefully removing the sand, many casts of bivalves were found. The sand was, however, not cemented in any way. It was simply balled together lke a snowball, and fell to pieces with any but the most tender handling. Ofcourse very few of such casts could be identified. Indeed, the only form of which I felt really sure was Cyprina cuneata, which seemed to be abundant. The search was, however, fascinating, and it led me at Jast to the discovery of a nest of fragmentary fossils silicified, and altogether resembling very poor Blackdown specimens. The nest was a roughly spherical patch in the sand, about 1 ft. in diameter, the matrix being rather darker and more ferruginous than the rest. Its origin appeared to be a chemical superinduced change around a nucleus of some kind. In this little spot I found evidence, mostly fragmentary, of the following forms :— AT BLACK VEN, NEAR LYME REGIS. 25 Cyprina cuneata (abundant). Cardium proboscideum (3 small Gervillia rostrata (abundant). fragments). CYther@d COPCTALG, «200...00%a-0-0-- +0 4 | Pecten orbicularts ?.......+-s+005++- 1 TPAG ONL SCAOTICUNE eae neeeecc-as=- +5 2| P. quinquecostatus...... (fragment) 1 Cuculled Glabra........+.0.+00sc0eceses 4 | Turritella granulata ............06 1 OL PDT OSEig) Saks ene ee tere eae a Do Phastanella 2? Spe esac cssdenascaes 1 EELOMYTG «see%en. | See age ees ates 1 | Serpula. Siphonia ? The spot in which these occurred was about 50 ft. above the spot in the Gault where I obtained the other fossils, and in nearly a straight vertical line above it. All my subsequent endeavours to find another such nest of fossil remains proved futile; but its occurrence is a remarkable comment upon the fragmentary character of geological evidence. But for this little local alteration of the matrix, affording conditions for preservation, and proving that it had once been teeming with life, the rock might have been pronounced altogether barren of organic remains. In this spot, then, 50 ft. apart vertically, are two very distinct hori- zons. There is but one (possibly not even one)specific form in common. That one would be Zurritella granulata; but the specimen from the Gault-bed is too poor a one for exact determination. The fauna of the upper bedis a much nearer approach to the Blackdown fauna than that of the lower, and for this reason as well as from its position, is probably its equivalent; but the absence of some of the commonest Blackdown forms is noticeable. Among the commonest Blackdown forms is Pectunculus umbonatus, and the closely allied form P. sublevis ; these, however, at Blackdown are distinctive of rather high horizons. One might therefore be justified in reasoning from this fact that the upper Black-Ven bed might be the equivalent of the lower Black- down. But per cont‘a in the Black-Ven bed we have a great preponderance of Cyprina cuneata, which at Blackdown is distinctive of a bed intermediate between the two Pectunculus-beds. The evidence, so far as it goes, seems to show alternation of specific horizons. It would seem as if inosculations due to changing littoral conditions occurred among the beds, as before suggested by Prof. Seeley *, with certainly a general thinning-out to the westward. Under such circumstances it is questionable if we shall ever be able to subdivide the Cretaceous beds of the West of England into the marked divisions of Gault and Upper Greensand which are applic- able to the beds to the eastward. The black Lima-parallela bed of Black Ven is, however, clearly of lower horizon than the lowest of the Blackdown beds ; for it thins out before reaching Sidmouth, and apparently immediately underlies the Blackdown series. The general thinning-out to the westward is very evident. Mr. Hudle- ston has pointed out that the Lower Greensand has thinned out eastward of the vale of Wardour, though, according to Mr. Etheridge, there are some traces of it to be found in the more southerly beds at Black Vent. The Gault, as shown in the coast-section, evidently * Quart. Journ. Geol. Soe. vol. xxxviii. (1882), p. 92. T Ibid. p. 93. 26 REV. W. DOWNES ON THE CRETACEOUS BEDS thins out to the eastward of Sidmouth ; and my own investigations at Blackdown and Haldon will, I think, prove that at least the lower two thirds of the Blackdown series have thinned out in the hiatus which separates Blackdown from Haldon. I will heretake the opportunity of saying, as germane to the present subject, that I have afew additions to make to the list of Blackdown and Haldon fossils published in the Quarterly Journal of 1882. In that list, under the head “ Actinozoa,” appears ‘ * Smilotrochus Austem (EK. & H.) [? Trochosmilia| T. C.” As regards the Black- down form, I believe it ought to have been written “ Trochosmilia tuberosa (Ed. & H.) T. C. D.”; but the specimens are not good, and Prof. Duncan, to whom I showed them, would not be responsible for their nomenclature. This species, or one closely approaching it, is less uncommon at Blackdown than has been supposed ; but it comes from an horizon far removed from that of the Haldon corals, and therefore should not be confused with them. I obtained five specimens from bed 3 (see tabular view, Quart. Journ. Geol. Soc. Feb. 1882, p. 84), whereas the Haldon corals, mostly compound forms, are found in bed 13. After Inoceramus sulcatus, as Mr. Meyer has pointed out to me, ought to be added J. scrnisubentus. Nucula pectinata, Sow.,? variety. This species is referred to Blackdown in Morris’s Catalogue; but the actual specimen appeared to have vanished from all known collections. IL therefore omitted this species in my list; but I have since found it. Mr. J. 8. Gardner considers thaS my specimen more resembles those from the Chalk Marl than those from the Gault. Solarium, clearly allied to S. ornatum, but (as Mr. J. 8. Gardner has pointed out) differing from Folkestone specimens “ in the absence of the distinct row of ribs which extend about halfway across the upper part of the whorl.” The same correspondent informs me that my specimens very closely approach a form from the Grey Chalk. In the list of Haldon corals (p. 91) two of the commonest forms have somehow been omitted. I allude to Astrocenia decaphylla (Ed. & H.) and Isastrwa haldonensis (Duncan). ‘¢ Orbitolina-chert ” (bed 15). This, I am now inclined to think, is no distinct bed, but merely a local variation from an ordinary chert bed. I have also to add, from bed 13 at Haldon, Hlasmostoma Norma- nianum, of D’Orbigny. I am told by Dr. Hinde that this is one of the calcareous sponges, since silicified, and that this species also occurs at Warminster, and in the Tourtia at Essen-an-der-Ruhr. Discussion. Mr. Eruerines generally confirmed the correctness of Mr. Downes’s section. He stated that a bed of ‘ Carstone,” from 1 to 2 ft. thick, rests on the Lias of Black Ven. AT BLACK VEN, NEAR LYME REGIs. 27 Mr. Mayer stated that he had not been so fortunate in his visits to Black Ven as to find the bottom beds of the Cretaceous un- covered; nor had he succeeded in finding fossils in the sand above the Gault. He agreed with Mr. Downes that the Blackdown beds represent the whole or part of the Gault. He himself had thought at one time that the Blackdown beds might represent the Gault and Lower Greensand; but he had now been led to conclude that the supposed Lower-Greensand fossils from Blackdown were really of different species. The AvrHor was inelnied to regard the Blackdown beds as being rather Upper Greensand than Gault; but he did not think the. distinction of Gault and Upper Greensand could be made out in the western extension of those Cretaceous deposits. The term “Gault ” had been used in the paper to signify the black argillaceous bed, and not as a time-limit. There were certainly many Gault forms in the Blackdown beds. 28 SIR R. OWEN ON THE UPPER 4, Note on the RusemBLaNcE of the Upper Morar TEeTe of an EocenE Mamuat (Nzopracratitax, Lemoime) to -those of Tritytopon. By Sir Ricwarp Owen, K.C.B., F.RB.S., F.G.S., &c. (Read November 19, 1884.) Suortiy after the communication to the Geological Society of the paper on Tritylodon * I was favoured by the author, Prof. Lemoine, with a copy of his ‘ Mémoire,’ “ Etude sur le Neoplagiaulax de la Faune Inférieure des Environs de Reims *+. The chief interest of that ‘Mémoire* was, to me, the dental oo of the small mammal there discovered, especially those of the upper molar teeth ; while the general characters of the dentition, by their resemblance to those of the Mesozoic Plagiaulax, are also notably suggestive ¢. With a premolar, in relative size, shape, and sculpturing of crown, so closely repeating the peculiarities of that tooth in our Oolitic marsupial as to have suggested the generic name of the lower Eocene mammal of Reims (Neoplagiaulaa), were associated true molars more nearly resembling, in those of the upper jaw, the corresponding teeth of Tritylodon than did the teeth of the genera Microlestes and Stereognathus with which I compared them §. Figs, 1-3.—Upper Molars of Neoplagiaulax eoceenus, Lemoine, after Lemoine, Bull. Soc. Géol. Fr. sér. 3, tom. xi. pl. vi. figs. 17 u, GSC Ae: 1. From beneath. 2 & 3. From the sides. a. Natural size. The figures 17 w, 17 1, 17 e, pl. vi, of M. Lemoine’s ‘ Mémoire’ appended to the present note, will enable the resemblance of the upper molars of Neoplagiaulax eocenus to those of Tritylodon to be appreciated. In size the difference is almost as great as that shown by the molars of Microlestes ||. And here I may observe that, as the lower molars of Weoplagiaulagx have only two longitudinal series of tubercles, it suggests a surmise that the lower molars of Tritylodon may be found to present the same less complex character as com- * Quart. Journ. Geol. Soc. Feb. 1884, vol. xl. p. 246, pl. vi. t+ Bulletin de la Société Géologique de France, 3e série, t. xi. p. 249. { Compare “pl. v. figs. 1-3,” with figs. 9 and 16, pl. iv. of my “ Extinct Marsupials of England,” pp. 75 ie 87, in the ‘Extinct Mammals of Australia,’ 4to, 1877, p. 75. g Loct cit pp. 150, 151. || Loc. cit. pl. vi. figs. 8-10 (magn. 3 diameters). MOLAR TEETH OF NEOPLAGIAULAX. 29 pared with the upper ones; and, at the same time, that the rare detached molars on which the genus Microlestes is founded may be also those of the lower jaw. I add the following paragraph from the close description by Prof. Lemoine of the upper true molars of his rare and interesting fossil :— ‘“‘ Molaires supériewres (pl. vi. 17-17 bis) présentent trois rangées de denticules bien caractéristiques.”—“* La rangée médiane de denticules se trouve séparée des deux rangées latérales par un sillon assez large. Les rangées latérales de denticules bordent de chaque cdté la couronne ; les denticules en question sont de méme forme que les denticules médians, mais ils sont plus petits. Nous avons compté cing denticules pour chacune de ces rangées ” (oc. cit. p- 260). Here is indicated the chief difference, besides size, between the upper true molars of Neoplagiaulaw and Tritylodon. In the latter the tubercles (‘ denticules”) do not exceed three in number in the middle row and the inner row, and are but two in the outer row: and they are of proportionally larger size. Discussion. The PrestpEnt expressed his regret and that of the Society that the care which the author’s health now required prevented him at this season of the year from being present at the reading of the paper. ; Prof. Szzrzy referred to the discovery by Dr. Fraas of teeth of the Trias of Wurtemberg, to which he gave the name of T'riglyphus. Prof. Neumayr of Vienna had lately pointed out the resemblance between the teeth of Zritylodon and Triglyphus. He could not agree with the author in thinking there was any evidence that the molars of the lower jaw had only two rows of tubercles. Mr. LyprxKer also doubted the truth of the author’s suggestion concerning the teeth of the lower jaw. He thought that the con- dition of the teeth in the upper jaw of Tritylodon, the fourth molar being less worn than the fifth, pointed to the conclusion that this form belonged to the Marsupialia rather than to the Hutheria. 30 MR. METCALFE ON ELEPHAS PRIMIGENIUS AT CRESWELL CRAGS. 5. On the Discovery in one of the Bonr-caves of CreswEtt Cracs of a portion of the Urvrr Jaw of KLEPHAS PRIMIGENIUS, containing in situ the first and second Mirx-mowars (right side). By A. T. Mercatre, Esq., F.G.S. (Read November 19, 1884.) ' [Abridged.] I pxstRE to bring under the notice of the Society a portion of the upper jaw of Elephas primigenius, containing in situ the first and second milk-molars, discovered by myself in one of the bone-eaves of Creswell Crags. It will be remembered that these caves have, during the last ten years, through the exertions of the Rev. J. M. Mello, F.G.S., been systematically explored under the auspices of a committee of the British Association, and that papers describing the caves and giving the results of the explorations have appeared in the Society’s Journal. The specimen now on the table was obtained by me prior to these explorations. In securing it, therefore, I in no way interfered with any authorized investigations; for none had then been set on foot. I found the specimen in the red sand or cave-earth of the “ Pin-hole Cave,” and quite at its entrance. This cave is the most westerly on the north or Derbyshire side of the ravine, and has been fully described by Mr. Mello, who gives the following section of its beds (Quart. Journ. Geol. Soc. vol. xxxi. p. 681) :— 1. Surface-soil, containing recent pottery, bones &c., 1-6 inches. 2. Damp red sand. with rough blocks of magnesian limestone, quartz, quartzite, and other pebbles. and numerous bones, 3 feet. 3. Lighter-coloured sand, consolidated by infiltration of lime. No bones(?). Sir Richard Owen has very kindly undertaken to describe my specimen. He informed me some time ago that the National Collection had evidences of all the phases of dentition of the mammoth except the earliest, which is exemplified in the small anterior tooth in the portion of jaw discovered by me, and that the true value of my specimen would be its completion of the series now arranged for public instruction in the British Museum. I naturally feel that a suggestion from such a high quarter cannot be disregarded, and, in accordance therewith, I have undertaken to present the specimen to the British Museum. SIR R. OWEN ON REMAINS OF ELEPHAS PRIMIGENIUS. ol 6. Notes on Remains of ELEPHAS PRIMIGENIUS from one of the CRES-_ WELL Bonz-caves. By Sir Ricnarp Owen, K.C.B., F.R. ae - F.G.8., &e. (Read November 19, 1884.) Cuvier, in his chapter “Sur les Eléphans Fossiles” *, notices a fossil molar tooth discovered at Fouvent as having come from a very young individual and as being ‘“ une vraie molaire du lait ;” a figure of the grinding-surface is given, of the natural size, in pl. xii. fig. 2. The antero-posterior extent of that surface is 22 millim., the extreme transverse extent is 13 millim. The difference of size between the tooth figured by Cuvier and that preserved in the jaw in Mr. Metcalfe’s specimen is such as to suggest one of specific value; but the greater degree of wear to which the Cresswell-cave fossil has been subject, during life, and the inability to compare it with the original of the figure above cited, prevents such conclusion. The second detached molar figured by Cuvier, and noted as a “ second molar of a young mammoth,” shows no such increase of size: it is stated to have been derived from the environs of Toulouse. Subsequent figures and indications of the first and second molars ascribed to Hlephas primigenius represent, like Cuvier’s, detached teeth or tooth-crowns, leaving it undetermined whether they be from the upper or the lower jaw. In the account of the succession of the molar teeth of the existing Indian Elephant, the first molar, upper jaw, has a crown 20 millim. in antero-posterior diameter, 13 millim. transversely ; the crown consists of four principal plates and a fifth smaller one, or “ talon” tf. That the Elephas primegenius had a similar first grinder of the series was indicated by the socket in the lower jaw, from brick-earth at Ilford, Essex t. A reduced view is given of the crown of the second molar, lower jaw, from Kent’s Hole, showing eight transverse plates and a talon §. The specimen which Mr. Metcalfe has kindly submitted to me (figs. 1 & 2) 1s the first I have seen which demonstrates the cha- racters of the first and second upper molars in situ. It is a portion of the fore part of the maxilla, showing the bony palate, with those teeth of the right side ; the corresponding sockets and teeth of the left side are broken away. ‘The two molars have a longitudinal extent of three inches and one line (=78 millim.). The worn sur- face of the foremost has a length of 14 millim.; that of the second molar of 50 millim.; but the entire length (fore and aft) of this tooth is 25 inches (=62 millim.), the two hindmost divisions of the tooth not having risen into use. * Recherches sur les Ossemens Fossiles, ed. 8vo, 1834, tome ii. p. 175. t Odontography, 4to, 1845, p. 632, pl. 148, fig. 2, £ British Fossil Mammals, p. 223. § Ib. p. 224, fig. 87. ee ee nn ee ee ’ SIR R. OWEN ON REMAINS OF ELEPHAS PRIMIGENIUS. 32 Se: “> (Va) 3,8 ~ RS Ss) a D ss ooo 23 38 S S q 3 See 3 D a) Natural size ( Maxillary Bones of Klephas primigen ht side. Fig. 1.—Under or palatal v the rig : Mi a fm. a. Worn root of first. grinder. d,,d,. First and second grinders (Natural igenius. 1m the Right Maxillary, with yf the first and second Grinders cf Elephas pr = = S iS Ss > Qu 3 S 3 D > Ss iv) iS °sS ~~ S iS) ~ ea cs) 2. Fig d,, d,. Grinders. a. Worn root of first grinder. SIR R. OWEN ON REMAINS OF ELEPHAS PRIMIGENIUS. oe The worn, flat, and smooth surface of the first molar in annexed sketch (Fig. 1, d,) shows the foremost plate almost worn away ; the second plate retains a feeble indication of two of its mammilloid prominences ; the third and fourth plates have, each, indications of four such prominences; but their grinding-surface has been worn down to a hind “ talon,” which had just come into use. The original unworn or little-worn surface of this molar would have nearly the size of the tooth from Fouvent, and indicates that to have come from the upper jaw. The roots of the more worn molar in the Cresswell specimen are fully developed: the anterior one (Fig. 2, a) extends in a forward curve, with its closed end 13 miilim. in advance of the part of the crown it supports. The crown has been worn down to a subtriangular figure with the apex forward; the breadth of the grinding-surface near the base is 15 millim. The greatest breadth of the second molar (d,) where the hinder root begins is 17 inch (=32 millim.). Of this tooth, the fractured surface of the right maxillary exposes three roots, the first and second diminishing to their almost closed ends; the common, widely open pulp-cavity of the hinder root is also exposed ; its subsequent division into an outer and inner fang is indicated. The specific distinction from Elephas wmdicus is shown, in the present portion of Elephas primigenius, by the greater relative breadth of the second molar, especially towards the base of the crown. The thickness of the constituent enamel-clad plates is but little less in proportion to-the mass of the crown than in the larger variety (“ Dauntelah ” of Corse) of Hlephas indicus. But these plates show their specific proportions in a more marked degree as the subsequent progressively larger molars are acquired. The portion of the bony palate owes its transverse concavity chiefly to the development of the inner wall of the molar sockets. The broken surface above that plate gives indications of pneumatic cavities. In contemplating this rare relic I have not been able to suppress - sympathy with the unhappy juvenile British elephant, which, long ages ago, fell a prey to some dire contemporary spelean carnivore, by whose jaws the immature skull has been reduced to fragments. Discussion. Mr. Lyprxxer said that there was some ambiguity about the terms first and second milk-molars; they are better termed ante- penultimate and penultimate. There may be another anterior milk-tooth abnormally developed, and one specimen of the African Elephant in the British Museum apparently contains this tooth. The specimen now exhibited and described is not, however, the only one with the milk-molars in situ; there is another in the Bright collection from the opposite side of the upper ‘jaw, but from an unknown locality. Q.J.G.8. No.161. D 34 SIR R. OWEN ON REMAINS OF ELEPHAS PRIMIGENTIUS. Prof. SrELzy stated that a specimen of the full first dentition of Hlephas primigenius, comprising the teeth of both upper and lower jaws, found in the gravels of Barnwell near Cambridge, was formerly in the Woodwardian Museum. It was lent to the late Dr. Falconer, and after his lamented decease it could not be found. Dr. H. Woopwarp stated that a specimen of Hlephas antiquus, with milk-molars in situ, existed in the Museum of Practical Geology. He was not quite certain whether the specimen on the table did not belong to the same species. The specimen in the Bright collection is also labelled H. antequus. Young teeth of E. primigenius have been found in abundance at Ilford and elsewhere in the Thames valley, all proving that the animal was indigenous in ‘Britain. The specimen exhibited was of great interest as its exact locality was known. Mr. E. T. Newron remarked that the specimen in the Museum of Practical Geology was similar to that on the table, but it was very difficult to distinguish between the young molars of the two species referred to without careful comparison. Mr. Mercatre expressed his thanks to Sir Richard Owen for his kindness in describing the specimen, and to the Fellows of the Society for the manner in which they had received this communication. [Pie a Ly Vinee \ Quart.Journ.Geol. Soc. Vhntern Bros .imp. 3 Foord del et hth. AS EGON TAs.. E. A. WALFORD ON THE TRIGONLE OF N, OXFORDSHIRE, ETC. 30 7. On the SrratigRaPuicaL Positions of the Tricont# of the LOWER and Mipptz Jurassic Beps of Norra OxrorpsHirE and adjacent Districts. By Epwixn A. Watrorp, Esq., F.G.8. (Read November 19, 1884.) [Puare I.] A wett-defined family of the Mollusca making its appearance and attaining its maximum development within a limited geologic period must necessarily be of exceptional interest to the paleonto- logist. Such a family, the Trigoniz, though from their irregular dispersion and less vagrant habit inferior to the Ammonites as stratigraphical guides, supply nevertheless no unimportant evidence thereon, finding, as they do, a birthplace in the lower beds of the Lias, and in the Inferior Oolite leaping into such numerical luxuriance that Dr. Lycett has well described it as “a very metro- polis of the Trigonie.” Though fairly represented in the higher Jurassic series, yet with gradually diminishing importance notwith- standing a brief Neocomian revival, they range through the Meso- zoic period, and now in Australasian seas linger as the remnant of a once dominant race. In wealth of individual forms as well as in number of species the narrow Jurassic area of North Oxfordshire stands prominent. As elsewhere, the Lias species are few. Liassic SPECIES. TRIGONIA LINGONENSIS, Dumort.—In the zone of Ammonites Henleyr of the Middle Lias of Banbury a doubtful cast of this species has been found. Ihave recorded it also from the zone of Ammonites spinatus* at Kings Sutton and Aston-le-Wall, localities on the borders of North- amptonshire. At Preston Capes, in Northamptonshire also, it has been collected by Miss Baker’. TRIGONIA NORTHAMPTONENSIS, nov. sp. (PI. I. figs. 4-7.) The few immature forms of this species which had come under my notice until quite recently caused me to refer them with some degree of hesitancy to the Yorkshire shell 7. hterata, Y.& B. The adoption of a new name has seemed necessary under the additional light thrown by the acquisition of a better-developed series of examples and by an expression of opinion from a paleontologist of wider experience than myself. Though perhaps the differences between the two forms may to some extent be due to regional varia- tion, yet we have to remember that in the course of the Lias from Yorkshire through Lincolnshire and Leicestershire, no connecting link seems to have been met with. * “On some Middle and Upper Lias Beds in the Neighbourhood of Ban- bury,” by H. A. Walford (Proc. Warwicksh. Nat. & Arch. Field Club, 1878). Tt “On the Middle Lias of N. Gloucestershire,” by the Rev. F. Smythe, M.A. (Proc. Cott. Nat. Club). | D2 36 E. A. WALFORD ON THE STRATIGRAPHICAL Shell ovately trigonal, moderately convex, umbones erect, pointed and antero-mesial. The specimen (fig. 5, Pl. I.) measures in height 14 inch, breadth 13 inch, depth through both valves 13 inch. An- terior side produced and curving somewhat steeply to meet the lower border ; superior border slightly convex, making but a faint angle with the lower-area border. Inferior margin of the shell rather straightened. Escutcheon concave and lengthened. Area convex, occupying about a quarter of the surface of the shell. Marginal carina depressed and not prominent; mesial line of the area indi- stinct ; area covered with fine transverse lines. The nearly perpen- dicular coste, about ten in number, proceed from the marginal carina downwards, beginning near to the umbones; they are boldly marked until they reach the transverse subtuberculate coste pro- ceeding from the anterior margin. The transverse costee dip gently downwards from the anterior border. Traces of transverse strie cover the better- preserved. portion of the surface. The example described is much less convex than 7’. literata, and in the ornamentation the perpendicular costz are not prominent over more than a third of the surface, whereas in 7. literata that series occupies its larger portion. A second group of shells (figs. 4, 6, 7, Pl. 1.) presents many points of divergence from the form just described. In some of them, as in figs. 6 & 7, the outline is more oblique, and the anteal costee are either reduced to insignificant proportions, or are appa- rently absent. This condition much resembles the type of shell figured by Lycett (pl. xiv. fig. 4, Brit. Foss. Trigoniz), who speaks also of the very variable ornamentation of 7. literata. The per- pendicular cost of this variety of Trigoma northamptonensis enlarge as they pass downwards from the marginal carina, and cross towards the anterior or lower border. Fig. 4 presents an intermediate stage between the forms repre- sented by figs. 5 & 6. The anterior tuberculate coste are seen curving slightly downwards, transversely, towards the posteal series, the space between the two series being occupied by a few scattered tubercles. Trigonia navis, Lamk., has a more trigonal contour, and a nearly vertical anterior border. The Northamptonshire shells appear to be local representatives of the group Scaphoide, finding a place some- where between 7’. navis, Lamk., on the one hand, and 7’. hterata, Y. & B., on the other. Their state of preservation is far from satisfactory: the soft test has peeled off more or less by adhesion to the tenacious blue clays in which the shells are imbedded, and this has in nearly every case destroyed the beauty and prominence of the ornamentation. Perhaps the finding of better examples may ultimately allow the two varieties figured to be recognized as species. ni am indebted for my specimens to Mr. B. Thompson, F.G.8., of Northampton, who has been describing the Lias deposits of the county. The Zrigonie were obtained from Moulton, near North- ampton, and rough casts have also been found at Bugbrook in the POSITIONS OF THE TRIGONIZ OF NORTH OXFORDSHIRE, ETC. 37 same county. ‘The interest of the discovery is further enhanced by the recognition of the exact horizon of the fossil, at nearly the top of the Upper Lias and below Mr. Sharp’s stage E of the Northampton Sand. Mr. Thompson’s notes on its position agree with my own. He writes, ‘‘ The shelly band, a few inches in thickness, is about two feet below the junction (with the Inferior Oolite) where now work- ing; but the men say it dips so rapidly on each side of its present position that they had met with it in the same pit thirteen feet below the junction.” The associated fussils are Ammonites bifrons, Brug., Gresslya donaciformais, Phil., Inoceramus dubius, Sow., Pro- tocardium substriatulum, d’Orb., Cucullea, sp., &e. TRIGONIA PULCHELLA, Ag.—This also, an Upper Lias form, has been recorded from the neighbourhood of Northampton, though only as a Drift fossil*. Probably ere long we may hope to have a record of the discovery of the species in situ, as a layer containing small uni- valves (Cerithium, &c.), similar to those found by Mr. W. D. Carr, in the Upper Lias of Lincoln? associated with J. pulchella, has already been noted by Messrs. Thompson and Crick. The Lincoln- shire horizon of 7’. pulchella appears to be much lower than that of T’. northamptonensis, the former being at the base of the Leda-ovwm beds, the latter towards the top. INFERIOR OoLite SPECIES. The Trigoniz of the Northampton Sand have been catalogued by Mr. R. Etheridge, F.R.S.t, and by Mr. Sharp, F.G.8.§ It should, ’ however, be borne in mind that the Inferior Oolite of Oxfordshire neither satisfactorily agrees with the “‘ Northampton Sand” on the one hand, nor allows of easy correlation with the Cotteswold type on the other. Inasmuch as the latter series has presented many points of relationship, I have attempted a: comparison ||, and have summarized the matter in the following table, here slightly altered :— * «On the Drift deposits of Wymington,” by W. D. Crick (Northampton Nat. Hist. Soc. Proceed. 1883). t ‘On the Lincoln Lias,” by W. D. Carr (Geol. Mag. April 1883). { Appendix to Prof. Judd’s Geol. Rutland, by R. Etheridge, F.R.S. (Mem. Geol. Surv. 1875). § ‘‘Oolites of Northamptonshire,” by 8. Sharp, F.G.S. (Quart. Journ. Geol. ‘Noe, vol. xxvi. p. 388). | “On the Relation of the so-called ‘Northampton Sand ’ of North Oxford- shire to the Clypeus-grit,” by Edwin A Walford, F.G.S. (Quart. Journ. Geol. Soe. vol. xxxix, p. 224), ; 38 E. A. WALFORD ON THE STRATIGRAPHICAL “ampoug vvwobut 7, ¢ 0909800 “7, ‘a vsopnueds «7 “nadjnos «7, “ppnaugs *7 ‘varpoug nrtohut 7 ‘spgynd ‘nunhansoog wruobrl, 7, Ww "SISWALUWONO "LBA ‘Uopawony \T, “oops ‘TD, ‘sngnd 7, ‘opwubrs «7 ‘ogmur -wab “7, ‘wsind “7 ‘ogonp -oud “7, ‘ognjnbun nriobo7, “g0gsoo 7, ‘pponp -oud 7, “ogninbuo nrutobuty, A ¢ padrwos “0 i ‘“vanjpsoo = mouobrny, "9900 “iy “J, ‘vaonpoud «7 “vyn) ~noywap 7, ‘oyowubes nrwobe 7 ‘WINODIU,T, —_ —_—__. — dsosuaunl wupr “oynauyrup art DInanIgauaT ‘wavLOOApgns aT |r**tt ttt tereeeses Toppy ‘pyoydooouha wyjauoyouhyar \KopyQ ‘HO¥LONT YOOTT ‘swobojo anwnysp ‘snavbirusoop sano |"** OqUoortyAT ‘T[LEL sna) "vy ‘muosryoinpy “wp |KoYYOQ “KOJLON’ YOOTT "UpYOULA, DOLSVUUWOY T, ‘nysuoyy §— waugscQ “4 vhg ~hamog “Uo “pp0wo wownar \''"*'*** TITEL oqutoog9 “Yuop ORT “vunaghuoy vMugsnsy “DUNUIuh apLDIS ‘“DaDINH rr t*errrereereeeee THT -up'Yy ‘vsourds nyjauoyouhyar \kopyQ, “u0YLONT YOOTT "S[RIOC) ‘2200p -OUJVE “nupapugajqns vyjow |" mojo; Surddigqg -oyouliyey “ouvir aguogspy |*qysiaypoyy SLOT ANT “psogqub Duy “D2nq “oj myngmuqaway, “nppopg |" woysoyy SurddryD snadhig “wuosmywg “wp \4ustToy ‘dopAnyy say |reeteeeeseesstt09.0 NT -ofupiwo nuvy ‘vunw |surddiyg “uot anspy “wmosmylog ‘wy \-|{Ox ‘UOILONT YOOTT ee ov eeeeesee {USAT [Oy *TO4L0 NT “MOUNT ‘DLDONT ‘yang ‘snuabysngio “uy “STISSOH *ALITVOOT "a sasuaune ‘Uupy “DUosrtyounyy “Wy “DUOSryoInpT “Ur meres onupisauyd unt “Uy KO QUOSULY LT “210sUury Wg “Ut ¢2[0O JUL "NOZINOPL “Uy | V | Suiddiyy |purv ygaegy 8.10707 eesees 66 iG (TS Vv ** QUOWSOUMITT poytvoy-ontq Apuwg +E eesseaneenteenennreseentesseres BTBIOD UGTAL BOUOISOWLLT POCMO[OO-WUIVIAD OT}I[OO “EL OO ee ee ee ey SLB], pu souojsouliry yoysuoaT pus ATqqnyy *O sole tieieiy)s/oaisie vivieicieivipluipieies se ane. q1d9~BIMO STAT, LOMOTT =poq-quouroseq y1ad-snodATO *.O rirvnesrceeeormerseeres areBgnod dig ‘20 CCC ee etree eH ee eeeeeeeeeereeeeeeeeeeeeee SVL pus souojsoury Ayavur pue Apurg ‘q Peer ee eer eee eernee see (ouogsoumiry T0}.L0 NT -suiddigqg) Apues pue snoodiqis uoqyo ‘guoqysouniry AOAd LO Pornopoo-wivatg “Of "NALVULG ‘auryspsefog yon fo 900 wordafuy oyp fo suorsrarg fo 219], POSITIONS OF THE TRIGONI® OF NORTH OXFORDSHIRE, ETC. 39 As far eastward as Chipping Norton and Fawler, in N.W. Oxford- shire, the continuity of the upper beds of the Inferior Oolite of the Cotteswold type (the Ragstones or Clypeus-grit) is easily traceable. North-eastward of these points, however, so widely different are the conditions of deposit that Mr. Hudleston has well said * :—‘ The beds of this region have a type of their own, and it is no use trying to force them into the ready-made clothes of other districts.” The bed (C‘) at the bottom of the Clypeus-grit (C*) at Fawler, and that at the base of C at Hook Norton are similar lithologically, and both contain an abundance of concretionary and derived fragments. Associated with these in each locality are corals of similar species, blocks of limestone covered with oysters and pierced with Lithodomz, numerous shells such as Astarte minima, Ostrea Marshu, Isocardia, sp., Trigona producta, T. costata, and T. angulata. With so many features in common, it will be safe to assume the connexion of the seas of these areas with each other at the time of the deposition of the bed, whilst the irregularity of its occurrence at F'awler, where the bed rests, as at the Duckpool-Farm cutting, near Hook Norton, upon the Upper Lias, points also to long and continued erosion in the antecedent period. ‘The classi- fication of these beds with the zone of Ammonites Parkinsoni on the one hand, or the zone of Ammonites Humphresianus on the other, will depend much upon whether we look to the Cotteswold or to the Dorset types for comparison. The fauna is that of the Lower Trigonia-grit, a division, according to Dr. Wright, of the zone of Ammonites Parkinsoni, but placed by Mr. Witchell + in the zone of Ammonites Humphresianus. If the remains of the bored bed represent, as seems to be probable, the well-known Upper Freestone bed, then it would point to the destruction of that stratum prior to the formation of the lowest bed of series C. The ‘ Supplementary Monograph on the British Fossil Trigoniz,’ by the late Dr. Lycett, published in 1883 by the Paleeontographical Society, has done much to increase our knowledge of the strati- graphical position as well as of the species of the Oxfordshire Lower Oolites. Some additional information accumulated since the materials were sent to Dr. Lycett in the early part of the year 1882 has induced me to proffer these notes to the Society. Trieonta Broprer, Lyc., a pretty little local species, is not un- common in the Lower Inferior Oolite beds A and B’. Its occurrence ‘in any higher stratum is doubtful. It is nearly allied to 7. formosa, Lyc., of which it may possibly be a local development. The pro- minent distinguishing feature between the two species consists in the more vertical position of the lower coste of 7’. formosa. The beds A and B seem to represent the zones of Am. jurensis and Am. Murchisone. * “Report of the Excursion of the Geologists’ Association to Chipping Norton,” by W. H. Hudleston, M.A. (Proc. Geol. Assoc. vol. v. no. 7, p. 9). t ‘Geology of Stroud,’ by E. Witchell, F.G.S., p.57. Stroud: 1882. = 40 HE. A. WALFORD ON THE STRATIGRAPHICAL TrigonrA FoRMosA, Lyc.—Though it may appear unsatisfactory to class 7. Brodie. T. formosa, and T. striata from the same horizon and locality, yet certain well-developed shells of the “« Brodiec” type pass away into forms which agree so well with moderate-sized examples of 7. formosa that it.seems to be necessary either to make 7. Brodie a variety, or to admit the former into the Oxfordshire list. Locality: Hook Norton, beds A and B'. Triconta strata, Miller, is found sparingly and in an indifferent state of preservation in the beds A or B' of Otley Hill. In Glouces- tershire, according to Wright*, it occurs in the ‘“Cynocephala stage,” whilst Lycett records it from the zone of Am. Humphresianus only, referring the shell from the lower zone to J. formosa. T. striata is catalogued as common in the Lincolnshire Limestone. Other Survey Memoirs f quote it from the Great Oolite. Trigonra stenata, Ag.—The four varieties of this species figured by Dr. Lycett in his Supplementary Monograph, occur in an admirable state of preservation in the higher divisions of the Inferior Oolite of North Oxfordshire. In the beds C of Hook Norton the first forms appear associated with Astarte minima, - Rhynchonella spinosa, and many other species of mollusca, but they become the dominant fossils in the superior stages of other localities. The matrix of the latter stages is either sandy or an intensely hard compact siliceous limestone, from which the extraction of the shells is exceedingly difficult. A bored bed occurs above the Upper Tri- gonia-layer at Hook Norton. Some undescribed forms of Trigome, to which I shall presently allude, were procured by me some years since from the Trigonia-bed at Sharpshill near Hook Norton. At the Priory Farm by Chipping Norton and at Grayton Quarry near Whichford numerous specimens of the several varieties may yet be obtained, but in other localities they are now rare. 1’. signata, var. Stutterdi, and var. decurtata, have both been found in C of Hook Norton and Otley Hill; and though Dr. Lycett has referred the former to the superior beds, probably it would be better to restrict the varietal name to the shell of the lower beds (figs. 9 and 10, pl. u1. Foss. Trig., Supp. 2), which is like those found at Cold Com- fort near Cheltenham, and distinct from its allies of the later deposits. 7’. signata, vars. Zieten, rugulosa, and decurtata, occur in the higher series. Though in Yorkshire 7’. seqnata belongs to the zone of Ammonites Humphresianus, in the south-west of England Lycett gives the Upper Trigonia-grit as its only horizon. TRIGONIA sPINuLOsA?, Young and Bird.—A solitary and, unfor- tunately, imperfect example from bed B* of Hook Norton has many points of resemblance to the shell figured by Lycett (pl. i. fig. 6, Brit. Foss. Trigoniz). The tubercles are more distinct than in any * a < 39” > o °o (eee = eee Or é 23” q ives 5 an =: le To a yi” SS nee Beach ae a. Glacial deposits. 6. Greenish-grey tuff. e. Sandy clay with broken shells. d, Sandy clay, unfossiliferous, e. Sandy clay with fossils. Ff. Sandy clay without fossils, with a band of laminated sandstone with green grains. g. Four bands with Cyprina, the bottom layer with Acteon Noe, and Cardium echinatum. h. Bands of broken shells, with Cyprina, Acteon, and Cardium. 4, cabanas band of comminuted shells of variable thickness, average eet. . 12 1} |! Ik 96 J. 8. GARDNER ON THE TERTIARY separated from each other, the first from the second by 4 feet and the others by intervals of 3 feet each, of a more compact mar! of an almost stony character. The whole is capped by 30 feet of sandstone without plants. About a mile further east the lignites thin and are only four in number and of less uniform thickness. The base is still formed of greenish, indurated, sometimes ferruginous, sandy clay, about 200 feet thick, passing towards the west into a basaltie breccia at its lower part. The lowest bed of lignite is 18 inches thick, and the other three 1 foot each, separated respectively by 16, 12, and 6 feet, and the uppermost surmounted by 14 feet of matrix, termi- nating with a conglomerate of rounded pebbles. Half a mile beyond this, to the east, the whole of the lgnites dip below the sea-level. A mile further along the coast, at the angle of a chine, is the section shown in fig. 1. The fossiliferous beds rise inland, and cannot be traced more than a few hundred yards up the chine. They are much faulted,—one fault up the chine had a downthrow of 60 feet,—most of the faults being in a N.N.E. direction or nearly parallel with the shore, pro- ducing sometimes an apparent overlying of the shell-beds by the lignites (fig. 2). = ig. 2.— Fault causing Shell-beds to be apparently overlain by Lignites, near Hisavik, Iceland. a, Lignites. b. Lignites concealed by débris. ¢. Shell-beds. Much of the matrix, especially towards the base, is exceedingly like our London clay. The shells occur in pases and particular species are confined to particular horizons. Across the chine the beds almost immediately dip out of sight (fig 3), and are succeeded by higher and unfossiliferous beds, more compact and indurated, and paler i in colour. These are also much faulted. I ceased to take notes beyond the Cape, but I subsequently rode along the coast to the extreme point of Tjornes, where I understood oes had been met with; but for ten miles the unfossiliferous bed seemed to continue w ithout any change. I endeavoured to determine some of the species by comparison at the Jermyn Street Museum, and submitted the list of names which resulted, and the specimens, to Mr. Searles V. Wood and to Dr. J. Gwyn Jeffreys, who very kindly furnished me with the details embodied in the accompanying table. Dr. Mérch, in the work referred to above, gives a list of 58 [To face page 96. tsrRIBUTION and RrmarKs by SEARLES _ V. Woop, Esq., F.G.S. ‘o10T.M PUB ‘jou «0 SULATT MO OAMAae "0991p Jo 42d qsomo yy ROKR KX "0741p Jo yavd | x xxIx]3 ULLUE LO OTPPTFL Jn Jo]> Jo yaed qsaptO | “SVIQ OUTT[RI0D | | aarks. ||" +> Se oe Q.J.G.8. No. 162,] List of Fossm Suntts collected by Mr. J. Srarnre Garpner [Lo face page 96. ante of Distrruston and Remarks by SEARLES in Icetann. By J. Gwyn J pFFREYs, LL.D., F.R.S. V. Woon, Esq., F.G.8. er eedie 6 |2ulasls se gs = S) a é Z F Name of Species. Synonyms and remarks, Suleecniecr nam eas e)/2/ 5] 3 a |33 /a8 | 22 a PlE\a |: 2 | 28 |24)| €3| 23 ‘| 8 Ce SSatee a eee ConcntrEra. = — | «+ | Oardium echinatum, Dinné...t...ce-cceeesse. var = = = = islandicum, 2, ae == || = — |—— groenlandicum, Chemnitz ee ae —|—]|— |... | Cyprina islandiea, hg CaSO S RCE ROSE CORD EECO RE Banna] hone arcrcr as ure nua ne x 2 S ° B —|—}|..- | — | Astarte crenata, Gray . crebricostata, Forbes a = a x B —|—]—]|— |= compressa, Montag AVC SURIEtEN eee etey ey = ? x x B — | — | — | — | Tellina ba’ NGO Del ee RP a ot ak — _— — x B —|— — |——ealearia, Ch, . | And var. obliqua . x x x x ub) = — | — | Mactra solida, Z. ... oe a _ — x x B — | — Mesodesma deauratum, Turton oan oh —_— —_ x xe A —|{|— Glycimeris siliqua, Spengler .. 2G. angusta, Nyst, fide Scarles Wood x = x = H Bee ec eck Neh DIATE eels A eh TS tee een ie x x x B — | — | — | — | Saxicava norvegica, Sp. Gasrropopa, 5S | | Eaittonin ailitttonen Lita eneraan crenata) | ede eee mee eve a, Sete = = x x B = |= Natica heros, Say... ..| N. catenoides, Searles Wood = x x — 1D) = || — — affinis, Gmelin ..| Var. occlusa. — — aperta, Lovén ... .| Bulbus flavus, Gould. —|— — | Buecinum groenlandicum, Ch. ........... 20 = x = = G _ Murex cinereus, Say. _ — | Pusus despectus, Z. — curtus, Jeffreys. F. Stimpsoni, Morch; FP. Olavii, Beck ? ? — Nassa trivittata, Say ?N. propingua, Shy.; Searles Wood ... — x x _ A? atl sarin fons INONEVBIS) 2H ONO Spree eeae sy aston eee wees Reaee | Sedoore ee a = = x — E — | — | — | Pleurotoma turricula. Montagu Var. Fusus harpularius, Couthouy — x | x x B — |... | — | —— pyramidalis, Strdm...... F. pleurotomarius, Cowth. .... — — x x A ae === bicarinatas Gowth nc mes vssecierve eee | ER Ee ee = = | x — A — ?— Actwon nom, J. Sowerby -|? Tornatella pusilla, Mord. .... — x x — uD) | 20)} 23) || 10!) 18 27 | | Notes on Dr. J, Guyn Seffreys's List. The term “ Arctic” in the fourth column of this list includes not only those parts of the Atlantic and Pacific Oceans which belong to America and Asia, but also those parts of the European seas which lie within the Arctic circle. The list shows that of the 27 species collected by Mr. Gardner, 20 are found in the English Crags, 23 live in the North-American seas, 10 only in the Huropean seas as aboye restricted, and 18 in the Arctic seas of both hemispheres. It also shows that nearly the same number of species occur in the Crag and North-American seas; 16 species are common to both those categories; 5 appear to be American, and 3 Arctic, none of which are Crag. The con- nexion between the Crag and North-American Mollusca is therefore more intimate than between the Crag and European Mollusca, not taking the Arctic Mollusca into account. ‘Two species, and those questionably, are supposed to be extinct. I should regard this Iceland deposit rather as Post-tertiary or Quaternary thun as Pliocene, : All the non-existing species are inhabitants of comparatively shallow water ; some are littoral. The peculiarly North-American species (Mesodesma deauratum, Natica heros, Murex cinereus, Pusus curtus, and Nassa trivittata) have not heen recorded as living on the Icelandic coasts. Iceland is Seographically separated from North America by Greenland, where the marine Mollusca are more European than American *. But the course of the Great Arctic current is from Iceland to Newfoundland and the western coasts of North America; and this may account for the former occurrence of North-American species in Iceland, as evidence of their origin or source of distribution at that epoch when the shells were overwhelmed by a volcanic flow of laya. All the Mollusca which now live in the Icelandic sea are either Arctic or North European, and haye apparently been derived from Spitzbergen or Finmark by means of fhe same current which ewfoundland. ‘ ~ nated form which is Arctic, not British. ~ extinct. Notes on Mr. S. V. Wood's Table. B, Signifies living in British seus and elsewhere, A. On North-American coast only. G. Greenland and Arctic seas only. E, Not known as living. The large carinated shell referred to (p. 96) is probably Lrophon an- tiquus, yar. carinatus. Mr.8. V. Wood remarks that only the sinistral form of 7. antiguus occurs in the oldest part of the Red Crag, and this not carinated. Both the sinistral and dextral forms of var. carinatus occur in the middle part of the Red Crag. It is the cari- To these we may add the following species, overlooked by Dr. Gwyn Jeffreys, identified by Mr. Searles V. Wood, and also occurring in the paper by Dr. Mérch on the Iceland Crag at p. 321 of vol. viii. of the Geol. Mag. (1871) :— Buccinum Datei, only a fragment or two of which are known from the Coralline Crag, though it is yery abundant in the older and middle part of the Red Crag. Pleurotoma hispidula, a rather doubtful Coralline-Crag species, now liying in the Mediterranean. Mactra arcuata, known throughout the Crags and extinct. Tellina obliqua, rare in coralline and older parts of the Red Crag, but abundant in the rest of the Red Crag and in the oldest Glacial ; beds, ‘Treated as a variety by Dr. Gwyn Jeffreys. art 1, pretenuis. Very abundant in both middle and newest part of Red Crag, but rare in the oldest Glacial beds. In the newes: h of the Red Crag both these Tellens are associated with the Arctic species, 1’, calearia, which occurs in all Glacial beds L. obliqua and L. pretenuis are unknown from any but the oldest Glacial beds, and of the east of England only. They ar “ ; “ to ‘sip Mi fe ip BASALTIC FORMATION IN ICELAND. 97 species, at least 16 of which are of very doubtful value. I was unable to extract a large fusiform shell, which was much cracked, and in an almost inaccessible position ; but I made a drawing with measurements, before attempting to remove it, and saved the greater part of it. This can be reproduced when necessary. . a eo] —e Oe i) g <™. i : a D isn) ~= >. S = 5: on ao = -- 2 S a S on. e Lo = - 3 SS o°O Cie = leg as (oF) 2 a & >. ~ Ss S = S Ss =~ > & I z es © S = d ~? ots oe a A z.9 SS ae eae =: & z. Oe: SS =a rr) : Bet 5 a ’ on: SN . & = Alt. ; S Au . . — : ian! r ~N % Pa eee = + ites o i Ly = : = Si SS = i y Sg ry = ATHH Mp = m Dr. Gwyn Jeffreys has some valuable remarks to make upon these fossils ; but as I believe that further specimens have been submitted to his inspection from abroad, I trust he will be induced to com- municate a paper on the subject, which I forbear in any way to forestall. I think, however, I should, for various reasons, be in« clined to assign a greater age to the deposit, from its general 98 J. S. GARDNER ON THE TERTIARY a appearance on the spot, than Dr. Gwyn Jeffreys may do, or even than Mr. Searles Wood. ‘The occurrence of the fauna of the Red Crag, with Mediterranean species, so many degrees north, would dispose me to consider them as belonging to a somewhat warmer climate and therefore presumably to a rather earlier period than I should do if meeting with the same assembiage further south. This part of the country is a table-land, with mountains some distance inland, from which lava streams have issued in relatively recent times. Nearer Hasavik the chffs are of basalt and volcanic breccias, and to the east the plateau is composed of horizontal basalts with a thick alluvial capping of loam, ready to produce a bed of laterite if ever again overflowed by lava streams. It is impossible, from the coast-section, to form any just idea of the relationship of this sedimentary formation to the Tertiary basalts ; and the determination of its precise age cannot, unfortunately, at present throw any light upon their history, though presenting a problem of great independent interest. Coal is said to occur near the base of the mountains on the opposite side of the bay, facing Husavik; and as these do not present a basaltic contour, they might be worth investigation. TsaRNir (“short lakes”). About 25 miles due south of Akreyri is a valley the sides of which, about 2000 feet high, are composed of basalt, searcely intersected by any dykes. The coal reported to be found here proved to be obsidian. The rhyolitie lavas overlying the basalts form a very important series at this point. SANDAFELL (not the Sandfell marked on maps). This mountain is situated about 25 miles S. of the Skagafjord, and 6 miles above Abaer, the nearest farmhouse, on the river Banda. The basalt is covered by a clay bed with rootlets a foot thick, succeeded by brown coal passing into lignite, another foot, and then 150 feet of voleanie breccia, with large blocks of basalt imbedded towards the base. There are then 30 feet of pale tuffs, and a band of pitchstone decomposed into vertical needles overlain by pink and ivory-coloured banded rhyolites, and finally basalt. This section is at the angle of the two valleys formed by the rivers Tinnaa and Banda; and, looking up the former, the pitchstone band is conspicuous between the lighter masses for at least a mile, being on the right hand at an elevation of about 600 feet, and at least 800 or 900 on the left. Up the Banda the hgnite thickens to 3 feet. Well-preserved leaves have been obtained from the yellow tuff, and are now in the University Museum at Copenhagen. Though I searched diligently, I was not fortunate enough to discover any bed with fossils worth bringing away. At the corner of the Tinnaa are magnificent groups of columnar basalts, bent in many directions, and twice fanning out like the clam-shell eave at Staffa. Some fallen segments measured 3 and 4 feet in diameter. The pale- BASALTIO FORMATION IN ICELAND. 99 coloured rhyolites reappear in all the mountains at a high level as far as Akreyri. Hor. A few miles south of Godalir, at the angle formed by the first tributary to that river on its left bank, the section has been cut through by the stream, and forms a perpendicular bank 12 feet high, in which are over twenty layers of lignite separated by gritty marls and ferruginous bands, crowded with vegetable matter, with a soft sandstone at base, similar in appearance to that of Husavik. At 12 feet a bed of lignite composed of compressed tree-trunks occurs, and then another, 3 feet thick. The bank then slopes at an angle of 30° for a distance of 60 feet, still abounding in lignitic matter, when it is concealed by the greatly overhanging remnant of an old moraine. On the opposite, or south bank, the same beds are capped by columnar basalt. The plants again proved to be nothing but rush-like monocotyledonous débris, with seeds, and probably remains of Chara. ‘The dip shown in both exposures (S.H. and N.) is 9°, and the formation is probably extensive. The diameter of the largest compressed trunk I extracted was 20 inches; but this did not seem to be the full width. There were many large trunks in the bed of the stream, the branching of which suggested willows of large dimensions. In this neighbourhood, about 7 miles from Hofsgil, a magnificent section of over 1000 feet in depth can be studied (fig. 4). It forms the side of one of the wildest conceivable gorges or cafons. The precipitous and even perpendicular sides are composed of more or less columnar basalts, separated by partings of almost vermilion-red earth, which has stained them a reddish purple. Where the sides are not perpendicular, fragments of the old moraines, cold slaty grey in colour, cling to them, weathered into fantastic shapes and looking like ruined masonry. The torrent is just visible as pure white foam at the bottom. The section here reproduced is of general interest as showing the composition of the ordinary North Icelandic mountain from top to bottom. Its upper part, as viewed from across the gorge, forms a slope of from 50° to 60°, and overhangs a tremendous precipice, so that it would not be accessible without great danger. It is evidently similar to Sandafell, not many miles distant; and that the black band is really lignite is apparent from my subsequently picking up pieces in the bed of the river. This gorge was evidently at one time filled in solid with Boulder- clay or moraine, and enormous masses of rolled stones are spread over the valley below. The stones have been arranged into sharply defined terraces. A river entering from a valley to the east had accumulated an enormous mass of shingle, before the main river cut its way through and cut down at least half the area to a level of 30 or 40 feet lower; after which the rivers united and further reduced it as much again, affording an instructive example of terrace- formation. A better clue to the formation of parallel roads is furnished by a 100 J. S. GARDNER ON THE TERTIARY small valley, marked Sandklettavdtn, about lat. 64° 21’, between Reykholt and Thingvdlla. Itis marked as a lake without any outlet ; but in August there was only a little water at one end, the stream Fig. 4.—Cliff and Ravine about 7 miles from Hofsgil, height about 1000 feet. Po a Wii a Wi Wily J a. Boulder-clay. a’. Boulder-clay weathered into architectural forms. 6. Basalt. b'. Basalt with partings of bright red and brown earth. e. Rhyolite. d. Sedimentary rocks, about 130 feet, chiefly yellow and drab sandstones, with two intercalated bands of lignite, marked xx. connecting it with Ukavdtn being also dry. The plain is level, destitute of vegetation, about three miles long and one broad, closed in on three sides by mountains and on the fourth by a lava-stream. Its shores are regularly terraced all round, the terraces being only 2 or 3 feet high. It is evidently a shallow lake for a great part of the year, and the terraces have some connexion with the recurring formation and disappearance of a dam of snow or ice at its eastern extremity. BASALTIC FORMATION IN ICELAND. 101 HREDEVATN. This is a small lake in western Iceland, lat. 64° 41’. A bed of coal occurs in a romantic ravine about 800 feet above the lake, and towards its northern end. The coal is but 18 inches thick, and is immediately under a bed of basalt, with yellow tuffs underneath it. It reappears in a gully 100 yards to the N. W., with a dip of about 15° to the 8. W. The section is entirely overgrown and covered by earth, and would require much time to uncover ; but I exposed a bed of brown papyraceous shale, and underneath it a short brittle sandy clay, with rootlets and vegetable remains. Above the shale there was yellow tuff; but several hours’ search brought forth nothing in the shape of well-preserved leaves, though they are stated to have been found in the tuff at this spot. Another lignite or coal bed is said to occur four hours’ ride to the west. The coal is used for fuel, but is as costly to obtain, owing to its inaccessible position, as sea-borne Scotch coal. SraAFHOLT, This locality is a small promontory six or seven miles south of Hredevatn, on the banks of the river, and nearly at the sea-level. The point forms a low cliff, and does not extend beyond 50 yards. The matrix is a coarse yellow brecciated tuff, in which trees of considerable length and girth are imbedded separately, and princi- pally on one horizon, only a few feet above the water. Smaller pieces of wood lie above. These trunks are partly in the condition of lignite, and partly imperfectly silicified, with their structure beautifully preserved. The deposit is much cut up by dykes. DiscussIon. Dr. Gwyn Jurrreys said his attention was called to the Icelandic beds with fossil shells by Prof. Steenstrup at Copenhagen in 1869, and further material had been collected by the late Dr. Morch, to whose memory as a conchologist the speaker offered his tribute of admiration. Jt was remarkable that among the shells there were very few Arctic species. It reminded him of the Moel-Tryfaen assemblage of shells, among which temperate forms occurred in great abundance. Prof. Jupp stated that the series of rhyolites brought from the north of Iceland by the author consisted of stony rhyolites, exhibiting banded spherulitic and perlitic structure, passing into pitchstone and obsidian. Some of the rocks are vesicular and even pumiceous, and they are associated with obsidian- aud pumice-tutts. Mr. Erueriper bore testimony to the great perseverance shown by the author in working out the Icelandic and Irish beds. He thought the collection of shells from Husavik was of the most interesting character. The AurHor said that many of the shells occur in beds of about a foot thick. The shelly beds are covered by great thicknesses of stratified but unfossiliferous ashes. 102 J T, MELLARD READE ON THE 14, The Drirr-peposits of Cocwrn Bay. By T. Mettarp Reaps, Hsq., C.E., F.G.8. (Read January 14, 1885.) In a former paper* I gave a short sketch of the drift disclosed in the ballast-pit at Colwyn-Bay station ;* and as in February of 1884. I had an opportunity of extending my observations over a larger area, I now propose to give an account of them. From Colwyn Head to Rhos Point is a distance of about three miles; and all along the shore, except where obscured by the Colwyn- Bay parade or grassed over by the railway company, are to be seen in cliffs excellent sections of the drift. This drift, extending backward to the foot of the hills which sweep in a curve from headland to headland, rests nearly wholly on the Silurian rocks, representatives of the Wenlock Shale. Colwyn Head or Penmaen Cliffs, and Rhos Point, are denuded remnants of the Carboniferous Limestone, and near to each of these headlauds the drift is seen to rest directly on the limestone, there being no exposure of the underlying Silurians anywhere to be seen in Colwyn Bay. Fig. 1.—Section just beyond the Cottage west of the Colwyn-Bay Hotel. 1. Grey Till, packed full of stones, partly Silurian Slate and Grits, and Carbo- niferous Limestone. ; 2. Cream-coloured Till. 3. Sand. 4. Brown Boulder-clay. 5. Soil. The surface of the drift is remarkably level, excepting where it gradually creeps up the hills. Most of the houses in Colwyn Bay are built upon it. It is crescent-shaped on plan, thinning out to- * Drift of N.W. of England and N. Wales, part ii. Quart. Journ. Geol. Soe. wol.xxxix.p- £1. “s <2 DRIFT-DEPOSITS OF COLWYN BAY. 103 wards the outward curve, which.rests on the hills, and thickening towards the Bay. Fig. 2.—Section West of fig. 1. Sees eA 3 ee ae Ses ee a ee 1. Bluish-grey Till; and, 2. Cream-coloured Till, as in fig. 1. 3. Sand. 4. Brown Boulder-clay. 5. Finely laminated Boulder-clay. 6. Brown Boulder-clay. 7. Soil. The drift may be roughly grouped into three divisions in ascend- ing order, as follows :— 1. Bluish-grey Tull (bed 1, figs. 1 & 2), hard and tough, evidently composed of the combined grindings or decomposed particles of the Silurian and limestone rocks, and full of striated slaty rocks, lime- stone, Carboniferous grits, conglomerates, and trappean and ash rocks common to North Wales. This Till is not visible between the Colwyn-Bay station and the road under the railway from Old Colwyn, but between the latter place and Colwyn Head may be seen a mixed grey and brown Till. It may be seen on the foreshore opposite the Colwyn-Bay Hotel, and from thence appears at various points, rising up in bosses in the cliff sections until we reach Rhos village. It may also be seen on the foreshore opposite the cottage west of the hotel (fig. 1). From Rhos point westward, to the embankment across the marsh, it may be traced. At one point here, I observed a very large lime- stone block imbedded in it. The Till continues from the west end of the embankment to the Little Orme’s Head. The surface of the Till, which everywhere, excepting on the fore- shore, is overlain by the Brown Boulder-clay, presently to be de- scribed, possesses an uneven denuded surface, and is in places covered with a cream-coloured deposit packed with stones, appa- rently the wash of the Till below, one or two feet thick, as the case may be (2, figs. 1 & 2). I looked for granite boulders in this Till; but though they were not unfrequent on the foreshore, I could not find any actually imbedded, but I had no opportunity of making an exhaustive 104 T. MECLARD READE ON THE examination. It may, at all events, be averred that they are not common in it*. At the cottage befure mentioned, between Colwyn-Bay hotel and Rhos, I noticed a large granite boulder on the shore, full of large crystals of felspar, which looked uncommonly like grey Shap granite. The crystals of felspar did not, however, form protuberant knobs, as is often the case with boulders of Shap granite. It is probable that it may he either Shap or Cairnsmore of Fleet granite 7. On the foreshore opposite the Colwyn-Bay hotel, the character of the stones contained in the Till may be readily studied. They are mostly slaty rocks, flattish in form, and often rounded at the edges. The Till being of a very tenacious nature, the stones remain firmly fixed in it, though their upper surfaces and sides are exposed by the denudation of the waves. The striations are distinctly to be seen on most of the stones, though doubtless partly effaced by the attri- tion of other boulders and shingle moved by the sea. It is really remarkable how they retain their ice-markings under the circumstances. I looked for signs of striated pavements, but could not find any: the boulders are fixed in the clay at different angles, and the stones do not show striations in a parallel and uni- form direction. 2. Low-level Boulder-clay and Sands (beds 3 & 4, fig. 1; & 3, 4, 5, & 6, fig. 2).—The Chester and Holyhead Railway runs along the top of the drift near to the edge of the cliff, so that in places the railway company have made what formerly was cliff into railway-bank, by sloping and grassing it over. For this reason it is difficult to see what the bank is composed of near Colwyn- Bay station, but it appears to me to be a continuation of the gravel, shingle, sand, and clay beds seen in the ballast-pit. If this be so, it gradually changes into the Low-level Boulder- clay and sands which overlie the Blue Till over the whole cf the area described in this paper. This Low-level Boulder-clay and sands is evidently a marine deposit, and contains shell fragments. There are very few boulders in it; but in places a great many beds of shingle and gravel, which are, however, best displayed in the inland excavations, and at the sides of the brooks which run from the hills through the drift and across the railway to the bay. The clay is brown and decidedly sandy, and the sand-beds, often displaying current bedding, are well developed, and form an im- portant feature in the drift. I believe most of the erratics on the shore come from this bed. Among the loose shingle on the shore are to be observed many Eskdale and grey Scotch granites, which no doubt have originally been derived from this group of beds. Inland Sections—Inland on the north side of the road, behind the Hydropathic Establishment, is a large brick-pit in this clay, and * Mr. Mackintosh says he “‘ dug out of the blue clay two pebbles of Eskdale granite.” “Age of Floating Ice in . North Wales,” see Geol. Mag. 3872, p. 16. t See “Notes on Rock-fragmenis from the South of Scotland,” Quart. Journ, Geol. Soc. vol. xl. pp. 270-272. DRIFT-DEPOSITS OF COLWYN BAY. 105 there are also others near the Board Schools on the road to Llan- drillo-yn-rhos. Nearer Colwyn-Bay Wesleyan Chapel, on the same road, is a sand-pit. I believe the beds of clay and sand are discon- tinuous, and occupy the surface without any particular order. 3. Rearranged Gravels.—A good deal of the drift. surface, especially about Colwyn-Bay village and in the neighbourhood of the several brooks before mentioned, shows evidence of having been subaerially redistributed. It is difficult to draw a fine line between these gravels and those undoubtedly belonging to the drift, especially as the surface-deposits had doubtless been previously rearranged or deposited during the emergence of the land from the great submer- sion. At the new station at Old Colwyn, which was being built during my examinations, the excavations showed a shaly gravel occupying the surface. Alluvium.—aA deposit of marsh clay is to be seen on either side of the embankment between Rhos and the Little Orme’s Head. It is only a few feet thick, and rests upon a few inches of peat, which again rests on the ‘ brown Boulder-clay.” The surface of the Low-level Boulder-clay is at its minimum elevation at these points. I was unable to measure the heights of the cliffs, but I should judge that the railway was at an average level of about 40 feet above the shore of Colwyn Bay. Towards Rhos the surface-level of the drift declines to near the shore-level. Beyond the embankment towards the Little Orme’s Head it rises again to a considerable height. Denudation.—The sea has evidently cut into and washed away a great deal of the drift, hence the formation of the cliffs. The “ Dingle ” at Colwyn Bay, and the valley or gully in which runs the brook from Old Colwyn, are very deep narrow cuts in the drift. I attribute their depth and comparative narrowness to the geolo- gical recency of the denudation of the coast, which has brought the ‘base level of erosion ” nearer to the hills, and so, by quickening the grade of the streams, has enabled them to do more work vertically than horizontally. ConcLusI0Nn. It now remains to consider what light the foregoing facts throw upon the difficult question of Glacial geology. In the first place I may observe that in few sections is to be seen so clear a line of demarcation between two beds of drift as exists here between the grey Till and the brown Boulder-clay. This arises from the fact that the clearly marine “ Low-level Boulder-clay,” and the typical “ Till” are in juxtaposition over a comparatively large area. “Till” is evidently a deposit the materials of which generally have not travelled so far as those of the Low-level Boulder-clay. It is here, as elsewhere, largely, if not altogether, made up from the local rocks, the slates, shales, and limestones, and it is no doubt the great quantity of carbonate of lime in it that makes it set so hard. At Penmaenmawr, to the west of Colwyn Bay, and out of the limestone district, I had an 106 T. MELLARD READE ON THE opportunity of examining in the foundations of the British Schools, of which I happened to be the architect, the Till lying on the hill- side. Here and all about Penmaenmawr, after getting below the surface-affected portion, it was a hard grey Till full of large boulders and stones which were generally more or less rounded and waterworn. I noticed one slightly striated. These stones were so large and firmly imbedded that they were used in some cases for the foundations, being built into the walls without removal. The Till at Colwyn Bay is bluer, more clayey, and of a finer texture, and contains not nearly so many large boulders, though the total bulk of the stones in it may not be very dissimilar. According to my experience, true Till is rarely, if ever, found except in the neighbourhood of mountains or quickly sloping ground. In the present instance, I am inclined to believe that it has been formed by ice and snow descending from the mountains and accumulating the disintegrated matter at the foot. It does not appear to be the ground-moraine of a hill-and-valley-ignoring ice-sheet, as the con- tained stones lack the definiteness of direction one would expect to result from such an agency. It is better to admit that we are largely ignorant of the various modes in which land-ice acts—its effects, with our limited knowledge, belonging more to speculation and theory than to fact. Be this as it may, when we come to the overlying deposit of brown Boulder- clay, no such difficulties occur. It is undoubtedly an aqueous-marine deposit, and part of the extensive sheet of Low- level Boulder-clay and sands which occupies all the plains of the North of England, from the margin of the mountains to the coasts of the Irish ‘Bea, and; skirting the coast of Wales, here and there intrudes upon the lower valleys. With the exception of the portion of this deposit which approaches the limestone headlands, where it is mixed with the detritus therefrom, the extensive sheet of drift, which I have described as lyimg in Colwyn Bay, is composed to a large extent of travelled materials. The sands and clays of which it is composed are not what the immediate coast or mountains could yield. It is, in fact, a deposit almost identical with the sandier of the Boulder-clays near Liverpool, which are composed principally of Triassic débris, mixed with travelled and striated rocks. I have pre- viously stated ‘‘ The sands and clays of Colwyn are evidently derived from the Triassic rocks of the Vale of Clwyd” *. This further and more careful examination over a large area has confirmed me in this opinion. Four and a half miles east of Old Colwyn, the Triassic sandstones set in and extend eastwards a distance of nine miles across the mouth of the Vale of Clwyd. Most probably these rocks also extend seawards. The materials of which the bulk of the Colwyn drift is composed, has in the first place probably been worn off the Triassic sandstone by subaerial agencies, including der that head ice and frost, and has worked gradually down the valley, it may be, to the plains now occupied by the Irish Sea. On * Quart. Journ. Geol. Soe. vol. xxxix. p. 118. DRIFT-DEPOSITS OF COLWYN BAY, 107 the gradual submergence of the land, this material lying in the Vale of Clwyd, reinforced by other material continually being worn off the rocks, and working seawards, has washed round the coast towards the Little Orme’s Head, and become mixed with other material washed up from the sea-bed and with argillaceous matter from the underlying Till. No’ice-sheet will account for this drift. It is evidently a marine drift. The Hskdale-granite boulders which it contains must have travelled to where they lie by floating ice; for many of the boulders k ve come from the north, while the sands have heen derived from the east. At all events, if this be not a true explanation, all the complicated machinery of at least two ice- sheets will have to be invoked. This appears to me to be un- necessary, especially as it would not explain the structure of the drift, which bears internal evidence of aqueous deposition. Discussron. Mr. W. W. Suyra remarked on the interest of this paper, as these beds of Colwyn Bay are evidently connected with the drift- deposits of the Vale of Clwyd, proved to be of great thickness in coal-borings at Rhy]. On the other hand, the classic deposits of Moel Trytaen might also be connected with the same deposits. Dr. Hiype pointed out that Till, undistinguishable from that in Wales, covers extensive areas in North America, far away from any mountains, and that consequently these are not essential to its formation. Mr. WuitaKker bore witness to the great care with which. Mr. Reade worked out his results by tracing the region from which the different stones came. He himself hardly understood the dif- ference between Till and Boulder-clay. Dr. Hicxs said that in the Vale of Clwyd we have three stages: —local deposits of gravel, marine sands, and widespread Boulder- clay. He thought that the Boulder-clay was formed by a mixture of local materials and ice-borne blocks. Mr. Toriry pointed out that the main interest attaching to the paper arose from the care with which the section had been recorded and the origin of the different materials traced. The succession of beds described was that generally to be seen in the North of Eng- land, where the drift-deposits are well developed. In Northumber- land and Durham the middle sands usually occur in greatest force near the old preglacial valleys. Prof. Jupp, in the absence of the author, further explained his views as to the distinction, character, and relations of the Till and Boulder-clay of the district. 108 G. R. VINE ON PHYLLOPORA AND THAMNISCUS FROM THE 15. Nores on Spxcres of Puytiopora and Tuamniscus from the Lower Stiurran Rocks near WutsurooL, WaLes. By Grorex Rosert Vine, Esq. Communicated by Prof. P. Martin Duncan, F.R.S., F.G.S. (Read December 17, 1884.) Mr. G. W. Shrubsole, in a paper “On the Occurrence of a new Species of Phyllopora in the Permian Limestone”*, remarks that “the genus Phyllopora has as yet been but imperfectly worked; its rarity in the more recent and its imperfect preservation in the older rocks go far to account for this..... In the Lower Silurian rocks Phyllopora is most abundant. There are at least two distinct species, if not more. The preservation of the remains in these beds is most unfavourable for exact work, occurring, as they often do, in coarse: ash or shale, and distorted by cleavage.” In the collection of the School of Mines there were ft several specimens of Phyllopora catalogued and labelled as such, which I was allowed to examine when collecting material for my Second British Association Report on Fossil Polyzoa. The specimens from the Lower Llandeilo rocks are the common forms, generally designated Retepora by early authors. One specimen is in the Wyatt-Edgell collection, and we have only the reverse aspect of the form ; but in places where the branches are worn the cells can be seen, not sufficiently, however, to enable us to make out their cha- racter. The fenestre are oval or irregular, branches anastomosing, consequently without dissepiments. In the Caradoc series of fossils of the same collection, several specimens are labelled, and also catalogued, as Phyllopora Hisingeri, M‘Coy, and one, belonging to the Wyatt-Edgell collection, is cata- logued as P. ornata, MS. Generally speaking, all these forms are very indistinct or ill-preserved. In a box with one specimen (-4, Case V) labelled Phyllopora? Hisingeri, M‘Coy, a small portion of the zoarium of fetepora cellulosa, Linné, is placed for the purpose of comparison. The Lower Silurian fossil is from Robeston Wathen, Pembrokeshire. I have several specimens of P. Hisingert, M‘Coy, in my cabinet; for it is the most common of all the forms found in the Caradoc or Bala beds ; butit is only by careful manipulation, and adjustment of light, that the cell-structures of these species can be made out; and even then not much dependence can be placed on the diagnosis. In the Lower Llandovery beds one specimen is marked and catalogued (op. cit. p. 64) as Phyllopora, sp. Besides these I have no other knowledge of species of the genus found in the Lower Silurian rocks in Britain sufficiently characteristic to be individualized. In the beginning of August, 1884, Mr. J. B. Morgan, of Welshpool, * Quart. J ourn. Geol. Soe. vol. xxviii. pp. 347, 348. t+ In 1881. See Catalogue of Mus. Pract. Geol., Cambrian and Silurian fossils, 1878. LOWER SILURIAN ROCKS NEAR WELSHPOOL, WALES. 109 sent some fossils to Professor Lapworth for identification. Amongst them were some Polyzoa. These Professor Lapworth asked Mr. Morgan to send to me, and their study has enabled me to throw a little light on essentially characteristic features of at least one Lower Silurian species of Phyllopora. This is clearly not the P. Hisingeri of authors, and I shall be compelled, much against my wish, to characterize it as new. Fig. 1.—Portions of Phyllopora tumida, sp. n. (Enlarged 6 diameters.) ie f * nN YANG A. Poriferous surface. B. Interior of non-ceiluliferous face. ]. Puytnopora TuMIDA, sp.n. Fig. 1. Zoarium an open net-work of undulating branches; base and general dimensions of zoarium unknown, branches anastomosing, apparently thick, occasionally tumid, and varying in breadth from one tenth to one twelfth of an inch. Senestrules oval or irregular, sometimes less, but occasionally rather longer than the breadth of the branches. Zoccia tubular, short or stunted, cell-mouths circular, prominent, with a rather thick peristome, from four to five arranged diagonally in the branch. Reverse, on account of the peculiarity of its preservation, indistinct. Horizon and Locality. Caradoc beds ; Wern-y-seadog, Llanfyllin. Cabinet. J. B. Morgan, Esyg., Welshpool; 2 specimens. I have been fairly successful in drawing a portion of two branches, on which the cell-characters are pretty distinct. The specimen from which the drawing is made is rather more than half an inch square ; it contains about twenty-three perfect and imperfect fenestrules, and nearly the whole of the branches are more or less covered with cell-apertures (fig. 1,4). In places where the cells are worn the tubular prolongations are seen, and, judging from the peculiarities of the form, I should not imagine that the branches are Q7d.G.S8. No. 162. K 110 G. R. VINE ON PHYLLOPORA AND THAMNISCUS FROM THE thick. In places where the whole of the cells are worn off, their former localization is indicated by wavy outlines, as shown in fig. 1,8; but I cannot trace any other special character of the reverse than this. With the exception of the prominent lips of the cells of the species, nearly the whole of the original organic matter of both specimens is replaced by iron oxide; consequently the once living form now appears upon the shale as a dark brown friable mass. Because of this, | am unable to fill in all the details that are necessary for the full study of Lower Silurian species. It is to be hoped, however, that the publication of these brief notes may be the means of bringing to the front other fossils with the poriferous face exposed, rare though they may be. Prof. H. A. Nicholson has described one species of Phyllopora from the Trenton Limestone, Peterborough, Ontario*, and as the Trenton Limestone is of, or about, the same age as our Caradoc beds, the species is interesting for the sake of comparison. The Ontario form is named Retepora trentonensis, Nich., and the fossil was only known to the author “by several more or less imperfect specimens, from which some of the essential characters cannot be determined.” There is no possibility of uniting the two forms under one specific name, because, even from the characters which Prof. Nicholson was able to draw up from the best of his specimens, there are many differences between them, as a comparison of the two descriptions wil show. ‘The Ontario specimens are better preserved than ours, and we learn from the description that the “ reverse aspect is strongly striated with wavy or straight longitudinal striz.” In the Caradoc species I cannot trace any other character of the reverse aspect than that already given. Mr. E. O. Ulrich describes 7 and figures one species of Phyllopora in his series of papers on “ American Paleozoic Bryozoa.” This he names P. variolata, Ulr., but he says “the genus is represented by two species in the Cincinnati rocks, P. variolata and another which I believe is the same form that was described by Miller and Dyert under the name of Intricaria clathrata.” The species found in our British rocks is related to, but not identical with, Mr. Ulrich’s. In his species the “ cell-apertures are arranged either in two series or three alternating rows; intercellular spaces thin, raised into small nodes where longer; about fourteen cell-apertures occupy the space of ‘l inch. Branches on non-celluliferous side smooth.” Locality. Cincinnati, Ohio, in strata from 150 to 325 feet above low-water mark, in the Ohio river. There is another fossil in Mr. Morgan’s collection that merits distinction and description, not more on account of its peculiarly antique character than on account of its mode of preservation in the volcanic ash in which it is imbedded. * New Paleozoic Polyzoa, Geol. Mag. Dec..2, vol. ii. p. 2, f. 4, 4 8. +t Journal Cincin. Soc. Nat. Hist. Oct. 1882, p. 160, pl. vi. f. 14. ¢ Contributions to Paleontology, no. 2, 1878. LOWER SILURIAN ROCKS NEAR WELSHPOOL, WALES. 111 Fig. 2.—Thamniscus antiquus, sp. n. oO A. The specimen, enlarged 2 diameters, B, C, D. Details more highly magnified. 2. THAMNISCUS ANTIQUUS, sp. n. Fig. 2. Zoartum apparently springing from a root-like base, strong and thick towards the bottom, where several root-branches appear to be united, more delicate towards the younger or growing portion of the zoarium. Branches frequently dichotomising, free. Zoecia tubular, shown on one side only of the branch. Tubular cells not contiguous, rather broad at the openings, gradually thinning out towards the axial region of the zoartwm: cell-mouths, so far as I can make out, rather elongated, peristomes not prominent, reverse striated ? Formation. Imbedded in volcanic ash, probably of the age of the Bala rocks. Locality. Middleton Hill, near Welshpool. Cabinet. J. B. Morgan, Esq., Welshpool; one specimen. This beautiful specimen, which I have drawn magnified about four diameters, is buried in volcanic ash, which is so friable that it breaks away with the least touch. It is very certain that it is the reverse surface that is exposed; but towards the bottom the thick- ened branch is broken away, and the cells are exposed. The appearance of the branch at this part is shown in fig. 2, B; but when more highly magnified the arrangement of the cells is seen to be pretty regular, and is shown in fig.2,c. By extracting a minute fragment of the specimen from the matrix, I have been able to expose the poriferous surface, and this is shown in fig. 2, D. So far as I am able to judge by carefully manipulating this delicate fossil, I can almost confidently assert that the species now described differs considerably from the species previously described by myself * * Quart. Journ. Geol. Soc. vol. xxxviii. p. 60. K2 112. @. B. VINE ON PHYLLOPORA AND THAMNISCUS FROM THE and by Mr. Shrubsole * as Thamniscus crassus, from the Wenlock Shales and Dudley Limestone. Referring again to Prof. Nicholson’s paper on “ New Palzozoic Polyzoa” (op. eit.), I wish to draw attention to two of his figures, because these have some resemblance to the present species. of figs. 3 and 3 ain pl. ii. the author says (explanation of pl. op. cit. p. 5), ** Fig. 3.—Fenestella Davidsont, a small portion of the non-poriferous side of the natural size. Fig. 3 a.—Portion of the same enlarged.” Both these figures appear to me to be portions of a free-branching Thamniscus. There are no fenestrules or dissepiments. Figs. 36 and 3 ¢ of the same plate, ‘‘ portions of the poriferous side of another specimen” (Nich.), belong, so far as 1 can judge from the figures, to a different species,apparently a true Fenestella. I know Prof. Nicholson will receive my remarks in the spirit in which they are offered ; my only desire in criticizing his labours is to bring out all the information that is possible in describing forms still older than, but apparently generically related to, the Hamilton species described as Henestella Davidsone by Nicholson, Range of Lower-Silurian Phyllopore. . Phyllopora. Lower Llandeilo. Cat. p. 207. —— Hisingeri, M*Coy. Caradoc. Cat. p. 44. From several localities. ornata, MS. (Wyatt-Edgell). Caradoc. Cat. p. 44. tumida, Vine. Caradoc (fig. 1, above). variolata, Ulrich. Cincinnati Group. clathrata, Miller and Dyer. Cincinnati Group. trentonensis, Nicholson. Trenton, L. Ontario. sp., Lower Llandovery. Cat. p. 64. sit give the whole of the forms known to me; but I would advise the examination especially of those numbered 1, 3, and 8, in the above list. The Upper Silurian Phyllopore merit full description and illustration ; but unhappily the really good specimens are not in my keeping, although ample material is in existence in the cabinets of others for the purpose suggested. M2) al Lower and Upper Silurian THAMNISCID&. . Thamniscus antiquus, Vine. Agé?, Bala beds (fig. 2, above). crassus, Lonsdale. Wenlock Shale, Dudley Limestone. variolata, Hall. Lower Helderberg?. nysa, Hall. Lower Helderberg. nysa, variety, Hall. Lower Helderberg. fruticella, Hall. Lower Helderberg. ? cissets, Hall. Lower Helderberg. TT OU co tS HLT | * Quart. Journ. Geol. Soc. vol. xxxviii. p. 344. + Mus. Pract. Geol. Catalogue. Silurian fossils, 1878. t Corals and Bryozoans of the Lower-Helderberg group, by James Hall. Albany, 1880, pp. 3/ & 38. LOWER SILURIAN ROCKS NEAR WELSHPOOL, WALES. 113 Note on Licnenovora pavcrvora, Vine. (Quart. Journ. Geol. Soc. vol. xl. p. 853.) Immediately after the publication of my ‘‘ Notes on Cretaceous Lichenoporide,” Mr. Thomas Jesson, F'.G.S., of Pulborough, wrote me respecting L. paucipora, Vine. Mr. Jesson says that it was he who forwarded to Prot. Duncan the specimens described, and that the fossils were found in washings from the coprolite-bed near Cambridge. In all probability Prof. Duncan had mislaid Mr. Jesson’s letter sent in with the fossils, and I am glad to be able to add the locality to the description of the species. Discussion. Dr. Hiypr remarked that it was impossible to discuss the con- tents of such a paper as this without having either specimens or good figures to refer to, and he protested against descriptive pale- ontological papers being read before the Society without such adjuncts. The CHarrman (Mr. Carruthers) agreed with Dr. Hinde that it was very desirable that specimens should be exhibited if possible, but at the same time it seemed to him that the present paper had been carefully drawn up and would prove useful. 114 A. J. JUKES-BROWNE ON THE 16. The Bovrper-Crays of Lrxcotnsnire. Their GEoGRAPHICAL Ranee and Retative Acre. By A. J. Juxus-Brownz, Esq., B.A., F.G.8. (Read January 28, 1885.) (Communicated by permission of the Director-General of the Geological Survey.) Introduction. Wuen I commenced the survey of East Lincolnshire, in 1877, the only connected account of the Boulder-elay was to be found in the well-known paper by Messrs Wood and Rome *; and up to 1879, when I wrote a paper “On the Southerly Extension of the Hessle Boulder-clay in Lincolnshire” 7, I saw no reason for doubting the propriety of their classification. The mapping of these clays by myself and colleagues during the subsequent progress of the Survey has, however, brought to light many facts which were unknown to Mr. Searles Wood, and has led us to question the accuracy of his interpretation of those facts which were known to him. The classification of glacial deposits is always a difficult matter, and in Lincolnshire there are special circumstances which make it very difficult to ascertain the relative age of the several masses of Boulder-clay. Mr. Searles Wood himself, though still adhering to the divisions which he first established, has considerably modified his views with regard to the correlation of the Lincolnshire Boulder-clays. His original classification of the glacial series in East Yorkshire and Lincolnshire, as published in 1868 t, was as follows: — 5. Hessle clay. 4. Hessle sand and gravel. 3. Purple clay. 2. Sands and gravels. 1, Basement clay. He then regarded the Basement clay as the equivalent of the East Anglian Upper Boulder-clay, and considered the overlying Purple and Hessle Clays as newer than any part of this. southern Chalky Boulder-clay. In his last paper (1880) he takes a different view, and appears to look upon the Basement and Purple Clays as together representing the whole East Anglian series $. In both memoirs he insists upon the existence of a great break at the base of the Hessle beds, and even goes so far as to exclude these beds from the glacial series altogether, grouping them as Post- glacial, because they are bedded into the Wold valleys and because at one locality they happen to contain the shell Cyrena fluminalis. * Quart. Journ. Geol. Soc. vol. xxiy. p. 146. t Op. cit. vol. xxxv. p. 397. t Loe. cit. § Quart. Journ. Geol. Soe. vol. xxxvi. p. 527. 115 BOULDER-CLAYS OF LINCOLNSHIRE, (Scale IW Hessle Clay. = Chalky Clay. clays: reduced from the maps of the Geological Survey. miles to an inch.) Fig. 1.—Sketch-Map of Lincolnshire, showing the range of the Boulder- about 12 116 A. J. JUKES-BROWNE ON THE I propose, therefore, to set down some of the evidence which I have obtained during the last six years, in order that the present state of the case may be properly apprehended, and that the links which are wanting in the chain of evidence, and the difficulties which call for explanation, may be clearly perceived. No one who studies the Lincolnshire Boulder-clays can fail to be struck with the great differences between the two principal types of glacial clay which occur in the county; they fall naturally into two groups—a brown series and a grey or blue series, which are not only lithologically different, but also to a great extent geographically separate. It will perhaps clear the ground if I commence by briefly sketching the range of these two types of Boulder-clay, leaving their points of contact to be considered afterwards. The relations of the two members of the “‘ brown series,” namely the Purple and Hessle Clays, will next be discussed ; and in conclusion such inferences will be drawn as appear to be warranted by the facts described *. § 1. The Range or superficial Extension of the Chalky Boulder-clay. This type of Boulder-clay only occurs in the southern, central, and western parts of the county. In the south-west, about Corby and Ponton, it is generally of a light grey or greyish-blue colour, full of chalk and oolitic débris; beneath the Fens and northward along the central valley it is usually of a deep blue or blue-grey; but eastward as it nears the Chalk Wolds it becomes lighter and lighter, finally passing into an intensely chalky clay or marl of a pure white or yellowish-white tint. . There can, I think, be little doubt that these grey-blue and white Boulder-clays form part of the great sheet which spreads over the eastern Midlands, and which appears to be continuous with what has been termed by Mr. Searles Wood the Chalky Boulder-clay or Upper Boulder-clay of Kast Anglia. The mapping of sheets 70 and 837 has disclosed certain peculi- arities in the lie of this Boulder-clay which deserve attention. In sheet 64 (south of sheet 70) spreads of Boulder-clay occur both on the lowest and on the highest levels ; and some of these entering sheet 70 extend northward along the high ground by Great Ponton and Somerby to Kelby, a village about two miles 8.E. of Ancaster. But from Ancaster and Sleaford northward to Lincoln no trace of this clay has been found along any part of the tract occupied by the outcrops of the Jurassic strata. Again from Lincoln northward no Boulder-clay is found along the higher ground, though it is * For a full description of the Lincolnshire Boulder-clays and of the sections observed during the progress of the Geological Survey the reader is referred to the explanations of sheets 70, 83, 84, 85, and 86, which are now in course of publication. In the following pages only a few sections are described as specially illustrating the relations of the several clays, and the paper is designed to convey such theoretical conclusions as do not find a place in the Survey Memoirs. These conclusions are not, however, to be taken as expressing the general opinion of the officers of the Survey, but are my own personal views. +t These numbers refer to the sheets of the Ordnance Survey map, and their limits are shown on the map accompanying this paper. BOULDER-CLAYS OF LINCOLNSHIRE. EV? continuous on the eastern flank and soon begins to set in on the western flank. The great sheet which slopes northward through Cambridgeshire and caps the islands of Ely and March dips beneath the Fen-level along a line running south of Crowland and Wisbech and continues to underlie the plain of the Fenland by Spalding, Donington, and Boston. It may have been, and probably was, connected with that which spreads over the high land in the south part of sheet 70, but it is now disconnected by erosion along the Fen border. Unlhke the high-level mass, it does not terminate in the latitude of Ancaster, but appears to run northward below the Fens bordering the Witham, emerging along their eastern border by Tattershall, Kirkstead, and Bardney. Thence this Chalky Boulder- clay spreads northward through Wragby and Market Rasen to Brigg, and eastward to Horncastle and the high ground between the valleys of the Bain and the Steeping in sheet 84. It also sends a tongue-lke prolongation north-eastwards, from Hainton and South Willingham, across the escarpments of the Lower Neocomian and the Chalk, by Gayton-le-Wold and Brough-on-Bain, up on to the summit of the Chalk Wolds near Kelstern and Elkington to the north-west of Louth. Near Gayton the Boulder-clay and associated gravels are seen to be bedded against the slope of the Chalk escarpment, showing that this escarpment had retired to its present position in pre-glacial times. The height of the ground near Kelstern is about 400 feet above datum-level. Another important point in connection with the distribution of this Boulder-clay is this, that with the exception of the tongue above mentioned and a small outlying patch to the southward, it is not found anywhere along the broad tract of the Chalk Wolds from their commencement near Candlesby to their intersection by the Humber. This is the more remarkable because this clay caps the high ground formed by the Lower Neocomian escarpment near Greetham, Fulletby, and Scamblesby, which is as high as,if not higher than, the corresponding part of the Chalk escarpment. Still the occurrence of the single outlier near Maidenwell, and the fact of its climbing on to the Wolds by Kelstern, seem to indicate that the Boulder-clay once had a continuous extension over these hills. We are consequently obliged to conclude either that the Wold hills have been in some way exposed to more severe and long-continued detrition than the rest of the county, including the Neocomian ridge, or else that the amount of Boulder-clay originally deposited on the Chalk hills was very much less than elsewhere. It is very probable that its thickness was less on these hills, and I have shown in pre- vious papers that erosive agencies have been very active over this tract. § 2. The Range of Brown Boulder-Clays. The Eastern Border.—In describing these clays and their mode of occurrence it will be convenient to commence on the north border of the Fenland, near Firsby, a station on the Great Northern line; 118 A. J. JUKES-BROWNE ON THE and for details of the sections visible in this neighbourhood, I may refer to my paper “On the Southerly Extension of the Hessle Boulder-Clay in Lincolnshire ”*. The map accompanying that paper also shows the manner in which this clay, together with the under- lying Purple Clay, stretches northward, and forms a broad tract of undulating land between the Chalk Wolds and the eastern marshes. That map, however, having been drawn before the boundaries of the Boulder-clay had been accurately mapped north of Alford, it is necessary to give some account of its inland boundary from this point, and the map (p. 115) will enable the reader to follow the ensuing description. This boundary, to the west of Alford, is almost a straight line; the clay ends abruptly against the rise of the Chalk Wolds, and the depth of the clay increases with the rise of the ground from Alford towards the hills. Thus near Alford the usual depth of the Boulder- clay is about sixty feet, but near Rigsby a well was sunk within a furlong of the boundary-line, and passed through ninety feet of clay without piercing it. These facts show that the plain of Chalk on which the Boulder-clay rests is nearly horizontal, and extends up to the foot of the Wolds. They also seem to indicate that the clays are banked up against a buried cliff of chalk. This sharp boundary- line continues north-westward for about two miles, till it is broken by the outlet of the Caleeby beck between Aby and Belleau. Here there is an extensive bed of gravel, intercalated apparently between an Upper and Lower Boulder-clay, and evidently a beach-formation, containing broken marine shells in the sandy beds, and rolled pebbles of chalk, pierced by, Pholades,in the gravel beds. At South Thoresby there are two beds of gravel, separated by a layer of clay, about 20 feet thick, and the same is the case at Claythorpe station. At and beyond Belleau the Boulder-clay overrides the cliff or slope of the Chalk, and for some distance caps the ridge which runs through Burwell Park. From this place to the neighbourhood of Louth, the boundary is very irregular, outliers of Boulder-clay occurring on the highest hills, and tongues of the same clay occupying the bottoms of the valleys which ramify through the Wolds. The height to which the Boulder-clay here ascends must be nearly 300 feet; but in colour and general appearance it is precisely the same as that found near the surface of the lower ground. North of Louth, for a short distance, the border of the Chalk Wolds is similarly smothered in Boulder-clay ; but near Fotherby the boundary descends to a lower level and becomes again sharp and clear. Striking N.N.W., and only interrupted by tongues thrust up the older valleys, it passes into sheet 86, between Wyham and Hawerby. At the latter place the boundary-line appears to pass between the church and ‘the Hall” occupied by Mr. Harness; this gentleman in- formed me that a well had been sunk in his yard to a depth of 156 feet without meeting anything else than clay. As chalk comes to the surface at a distance of about 150 yards, there is a very steep slope * Quart. Journ. Geol. Soc. vol. xxxy. p. 397. BOULDER-CLAYS OF LINCOLNSHIRE. 119 (if not a cliff) of chalk at this place, and probably all along the line of rise from the lower plain to the Wold hills. At the same time it is clear that the Boulder-clay overrode this cliff-line, and buried a considerable portion of the Wold land to the westward. A thin outlier caps the high ridge between Hawerby and Wold Newton, the summit of which is 382 feet above datum-level; and the same Boulder-clay occupies the valley-bottom which runs northward from Wold Newton to Rayendale. Fig. 2.—Plan of the country near Hatcliffe. (Scale 1 inch to a mile. The ground occupied by Drift is indicated by diagonal shading.) ~ ANS i = N QQ ios. wyy, SSSSINN e\ve an Ne = S xa CAS pa A Go <<) Ey | =| divs BH isa) & SS * S{= : Is BR PAs sé NK \K KC S) N LS Y E YG, S NG 2) YA lily Nii SE Z Se OTT = iu, “My Yyjs Tt Lig) er TL. WD N i} Q, y / 2 [FE Ne TINCT H SS (Mechanismus der Gebirgsbildung, Band il. p. 55) calls attention to the fact that in a cleaved crystalline limestone belonging to the Hochgebirgskalk, the individual calcite grains are of unequal dimensions in the different directions, and have tlieir longest diameters lying parallel to each other in the plave of cleavage, although in the uncleaved rock the crystalline grains are of nearly equal dimensions in the different directions. He suggests that this is due to the plastic deformation of the individual grains of calcite. Lehmann (Die Entstehuzg der altkrystallinischen Schiefergesteine, p. 197) objects to this view, and calls attention to the evidences of fracture and crush occurring in the rocks investigated by him. The fact established by Heim requires an expla- nation, however, and the most obvious one is the assumption that a molecular rearrangement occurs in the calcite under the mechanical conditions which determine the cleavage. The following important questions remain to be solved :— Under what conditions is the deformation of rocks accompanied by a crushing of the individual constituents? Under what conditions is it accompanied by entire molecular rearrangement? And lastly, Under what conditions do these two more or less opposite phases of metamorphism occur at one and the same time? In the north-west of Scotland there are schists that have been formed by: DOLERITE INTO HORNBLENDE-SCHIST. 141 the intervening material lost; but the two portions are represented in their natural position, and the zone of transition is fortunately preserved in the upper one. A large section prepared through the zone of transition shows in a very perfect manner its gradual character. In what way was the foliation produced? The only answer that seems possible is, that it was caused by movement when the mass was in a plastic state; but plasticity may arise in two ways. Under moderate pressures it can only occur when the material is in the fluid condition, that is, when the cohesion is slight; but under very high pressures it may be produced in bodies which are solid under ordinary circumstances *. This notion of the plasticity of solids is, of course, one of immense significances in relation to rock- deformation, and is doubtless destined to play a most important part in all questions relating to the origin of the crystalline schists. The phenomena of the Scourie dykes appear to me to show that the plasticity which has led to the development of foliation, is that due to high pressure at ordinary temperatures, rather than to high tem- peratures at ordinary pressures. The optical anomalies due to strain, the bending of the twin lamelle, and the actual fracture of the felspar crystals of the dolerite, are best explained on the assumption that the rock has been affected by pressure after consolidation, and the same assump- tion explains the curved and confused arrangement of the joint- planes which is occasionally observed. Then the fact that the planes of foliation frequently cut across the dyke and run parallel with the prevalent strike of the gneissic banding, is difficult to account for on the view that the foliation was produced by movement during the final stages of consolidation, though easy to explain on the alternative hypothesis. The curious interfelting of gneiss and dyke at the junctions in certain places also appears to indicate movement posterior to consolidationy. Mechanical deformation accompanied by molecular rearrangements has profoundly affected the gneiss itself; and I have little doubt that some of this has taken place since the intrusion of the dyke. mechanical action alone, others that have been formed by mechanical action supplemented by a certain amount of molecular rearrangement, andothers, again, like the hornblende-schist of the Scourie dyke, in which a complete, or nearly complete, molecular rearrangement has taken place. The data for the solution of the above problems are therefore in all probability to be found in this region. * Tresca, ‘ Flow of Solids,” Proc. Inst. Mech. Eng. 1878, p. 301. 1 It is interesting to note that if this process of interfelting were carried on to a much greater extent, it would lead to the disappearance of the dyke as such. The only evidence that would then remain to attest the former existence of the dyke would be the presence of bands of hornblende-schist in the gneiss. We know nothing as to the age of the dyke except that it is later than the so-called _Archean gneiss. It is somewhat interesting to contemplate the possibility of a later dyke of unknown age becoming part and parcel of Archzan gneiss ; and the reflection may serve to suggest that our gneisses and schists may be of very complex origin, and may contain, as Prof. Lapworth holds, elements derived from formations of very different geological age. Q.J.G.8. No. 162. M 142 J. J. H. TEALL ON THE METAMORPHOSIS OF One fold occurring not far from the dyke is figured below (fig. 2). The parts marked with crosses are lumps of hornblende-rock. Fig. 2.—Fold in Hebridean Gneiss, 3 or 4 feet across. Another argument tending to show that the foliation has been developed by mechanical action subsequent to consolidation may be founded on the fact that the parallel structure does not occur in the rock in which the original augite and felspar may be recognized. The hornblende occurs alone in the foliated portion. The relations of augite to hornblende are of great interest in connexion with the origin of the crystalline schists, and they have recently been discussed by the American lithologists, Prof. R. D. Irving * and Mr. G. H. Williams +, at considerable length. Mr. Williams points out that augite appears to be the stable form at high temperatures, hornblende at low temperatures, so that any condition tending to facilitate molecular readjustment at ordinary temperatures must necessarily tend to facilitate the change from augite to hornblende. The enormous pressures brought into operation in the process of mountain-making may, as Mr. Williams states, not unreasonably be supposed to supply such conditions. The relation of crystals to their environment is one which lithologists have most carefully to consider. A crystal is doubtless in stable equilibrium, so far as the molecular forces are concerned, when subject to the conditions under which it is formed. Under other conditions it may be in unstable equilibrium, and ready therefore to undergo molecular readjustment the moment such readjustment becomes possible. We conclude, then, (1) that the hornblende-schist of the Scourie dykes has been developed from a dolerite by causes operating after the consolidation of the dolerite, and that the metamorphosis has been accompanied by a molecular rearrangement of the augite and felspar; and (2) that the molecular rearrangement has, in certain cases, taken place without the development of foliation. * Amer. Journ. Sci. ser. 3, vol. xxvi. p. 27 (1883); ibid. vol. xxvii. p. 180 (1884). t+ Amer. Journ. Sci. ser. 3, vol. xxviii. p. 259 (1884). DOLERITE INTO HORNBLENDE-SCHIST, 143 To give anything like a critical account of the previous work bearing on the subject would increase the length of this paper to an extent that seems scarcely desirable. I may mention, however, a few facts which show that the point here advanced is by no means new. Dr. Geikie, in his review of Dr. Lehmann’s work, in ‘ Nature,’ mentions that Prof. Jukes long ago suggested that many areas of hornblende-rocks may be due to the metamorphosis of basic lavas and tuffs. Mr. Darwin in his ‘ Geological Observations,’ 2nd edit. p- 482, calls attention to the gradual passage from hornblende-slate to greenstone; but he regards the latter rock as representing the extreme of metamorphism. Mr. Allport, in his valuable paper ‘“‘ On the Metamorphic Rocks surrounding the Land’s-End mass of Granite”’ (Q. J. G. 8. vol. xxxii. p. 422), refers to certaim greenstones which ‘‘ might almost be described as hornblende-schists,” and in his summary expresses the opinion that ‘“ hornblende-schists may be metamorphosed igneous rocks, some being derived from dolerites or gabbros, while others are very probably foliated diorites.” ‘‘Schistose greenstones” are described by Mr. J. A. Phillips in his two papers “ On the so-called Greenstones of Cornwall” (Q.J.G.S. vol. xxxii. p. 155 and vol. xxxiv. p. 471). Prof. Bonney, in a paper on ‘The Hornblendic and other Schists of the Lizard District” (Q.J.G.8. vol. xxxix. p. 14), refers to the transition from hornblende- schists to a rock resembling diorite. Dr. Lehmann, in his work ‘ Die Entstehung der altkrystallinischen Schiefergesteine,’ describes the passage of gabbro into schistose amphibolite. M. Renard, M. von Lasaulx, and others hold that the amphibolite schists of the Ardennes have been produced by the mechanical metamorphosis of diorite. Adolf Schenck describes schistose diabase in a paper on ‘* Die Diabase des oberen Ruhrthals,” Inaugural Dissertation, Bonn, 1884. This account of previous works bearing on the subject is very incomplete, but it is sufficient to show that the conclusions suggested by an examination of the Scourie dykes have been more or less anticipated by many previous writers. In concluding this paper, I should like to take the opportunity of acknowledging my indebtedness to Prof. Lapworth. In the summer of 1883 he very kindly conducted Prof. Blake and myself over the Erribol area, and explained to us the very complicated stratigraphy of that interesting region. He called our attention to the secondary structures developed in the rocks by mechanical action, and instructed us where to collect specimens that would best serve for the purpose of microscopic examination. At the time we were on the ground I could not follow him at all points, because the subject was new to me as regards both the stratigraphy and the petro- graphy. Indeed it was not until I had examined the rocks collected under his supervision, as well as others obtained by myself in other regions of the north-west of Scotland, by the aid of the microscope, and had read the work of Dr. Lehmann, published shortly after, that I fully realized the significance of many points that Prof. Lapworth had insisted upon. Although Prof. Lapworth has not seen the M2 144 J. J. H. TEALL ON THE METAMORPHOSIS OF Scourie dykes, I feel that it would not be right to allow this paper to pass without pointing out that the ideas expressed in it have been to a very great extent suggested by the lessons he taught me in the Durness-Erribol area during the summer of 1883. EXPLANATION OF PLATE II. Fig. 1. Dolerite (diabase) section showing lath-shaped felspars, crystalline plates of augite, titaniferous magnetic iron-ore, secondary hornblende, and green decomposition-products. Magnified 24 diameters. 2. Hornblende-schist viewed with polarizer only. Plane of vibration at right angles to schistosity. Hornblende, colourless crystalline grains (quartz and modified felspar), and titaniferous iron-ore partially surrounded with sphene. On rotating stage through 90°, ali the yellowish-green grains change simultaneously to deep green. Magni- fied 50 diameters. The hornblende is more abundant in the portion of schist here represented than is usually the case. Discussion. The Present pointed out that while others had suggested the relations in certain cases between igneous and metamorphic rocks, to the author belonged the merit of having demonstrated this in a particular instance. He agreed with him that the schistosity of the rock of the dyke could not have been produced during the cooling of the mass. He had always thought that some of the hornblende-schist of the Lizard might similarly have been derived from basic igneous masses; but when working there he had failed to obtain any proof of it. Mr. Bavrerman remarked on dykes in the older Archean rocks of South America, which sometimes run along planes of foliation and at others cut across them. He thought that in such cases the dykes were probably not very different in age from the gneiss which they traverse. Prof. SrELry said that the interest of Mr. Teall’s work was in the direct conversion of a volcanic texture into a schistose texture ; but though the fact was new, it did not need any new views in metamorphism to explain it. We could only conceive of the change taking place after the dyke had cooled and cracked, because the rock could not otherwise have offered the resistance under which the crystals would extend themselves at right angles to pressure in the foliated part. He thought that the change had been an ex- tremely slow one, due to the temperature of the water in the cracked rock being raised by pressure, so that it had slowly dis- solved the material of the dyke, which had as slowly recrystallized in a schistose form. Mr. Teall’s account was conclusive; but such origins for hornblende-schist are necessarily local. Dr. Hicxs thought that the case cited in this paper, where one crystalline rock was changed into another and into closely allied minerals, probably by infiltration along minute fissures, lent no DOLERITE INTO HORNBLENDE-SCHIST. 145 support to the extreme views held by some concerning the meta- morphism of sedimentary rocks. Prof. Buake asked how it was that one part of the dyke was changed while the other part was not. He objected to the view that because the change might take place in a range of a few inches, therefore great masses of rock could be changed in the same way. Mr. Hupteston remarked on the difference between the horn- blende-schist of the dyke, consisting largely of hornblende and an altered felspar, and the common hornblende-schist, which consists chiefly of hornblende and quartz. Mr. Kiteour called attention to the fact that by pressure a similar fibrous structure is produced in cast-iron. The Avrnor, in reply, pointed out that while the gneiss of the country showed signs of great disturbance, the dyke maintained its direction with a considerable amount of regularity. It seemed evident then that the disturbances to which the gneiss had been subjected must in the main have been produced before the intrusion of the dyke. He had not argued that all hornblende-schists were metamorphosed dolerites, but only that a particular hornblende-schist been produced in this way. Why movement and metamorphism had occurred at certain points and not at others he could not explain. The typical schist of the dyke was composed almost entirely of hornblende and a mineral or minerals occurring as colourless crys- talline grains. Turbid felspar was rare, and, in the most perfect schist, almost if not entirely absent. The colourless grains he originally regarded as quartz, but he now felt considerable doubt as to their precise character. In every respect, so far as his expe- rience enabled him to judge, the schist appeared to resemble the typical hornblende-schists of the so-called Archean rocks. i if 146 C. L: MORGAN ON THE S.W. EXTENSION 18. On the S.W. Extension of the Cuirton Favir. By Pror.C. Lioyp Morean, F.G.S., Assoc. R.S.M. (Read December 17, 1884.) On the right bank of the Avon, somewhat below the Suspension Bridge and a little beyond the Clifton station of the Bristol Port railway, the Clifton fault cuts across the strata somewhat obliquely. On the southern side of the fault is massive Mountain Limestone, forming the bold bluff of the Observatory Hill. On the northern side are much contorted red grit and limestone shales (see Map, p- 147). Viewed from the opposite side of the river, the right bank, from the Suspension Bridge for half a mile northwards, shows the following features. The eastern tower of the Suspension Bridge is built on a solid mass of limestone, the western face of which fronts the river as an almost perpendicular wall of rock. At right angles to this, and parallel with the bridge-road, there is a second face due probably to a joint plane, or a minor dislocation of the strata parallel with that caused by the Clifton fault. This vertical face forms the southern boundary of a little recess in the rocks, in which lies the Clifton station. On the northern side of the station rises the somewhat dislocated mass of limestone which forms Observatory Hill, and which, on its southern side, abuts against Millstone Grit and Upper Limestone Shales brought down by the Clifton fault. The whole appearance of the side of the ravine now changes, and in place of vertical limestone cliffs there is a wooded slope. Close to the river, however, the rocks are well seen in section, and show bands of hard grit characteristic of the Upper Limestone Shales. These bands, passing under the Avon at the point marked a on the map, have hitherto caused a shallowing of the river at this point. Blasting operations are at present in progress by which this obstruction will be removed. Some 370 paces from the fault, solid limestone rises from the river-side (at c), but is, a little further north, cut into by a wooded notch (6) in which runs the path, known as the New Zigzag, which joins the road near Proctor’s Fountain. This notch starts from the point of junction, at the surface of the downs, of the solid Mountain Limestone and the Upper Limestone Shales, which are, however, here unconformably overlain by the dolomitic conglomerate of the Trias. The throw of the fault on this Gloucestershire bank I estimate at about 1150 feet vertically, which is some 350 feet greater than that given by Buckland and Conybeare (Trans. Geol. Soc. 2nd series, vol. i, p. 241), and by W. Stoddart (Proceedings of the Bristol Naturalists’ Society, new series, vol. i. p. 328). On the Somersetshire bank I make the throw 50 feet less. This difference may be due, in part at least, to the dying-out of the fault in that direction. Taking as a datum-point the intersection of the line of fault and that of high water on the Gloucestershire side, the rocks which have been relatively shifted downwards are Mountain Limestone, about 710 feet, and Upper Limestone Shales about 440 feet. If we take Ajqetoods soryrqeoory +/—n "4X0q OY} UI 04 po.trozor OF THE CLIFTON FAULT. 147 soTeys OMOJSOULIT LOMO'T |: hae sa Sa aay (Dae TI a (| aT ies | 0 1 “Ts Ue al oy een I 5 4 ater a “Wht. 3 i aa = AML yy Mil) AE Ff SINE Je TOSS VES (Ca Ve ZA Mm UT i. SPSar) Ei \_ ff LST a is a aT Y fs a 1 7 ul Nat) lll mT eu 2 i 2 | en SSS] 2] an i 00 77 Te a ; r = é Rai areas AAS 0 7 — ——o q) AN i \ un yf PEF Dee TF 1 See ges Se x Z Mi = NOLH s ie “Ave Ai I te LAI. VOB | aes ant ae Sih < igh "ih ‘Z D 7 7 TT a Ty jis fl ts ar 1 DL Sy = Ss am TNT) = * ~ = TH uy = . ‘soyeys | Z euojsoury, codd gq | i Ms i v ul oF a MW n ie Hix chee LSS = {i Silt n uh i 2 San SSS SE al Ii = = ae = i EF 7 TT (pas oat a h ith a Ay ae an a so Tw 4 z Lh A, {il TA nT ait T- te in in aie a Nee fA a MN de MIEN, a Dpeb7 SESS < SL Te Sani SS aa Sai Sia SD fe OO 7- me he He S SNE dea0 Amin ane ba soc es 17°26 Protoxide of iron (with a little \ 12-94 PELOMIGO)) ee L hoes alee Tamer? GUL Aceh. pee ee ae 6:94 WWapnesian4. 226 23.04. ube oe 4-74 Soda (with a little potash) .. 3°41 oss atc i). Sark eS eee 1:55 100-00 Specific gravity 2°931 The Porphyries—These are for the most part quartz-porphyries, which have nothing particularly remarkable in their appearance when compared with similar rocks from other districts. Some are more highly quartzose than others, but in all porphyritically developed crystals of felspar of more than microscopic size are extremely rare except in a few localities. Lithologically two varieties are di- OF THE RIO-TINTO MINES. O51 stinguishable, compact and schistose, but passing into each other. In general the interior of a mass is compact, while a schistose structure becomes more and more evident as the outer portions are reached, 7. ¢. those near the junctions with the slate. The difference in chemical composition between the two varieties of the porphyry is by no means great; and I am disposed to believe that the schistose structure has been developed by a continuance of the same pressures which have converted the Paleozoic mud- stones into slates. Reference has already been made to the existence of bands of porphyritic schists (altered shaly sandstone) in the slates. These so closely resemble the bands of schistose porphyries, that it is not in all cases possible to distinguish between them in hand specimens; indeed, the more one examines these rocks in the field, the more one is disposed to regard them merely as varieties of one and the same rock, serving as intermediaries in bridging over the passage from undoubted slates on the one hand to undoubted felspar-porphyries on the other. The following analyses of various specimens of the porphyries will show how closely they resemble each other. I add an analysis of the porphyritic schist for comparison :— Porphyritic Schistose Very solid schist. porphyry. porphyry. Water over H,SO, by 0°10 } 0:40 0-25 1 0-70 0-12 } 0-40 Bee OMELLOME ) (6. he ce5< : 0-45 | 0°28 LLG Fae Ae aia 64:50 67:00 76°34 PO VEAL TA 2 846 cha) ajtiayes eke 23°60 20°30 14°85 Oxide of iron... 2.5... 2°16 2°88 1:89 BR TO Ma Ph Se scans na esi sie: oe 1:40 2°80 0-10 MigeTReSTa: <1. 0%. 2. 5 wis ss 0:40 trace 0°50 ERLECS a Mats taste ots =o, trace trace trace Phosphoric acid ,..... 0°30 trace 0:05 Alkali as potash ...... 3°20 2°10 5:11 Carbonic acid, fluorine, PIMP LOSS) ee se os <5 = 4-04 4:22 0-76 100-00 100-00 100-00 Specific Gravity .. 2°62 2:60 2°65 Occasionally, as at the old-station quarry at Rio Tinto, the porphyritic schist may be traced right up to its contact with the compact porphyry, becoming more distinctly crystalline as it ap- proaches the junction, and leaving no doubt in the mind of the observer that the intrusive porphyry has been an active agent in producing the metamorphosis. It is remarkable how uniform in appearance the porphyries are, even when taken from localities widely separated from each other. Thus I have specimens from Valverde on the south, which cannot be distinguished from others broken near Madrono on the east, and Poderosa in the north. The porphyritic masses are usually lenticular in form, but they 252 J. H. COLLINS ON THE GEOLOGY often have fimbriated extremities as shown in fig. 1, where a is the lode-fissure, 6 the porphyry, and ¢ the slate. a. Lode-fissure. - 5, Porphyry. é. Slate. Their general direction is so similar to the strike of the slates, and their length is so much greater than their breadth, that they appear to be interstratified, unless the junctions are very closely examined. When, however, such examinations are made, the true nature of the association of the rocks is obvious enough, for the slates abut against the porphyries without in any way bending round them, or else the porphyry breaks up into branches and fingers, which are thrust between the lamine of the slates as in fig 1. This latter mode of occurrence may be well seen on the hill above Puerto Rubio. A bending of the laminz of slate around the porphyry is almost if. not quite unknown. In a few places the porphyry appears to be much like granulite. This is particularly observable between the Fuente Fria water- deposit and the first Malafio. Where the porphyries meet the slates by a faulted junction, as is frequently the case, a thick mass of “fault rock” is often observable at these junctions. This may be very well seen in the railway-cutting on the west side of the Mesa de los Pinos (see fig. 2) and on the Zalamea road about half a mile Fig. 2.—Section in Railway-cutting on the west side of the Mesa de los Pinos. c. Slate. d. Fault-rock. west of Bella Vista, both localities being situated on prolongations of the “ Valley lode”*. It is also well seen at the foot of the hill * In this railway-fault the slates (¢) are inclined at a very high angle to the north. They only appear to have a low angle because of the direction of the line of section, which forms but a very small angle with the line of strike. OF THE RIO-TINTO MINES, Oe below Gangosa, on the western prolongation of one of the branches of the North lode. This fault-rock consists of a hardened felsitic basis of disintegrated porphyry and slate enclosing angular fragments or partially rounded masses of porphyry, slate, and occasionally jasper—generally angular, and occasionally of considerable size. The bearing of these facts upon the age of the faults is obvious enough. Apparently the motion of the walls has broken up the porphyries and slates, the latter having been previously metamorphosed into the various forms noted above. In places the fissures must have remained open for a considerable time, while large quantities of fragments fell in and became surrounded by clayey matter. The Iron-ores.—In a considerable number of places, always on hill-tops, and always near masses of pyrites of greater or less extent, are horizontal beds of iron-ore, consisting of angular or occasionally rounded fragments of quartz, slate, and other rocks, cemented together by peroxide of iron, which is only slightly hydrated. The proportion of quartz or other matter in these rocks varies from less than 1 per cent. up to 50 or 60 per cent. In a few places these beds have yielded plant-remains, which indicate that they are of Miocene age. It would appear that they were formed at the bottom of lakes-—the ferruginous matter having been derived from the decomposition of the pyrites of the upper parts of the lodes— which stood much higher than at present. These beds of ore occur at various elevations, each different level no doubt indicating a period of approximate constancy in the Jevel of the waters, the different beds having been formed as the old lake-boundaries were broken through, and new ones formed at a lower level*. The following patches of iron-ore of a sedimentary character appear to indicate the former and successive existence in the neigh- bourhood of the mines, of no new fewer than six ferruginous lakes. The heights given are merely approximate, as determined by a pocket-aneroid. The patches bracketed together appear to have been once continuous, and have been separated by subsequent subaérial denudation. * 'The chief of these deposits, that of the Mesa de los Pinos, has been well described by Mr. J. A. Phillips in his paper ‘‘On the Occurrence of Remains of Recent Plants in brown Iron-ore,” Q.J.G.8. vol. xxxvii. p.1. He gives the following analysis of a sample of the iron ore from the Mesa, which may be taken as a pretty fair average result for the ore generally exported, except that there are usually present a few per cent. more of silica:— { hygrometric ......... 1-40 ete med 11-85 Po ECR me et au ee 1:53 IBEREICTOMICG) 2. ain sines cena det 84°65 PACIMEEMIR EH otis oes Sdn oho 0 eoeesie trace. Phosphoric anhydride ......... ‘14 Sul phe ee aeccsesces eo 23 \ i | 254 J. H. COLLINS ON THE GEOLOGY Above sea-level. Above sea-level. Cerro Colorado... 1794 ft. 4, Rio Tintillo .. 1370 ft. ‘| Cerro Salomon.. 1761 ,, 5 \Et. Planes» ...:; 4200 5,, Mesa de los Pinos 1500 ,, hassel 2: 7) DRSS yes ; | Cerro delas Vacas 1497 ,, G= Lai Nayas. i204 0500, 3 ee Wastar 322 VATS | poy eetalant. 0 oo... 5 2. 1470 ,, Notwithstanding the geologically recent origin of these ferrugi- nous lake-deposits, they are often traversed by quartz-veins fillmg shrinkage-cracks, and occasionally small masses of opal (Miiller’s glass) occur in cavities, showing that there must have been circula- tion of siliceous waters and deposition of silica in geologically recent times in this district. In addition to the iron-ore of these hill-top deposits, a very large quantity of excellent iron-ore of precisely similar character has been got out of the “‘ over burden” recently removed from the north side of the great open cast on the South lode. This has, I believe, been formed by the degradation of the ancient bog-iron deposits, and has sunk down over the pyrites into the extensive pre-Roman open workings. These are filled with brecciated masses, consisting largely of fragments of the iron-ore, mixed with slate and porphyry frequently in a state of complete decomposition. Occasionally the pyrites has decomposed near the surface so as to form a true “ gozzan” extending downwards for many fathoms, thus producing a ferruginous substance capable of being used as iron-ore under favourable circumstances, although, as it contains a large ad- mixture of clayey and earthy matters from the sides of the lodes, it is not usually preserved as such. Samples of this ferrnginous earthy matter often contain from 35 to 45 per ceut. of metallic iron, as shown by analysis. It is interesting to note that the waters issuing from the mines even now deposit considerable quantities of oxides of iron in the beds of the rivers wherever there are convenient situations. The following are analyses of some of these substances ; (H)—yellow ochre from the bed of the Rio Tinto near Manantiales, about 20 miles below the mines ; (1)—iron-ore from the Rio Tintillo :— H i Silica and insoluble .. 25°00 13°64 AOU TITIV AS ee aca tos Pkt 2°50 1:06 Ferric sulphate ...... 9:00 Ferric oxide... .(46'80)=hydrate 57:78. 73°00 ATSemi@ ate a. oe eee 0:27 Copper: © Besse ete trace. trace. Moisture and loss .... 5-45 12°30 100-00 100:00 The following may be regarded as typical analyses, (J) of the OF THE RIO-ITNTO MINES. 255 natural liquor issuing from the mines, and (K) of the liquor flowing from the cementation-tanks. Each of these is found to deposit iron-oxide wherever the waters are checked so as to allow of natural oxidation and evaporation. J. Natural liquor. K. Salida liquor. Ferrous sulphate........ 4-091 54276 grams per litre. Ferric sulphate ........ "036 6:075 E Aluminic sulphate ...... 504 °800 a Manganous sulphate .... "003 "016 % Zincic sulphate ........ *308 2°814 bs Cupric sulphate ........ L762 -282 pe Plumbic sulphate ...... “009 "040 ee Calcie sulphate. .. 2... .. "259 1:026 * Magnesic sulphate ...... 066 312 - Potassic sulphate ...... 023 -020 a Sodic sulphate ........ "052 "040 Fe Sulphuric acid (free) .... 1-274 “752 # pode chloride... - . ss 22s ‘017 *039 Pi Antimony and bismuth .. _ traces. traces. 5 a TSE GTe Tika eee Sain Beal ese 028 078 a SILL aretha 074 026 5s 8505 66:596 me Pyrites—The pyrites-masses are almost always contact-deposits, z.€. they occupy the enlarged portions of fissures separating two dissimilar rocks. Occasionally, it is true, both walls of a mass are composed of the same rock for a short distance, in vertical or hori- zontal extension, owing to the fact that the fissure has been made more nearly in a plane than is the bounding-surface of the two rocks, a phenomenon which has been frequently observed in other districts*. Some few of the deposits, however, appear to be con- tained wholly in slate, and others wholly in porphyry, but never far from a junction of these dissimilar rocks. The enlarged portions of the pyrites-lodes of Rio Tinto and other parts of the Sierra Morena, it seems to me, only differ in degree from the “shoots ” and “ courses of ore’ observable in connexion with fissure-lodes in other countries. Owing to the lenticular character of the porphyritic intrusions which occupy the original lines of weakness, and which have occasioned those openings which now form the lode-fissures, the junctions between the slate and the por- phyry are subject to considerable inflections (see map, Plate VI.) ; and although the more recent openings which now contain the pyrites have not followed these junctions everywhere exactly, still the result has been to produce fissures somewhat more made up of varying directions than is observable where a simple country-rock has been fissured. * See Foster “On the Great Flat Lode,” Quart. Journ. Geol. Soc. vol. xxxiv. p. 640. 256 J. H. COLLINS ON THE GEOLOGY It is obvious that any movement of one side of a fissure which is not a perfect plane, must result in bringing into juxtaposition pro- jecting portions of the opposite walls, in whatever direction the movement may have been; and consequently in eae irregular cavities of greater or less dimensions*. The cavities having been thus formed, it appears to me highly probable that they have been filled with pyrites by infiltration from the country rocks. Both porphyry and slate are almost everywhere impregnated, and the joints are often lined with pyrites, which invariably contains a trace of copper. The structure of the pyrites masses seems to me to bear out this idea. A somewhat banded arrangement or grain of the pyrites is often visible, running in a longitudinal direction; and frequently portions of the slate, very highly pyritized, have been detached from the walls, and enclosed within the main mass. Owing to the absence of cavities in the pyritous mass, crystals are exceedingly rare, and sometimes it is ab- solutely compact and structureless. The “lenticular” deposits of pyrites vary from a few yards up to three quarters of a mile or more in length, and in width from a few inches up to 500 feet. Frequently two or more of these are connected together by a thin vein, almost a thread, of pyritous matter; and they are generally traversed more or less by veins of richer ore, copper-pyrites, copper-glance, galena, &c., and occasionally also of nearly pure iron-pyrites, as well as by veins of barytes and quartz, these latter running in a direction transverse to the general direction of the mass. Character of the Ore.—As the average copper contents of the ores sent to England only vary between 3 and 4 per cent., I might almost. say 3z and 32, from year to year, an idea has been generally enter- tained that the ore deposits as a whole are remarkably uniform in composition. Nothing could be further from the truth, as was shown by the series of specimens sent to the Madrid Exhibition of 1883, which averaged from 20 to 30 Ibs. in weight, and contained from 0-5 up to 60 per cent. of copper. The following are the chief varieties of the ores which I have observed :— a. Poor sulphur-ore; almost pure iron-pyrites, but containing under 4 per cent. each of copper and arsenic. Generally minutely crystalline, but sometimes fine-grained and compact, breaking with an almost conchoidal fracture. Sold as poor ore (‘mineral pobre”). b. An ore like a, but containing variable quantities of earthy matters, silica, and silicate of alumina, up to 25 or 30 per cent. Valueless (‘‘ esteril ”). c. A substance like 6, but distinctly banded in structure, the siliceous matters often rising to 50, 70, or 90 per cent. The pyrites in this substance is generally more distinctly crystallized than in a or 6, the forms being the cube, the pentagonal dodecahedron, or a * This mode of formation, which is well known to all students of geological mechanics, is very simply explained by De la Beche in his ‘Report on the Geology of Cornwall,’ &c. p. 317. | ee ‘OF THE RIO-TINTO MINES. 257 combination of the two. Rarely the crystals reach the size of peas, but usually they are minute. This is absolutely valueless (“ esteril ”’). d. A soft powdery or easily pulverized substance, having the same composition as the poor ore a, seas valueless on account of its powdery condition. The particles under a lens appear to be crystals. This is known as “azufron.” Sometimes the crystals are coated superficially with galena or blende, as if they had been immersed in water capable of depositing those substances. e. Compact ore like a, but containing from 1 to 22 per cent. of copper, existing as copper-pyrites minutely disseminated throughout the mass. This is the typical ‘‘telera mineral,” and it is mostly treated on the spot. f. Compact ore like ¢ but richer, up to 32 per cent. This is the typical exportation ore so largely eotsomed in the manufacture of sulphuric acid, the copper, and sometimes the silver and gold, being afterwards extracted by “‘ wet” methods. g. Ore similar to f, but coated superficially or in the joints by basic sulphates of copper (brochantite, pisanite, &c.). This is also an exportation ore. * h. Copper-pytites, erubescite, and occasionally copper-glance, more or less mixed with iron-pyrites, quartz, blende, and other substances, occurring for the most part in veins or veinules traversing the ordinary pyrites. These assay from 4 per cent. up to from 12 to 14 per cent. en masse, and are all treated in the blast-furnaces, either raw or previously calcined, as ‘ mineral rico.” i. The same ore, but with much quartz present, reducing the percentage to 3 or 4 per cent. Valuable as a flux in the blast- furnaces (“‘ mineral cuarzo”). j. Mineral like hf, but very soft and much decomposed. Also remitted to the blast-furnaces, under the name of “ negrillo.” k. A compact mixture of galena, blende, and chalcopyrite, mingled with iron pyrites, yielding from.6 to 12 per cent. of lead and the same of zinc, with 3 or 4 per cent. of copper and 2 to 3 oz. of silver to the ton; known as “ plomizos,” and at present a béte noire at the mine. Some of this bears a considerable resemblance to the “bluestone” of Anglesey and to the “kilmacooite” of County Wicklow. 1. The same, but with the lead more differentiated into veins of galena, admitting of dressing or clean hand-picking. There is but little of this ore in the mines. m. Crystals, stalactites, or stalagmites of cupreous melanterite, containing from 4 to 12 per cent. of copper and from 2 to 10 per cent. of zinc. Often mixed with earthy matter, so that the copper is reduced to from 1 to 3 percent. This is sent at once to the washing-tanks, under the name of “ vitriolas.” n, 0. Porpyhry and slate, containing grains or veins of iron- pyrites; slightly cupriferous (“ esteril”). The varieties 6, c, and d appear to reveal much as to their mode of 258 J. H. COLLINS ON THE GEOLOGY origin. In ¢ we have, I think, the original pyritous schist or mineralized bands of the Paleozoic slate. The following analyses of the pyrites from different parts of the mines will give a very good idea of the composition of the ores as selected for various purposes, as well as of their freedom from vein- stone when well selected. For comparison I add two analyses (P) from a neighbouring mine where the ‘banded ” structure referred to above is very well marked. i. M. N. . i i Export Calcination San Filon al La Majada. ore. ore. Dionisio. Norte. — = eaeemT 1878. 1880. 1881. 1881.. Compact. Banded. : S11). i 43°98 50°19 47-25 50:00 49-50 37-00 | EL let 41°91 42°86 42°35 41:65 40°60 33-00 | Copper... .5.2:t0. S06 ., 2-99.00 4-46) 905. 213-622) 2442 | We Apap in Soin ee ]:47 ) undeter- {1:26 trace. | ATIC a Cee es mined. te trace. Copper sulphate .. 0-12 0-20 trace. — trace. Oxide of copper .. 0°50 trace. trace. trace. ATRGMIG: st. 55S.) a 1-00 0-92 0-61 0°25 0-49 0:47 ) Antony Fi _4-\ ae 0:06 0-10 trace. Alumina, bismuth, manganese, thal- 3 2 traces. traces. traces. traces. traces. traces. lium, nickel, cobalt, lime, and magnesia. Silica and insoluble. 0°28 trace. 2-40 2°62 2:14 22-60 Sulphate ofiron .. 0°50 — trace. eget: penton ces | Moisbure is¢ Sea. 2 3h 0°65 0:20 ‘ Oxygen and loss' .. . 0-73. 324 - 1:43) S25 99:88 100:00 100:00 100:06 96°35 97-49 Silver from 3 0z. to 1 oz. per ton in all. Gold from 8 to 11 grains per ton*. All the above are samples of well-mixed ores. I add opposite a series of analyses of picked specimens, none of them, however, distinctly crystallized. Q is chalcopyrite, of a good yellow colour, soft; Ris grey ore, with a good grey colour, and rather harder than usual; S, white pyrites, very light-coloured, a mass of minute crystals, very hard; T is galena, suberystalline and normal in appearance ; U, lead-mineral, fine-grained, grey, and granular. The pyrites-deposits at Rio Tinto are four in number, known respectively as the North lode, the South lode, the San Dionisio | lode, and the Valley lode. Of these, the South lode is that which was worked extensively by the Spanish Government before the mines were taken over by the present Company ; it is now chiefly worked as an open cutting. The thin branches or veins seen at * This small proportion of gold has hitherto resisted all efforts to recover it at a profit, except as regards a small portion of the ore treated at Widnes and in Germany ; yet it is worthy of remark that the terreros at Rio Tinto, which we may take in round numbers at 5,000,000 tons, contain more than 23 tons of gold, reckoning only 8 grains to the ton. The quantity of gold raised annually from the pyrites deposits of the Sierra Morena cannot be less than a ton and a half. Pe OF THE RIO-TINTO MINES, 259 Quebranto Huesos are, I think, connected with the eastern end of the South lode, while San Dionisio may be regarded as an extension westwards of the South lode. This and the North lode have been entirely opened up by the present proprietary, nothing haying been done upon them since the Roman times until about the year 1878. The Valley lode is not yet opened up. The North, South, and San Dionisio lodes all show abundant evidence of very extensive work by the Romans, and even of still more ancient works ; but as this paper is designed to deal only with the geological and mineralogical features of the district, and not with the mining operations which have been carried on from time to time, or with those which are now being carried on, I need not further refer to these points, except to draw attention to the series of enlarged sections given (figs. 3-8, p. 260), all of which refer to what is known as the South lode*. Q. R. S. de We Smlphar och. 33°04 24-03 52-81 15°82 40°89 Selenium...... Bec Warn trace. 0-10 0°13 ean 2 34-72 12a 46-12 aA | 36°24 Copper: 2465... 31°68 62-50 O-11 0-01 4-30 Arsenic :.::. i: 0-01 0:03 0-23 0-01 0-10 Lead 2 :s:ss%. 0:02 0-14 trace. 80-41 LEZE ARGIRONY- fea eee. trace. seh 0-40 0-20 PNG ee Ce 0°10 trace. trace. 0-14 6°66 Maat trace. play: 0-21 0-04 Silica andinsol.. 0°15 0:02 0-10 0-02 0-21 99°72 98°93 99°37 99°33 100-14 ro] CCl ae ia 0-033 0-010 0-005 0:015 0-015 Geld) aes. In all a few grains only to the ton. The Manganese-lodes.—A system of fissures having the same general directions as those larger ones which contain pyrites, occurs in the immediate neighbourhood of these latter ; indeed, the man- ganese-fissures often seem to be merely branches of the pyrites- fissures. Like them, they are frequently bounded by slate on one side and by porphyry on the other; but pretty often they have slate on both sides, although they are never found far from masses of porphyry. Occasionally they are entirely in porphyry. ‘The veins vary in width from an inch or less up to several yards. Unlike the pyrites-veins, in which siliceous deposits are conspicuously absent, the manganese-veins are generally very highly silicified, the walls being often converted into excellent jasper to a considerable depthr. The manganese-ore itself is sometimes very siliceous, but otherwise a fairly pure but hard variety of pyrolusite, assaying over 80 per cent. of peroxide of manganese. A great number of these veins occur in * A list of the various minerals which have been met with at the Rio-Tinto mines, comprising thirty-three species, is given by me in the ‘ Mineralogical Magazine,’ vol. iv. pp. 211-216. } An analysis of one of these jasper bands from Bella Vista has been given supra, p. 249. 260 J. H. COLLINS ON THE GEOLOGY Figs. 3-8.—Cross-sections of the South Lode at Rio Tinto, showing profiles of the ground removed. (Scale, 1 to 7500.) Fig. 3. Sec- tion at San-Inocente Shaft. Figs. 4-8, respectively 150, 200, 300, 3590 metres to the Kast. Fig. 3. \ ag VAP ag “yy Wes Uo son \/ \- Ne RANG SNe / . \ i / / \\ \ | Fated Porphyry. WW YU Slate. Petites Pyrites. “ss Sl ked P Hl rorhyry worked ate worked TUT) Preise word Oc > o% | Ferruginous breccia, and gozzan. rugin g the neighbourhood of Rio Tinto; but at present none of them are being worked, although a great many of them were in active operation some ten years since. The slate in the neighbourhood is generally of a purplish colour; sometimes it contains a series of concretionary kernels or “eyes” of cobaltiferous oxide of man- ganese, as shown in the sketch (fig. 9), which is taken from a specimen occurring a little to the west of Bella Vista. In the pyrites-region mineral veins other than those of cupreous pyrites and of manganese are extremely rare and of comparatively little importance. A few veins of lead, copper (oxides, sulphides, and carbonates), of blende, and of other minerals are known to Sl os eS Ne te LES IN } \ L— OF THE RIO-TINTO MINES. 261 exist in the quartz-syenite ; and some of these could certainly be worked to advantage by Cornish methods if the country were more fully opened up by roads and railways; but I reserve for the present all further reference to them. Fig. 9.—Slate with Kernels of Cobaltiferous Oxide of Manganese near Bella Vista. 4. Conclusion. A consideration of the facts here brought forward leads to the following conclusions :— 1. As to the Stratigraphy of the District :— (a) The slates are of late Devonian age, but they include in some places portions of still older clastic rocks, which have not yet been recognized in the neighbourhood in situ. (6) The slates, in parts, like the well-known “ Kupferschiefer ” of Mansfeld, were originally highly pyritous and cupriferous; but being interstratified with ordinary Posidonomya-schists, they are plainly much older. (c) Atter the slates had. been deposited and upheaved, they were cut through by great masses of syenite. As this syenite ranges pretty nearly with the present strike of the slate, it is probable that this latter had been folded into its chief synlines and anticlines before the intrusion of the syenite. The slaty cleavage, too, which now corresponds generally, but not invariably, with the bedding, was also produced previous to this intrusion, but may have been since “Increased. (d) Both slates and syenite have been penetrated by veins and masses of diabase. In the slates the diabase often follows the stratification for considerable distances and then cuts across at a very oblique angle, the mean direction being E.to W. In thesyenite no such prevalent direction of the diabase veins is observable. (e) The porphyries are distinctly intrusive in the slates, and not actually interstratified with them, although they often appear to be -so. A kind of selective metamorphism has, indeed, converted some Q.J.G.S. No. 163. U 262 J. H. COLLINS ON THE GEOLOGY of the stratified beds into a rock resembling the more schistose varieties of the porphyries; but proofs of the distinctness in origin of the porphyritic schists and the schistose porphyries are abundant. (7) The conversion of certain bands of the slates into chert or jasper was anterior to the appearance of the porphyries, since the cherty bands are traversed by them similarly to the slates them- selves, and since the “fault rock” contains fragments of the former enclosed within its substance. (g) As the porphyries were intruded into the stratified rocks long after these had been tilted up into their present position (7. e. nearly vertical), and as their composition, on the whole, is so similar, it seems not unlikely that they are actually composed of the melted-up lower portions of the synclinal curves. (h) While the porphyries were still in a semi-pasty condition, the pressures in directions normal to the strike probably continued to act, thus producing their markedly schistose structure parallel to the schistose structure of the stratified rocks. (z) The intrusion of the porphyry took place at a period so distant as to allow of immense denudation. We in fact see at the surface what was brought into its present condition at great depth. 2. As to the Ore-deposits :— (7) The opening of the main fissures took place along the lines of contact of dissimilar rocks, 7. ¢. along lines of least strength. (%) The process of filling-in these fissures was, as regards the pyrites, more chemical than mechanical; but still not entirely chemical. The great width of the fissures in certain places is here, as elsewhere, more apparent thanreal. On the one hand there seems to have been a great concentration of pyritous matter in solution, probably derived from pre-existing pyritous schists, into the more open parts of the fissures; and on the other a gradual removal, probably by the very same solutions, of much of the earthy matter of the enclosing slates, so as gradually to produce a large mass of very pure ore. The fact that schistose structure is often visible in the interior of great masses of the pyrites appears to me to be in favour of this theory of their mode of formation. The force of crystallization itself, too, may have enlarged the cavities continuously by pressure against the softened wall. (2) ‘That the solutions circulating within the fissures had solvent powers is evidenced by the softening and kaolinization of the rocks in the neighbourhood of the pyritous masses. Silica and lime appear to have been remarkably absent from these solutions ; but in the later vein-fillings the former has been deposited to a small extent, and sometimes accompanied by sulphate of baryta. (m) That the fissures were seldom really open to any great extent is, 1 think, indicated by the rarity of distinct and well-formed crystals of pyrites. At the same time the existence of fault-rock in the immediate neighbourhood proves that open fissures must have existed at one time. OF THE RIO-TINTO MINES. 265 (n) The formation of rich veinlets or “ leaders” of ore within the masses has been the result of subsequent operations, probably at very many different times. These veins appear to occupy faults and shrinkage-cracks, and to have been gradually filled by a segregation of substances from the main masses of pyrites. (o) Abundant evidence of numerous movements within the masses of pyrites is afforded by the numerous slickensides which are every- where and continually met with. (») The formation of the ironstone-beds which now cap the Mesa de los Pinos and other hills, although immeasurably more recent than that of the pyrites-deposits, took place so long ago that deep valleys have since been excavated through the iron-ore ; and the general level of the country has been so altered that the ancient lake-deposits now exist as hill-tops. 3. As to the Surface-Geology :— The broad features of the geology of the district, which have been described above, are very evident to any one who has studied the relations between geological structure and scenery. The slate- regions, which for the most part form the lower lands, generally consist of a series of low hummocky hills of a very bare and unin- teresting aspect; but occasionally the more silicified bands rise into sharp ridges of a rugged appearance, which, in the transverse valleys, are sometimes extremely picturesque, as in the gorge leading up to the Campo Frio “ digue”*. The jasper- and manganese-bands, too, are generally evident as distinctly purple stripes in the otherwise dull lead-coloured country. The barrenness of the slates seems to be due to their vertical condition, to the great and long-continued heats of summer, and to the absence of springs. The vegetation, where there is any, consists generally of the dull dark-green foliage of the gum-cistus. The valleys and watercourses, on the contrary, where the effects of the long summer drought are less felt, are usually filled with oleander bushes, whose abundant pinkish-red flowers mark out the topography in a very striking and beautiful manner. The por- phyries are scarcely more clothed with verdure than the slates, but the hills are much higher and more irregular in form, and the ground is generally strewn with rough greyish fragments of the rock. The asphodel, a palmetto, and little scrubby acacias are more frequently to be seen in the porphyry-tracts. The diabase has much richer vegetation, with many olives, oaks, and cork-trees, the surface between the trees being covered with brown and rounded fragments of decomposing diabase, while the rock-exposures are often markedly spheroidal or even columnar. The syenite has a very similar vege- tation to the diabase ; but the country rock is greyer, and the hills crowned with loose rocks, which often remind one of the granite tors * At Rio Tinto a reservoir of water, shut into a natural hollow by an arti- ficial wall or bank, is called a “‘ Digue” or a “‘ Dam” indiscriminately, although, of course, the term is only properly to be applied to the enclosing masonry or earthwork. v2 264 J. H. COLLINS ON THE GEOLOGY of Cornwall, but of course without their refreshing green turf-sur- rounding. In the immediate neighbourhood of the mines the natural barrenness of the mining part of the Andevallo is greatly height- ened by (1) The destruction of vegetation by the sulphur-smoke from, at Rio Tinto alone, the volatilization of about 200,000 tons of sulphur per annum ; (2) The destruction of brushwood and timber for the use of the mines ; (3) The removal of the unprotected soil by the occasional heavy rains. The climatal conditions have led to a much more rapid denudation than is observable in countries like England, and it will be readily understood that they have been greatly aided by the temporary conditions noted above. In the height of summer the surface-rocks of this region are often heated to 160° F., or even more during the day, while the coming of a wind from the north will sometimes reduce the temperature of the same rocks to 70° during the night—a range of at least 90° in perhaps eight or nine hours. These alternations of temperature have, in some cases, caused the scaling-off of thin layers of porphyry, diabase, ironstone-breccia, and other rocks from the more exposed masses on the hilltops and in the broader valleys in a most peculiar manner. I have picked up pieces of the ironstone-breccia measuring at least © 8 inches across, with a thickness not exceeding three quarters of an inch. In some spots the rocks have acquired, from this cause alone, rounded forms, which might easily be supposed to result from glacia- tion, while the flakes of rock cover the ground around to a depth of more than a foot*. It will be readily believed that disintegration, especially of the schistose rocks, proceeds very rapidly under such conditions as these. Furthermore, in the neighbourhood of the rock-junctions, a great part of the surface-slate, and even the porphyry, is so decomposed as to be commonly used as a kind of fire-clay (barro). The occasional heavy rains of spring and autumn, falling upon a ground so prepared, act with extreme energy and produce very marked effects, a single storm sometimes cutting out channels several yards in depth. These facts should be taken into account in forming an estimate of the time required to produce a given amount of denudation, as, for instance, * The finest example of this “ pseudo-glaciation ” which I ever saw occurred in the ironstone-breccia lying on the top of the hill alittle to the S.H. of No. 4 shaft on the North Lode; and at first I felt pretty sure that here, at least, I had met with a real glacial polishing —the angular pieces of quartz, with their ferruginous cement, were smoothed off so wonderfully. But I soon saw here, as I had seen on other oceasions, that there were no ice-scratches and that the apparently polished surfaces met each other in sharp re-entrant angles in such a manner that they could not possibly have been produced by friction. More- over, the stones were surrounded with bushels of thin flakes of precisely similar character which had peeled off from time to time, some of them being nearly a foot across, with a thickness of considerably less than one inch. OF THE RIO-TINTO MINES. 265 with regard to the relative ages of the successive ferruginous lake- deposits. Greatly as they differ in altitude, it is probable that their difference in age would not exceed a few thousands of years. Un- fortunately, however, we have no fossil. evidence on this point, since fossils have only as yet been found in the one deposit of the Mesa de los Pinos. EXPLANATION OF PLATE VI. Fig. 1. Map of the Rio-Tinto mining district. Scale z53o>:- 2. Section across the Rio-Tinto mining district. Scale zghoo- Discussion, Mr. P. Fow1er inquired why Mr. Collins attributed the iron- ore forming the outcrop of the pyrites-vein-deposits to the action of lakes. He believed they were due to decomposition of pyrites. With regard to the question whether the deposits of pyrites are to be characterized as veins or masses, he believed them to be veins, as they never cut out in depth; they often narrow, but open out again. Mr. Collins had omitted to notice that all the veins crop out in great depressions, due, probably, to enormous faults. he greater the depression the greater the width of the vein. Mr. Kirro agreed with Mr. Collins as to the iron-ore deposits being lacustrine in their origin. They were stratified, and contain the remains of plants. He also was inclined to class the masses of pyrites at Rio Tinto as veins. il} 266 CAPT. F. W. HUTTON ON THE GEOLOGICAL POSITION 27. On the Geotoeicat Position of the “ Wexa-pass Stone” of New ZEALAND. By Captain F. W. Horton, F.G.8. (Read June 25, 1884.) Tue northern part of Ashley County, in the Province of Canterbury, is, to the geologist, one of the most interesting districts in New Zealand ; for, as Dr. von Haast has truly remarked, it “ offers us the key to unravel the relations in which our young Secondary and old Tertiary beds stand to each other.” And as all the more important of the New-Zealand coalfields belong to one or other of these groups of rocks, the district becomes highly important from an economic point of view. The district in question is bounded on the north by the Hurinui River and on the south by the Waipara River, so well known to geologists as the locality whence Plesiosaurus australis, Owen, was obtained by Mr. Cockburn Hood. It is crossed by the railway and road from Christchurch to Nelson, which here. pass over a low range of hills by means of a depression called the Weka Pass, which gives the name to the limestone that forms the subject of this paper. In it there occurs a white, flaggy, argillaceous limestone, known as the Amuri limestone, which at both the Waipara River and Weka Pass lies conformably on green sandstones. All geologists who have visited these localities agree that the Amuri limestones and the green sandstones are parts of the same rock-system, which is called the Waipara System by Dr. von Haast and myself, and forms part of the Cretaceo-tertiary System of Dr. Hector and the officers of the Geological Survey of New Zealand. This Waipara System is considered to be of Cretaceous age, because the green sand- stones contain remains of marine Saurians and rest conformably on beds of coal and shales, containing leaves of dicotyledonous Angio- sperms, that form the base of the Waipara System. Above the Amuri limestone, both at the Waipara and Weka Pass, comes an arenaceous limestone, usually with small green grains scattered through it, called the Weka-pass Stone. It is of a yellowish white colour, but weathers white like the Amuri lime- stone. Above the Weka-pass Stone is a grey sandy marl, and above this, again, come thick beds of pale yellowish sandstone, with bands of shelly and coral limestone. These last beds, lying above the grey marl, are acknowledged by all New-Zealand geologists to be, probably, of Upper Eocene or Oligocene age. They are the Mount-Brown beds of the Geological Survey, and form the upper part of the Oamaru System of Dr. von Haast and myself. So far all are agreed; but opinions differ as to where the line separating the Waipara System from the Oamaru System should be » drawn. Dr. Hector and Mr. M‘Kay think that it should be taken between the Grey Marl and the overlying Mount-Brown beds; Dr. von Haast would make it between the Weka-pass Stone and the OF THE ‘* WEKA-PASS STONE ” OF NEW ZEALAND. 267 Grey Marl; while in my opinion it lies between the Amuri lime- stone and the Weka-pass Stone. On this point Dr. Hector says that he cannot satisfy himself “of any stratigraphical break be- tween the Amuri limestone and the overlying grey marls” *, ap- parently placing the Weka-pass Stone with either one or the other. Mr. M-Kay says, “‘ No doubt there is a considerable difference in the character of the fossils found in the calcareous green-sands [2. ¢. Weka-pass Stone] and those in the underlying Saurian beds; but, even admitting the conformity between them, this is to be expected. Stratigraphically, I could find no conclusive evidence of uncon- formity, and if the Weka-pass calcareous green-sands belong to the Waipara beds, no unconformity can be conceded as far as the upper- most beds of the Mount-Brown Series” +. Dr. von Haast says that in the northern parts of Canterbury the green sandstones of the Waipara are overlain by “ chalk marls, or chalk-like limestone” [7. e. Amuri limestone], which is succeeded by a glauconitic calcareous sandstone [z. ¢. Weka-pass Stone], and which is the highest bed of the series. He allows that a break sometimes, as at Weka Pass, appears to occur between these two calcareous rocks; but he argtes that this is only apparent, because the upper beds are always con- formable to the lower, and in some localities there is a gradual passage from the one to the other. He does not, however, name these localities. Such are the views held at present by those geologists who have visited the district. The object of this paper is to bring together all available evidence on the position of this divisional line. But before doing so it will be better to give the geographical distribution of the beds with which we are concerned. GEOGRAPHICAL DisTRIBUTION oF Rocks. The green sandstones and other associated rocks with acknow- ledged Cretaceous fossils extend from near Cape Campbell, on Cook’s Straits, along the east coast of the island, to the Hurinui, and then trend inland to the Middle Waipara and the Malvern Hills, lying between the Waimakariri and Rakaia rivers. In no other part of New Zealand are they known with certainty, and in no other part have any Cretaceous marine Saurians been found. The Amuri limestone occurs near Cape Campbell, and going southward, is found at various places along the east coast as far as Motunau, and again at Weka Pass and the Middle Waipara. Further to the south it is quite unknown, except possibly in the Trelissic basin on the Wai- makariri§. In the North Island it has been recognized by Mr. * K 28. —— coscinopora, var. armata, W...| 295 |]...|3¢/3€|.-.|..- * 29. —— violacea, Johnst., var. fissa, W.| 295 |-%|...|... +-|44]...|...| Adelaide. 30. ——symmetrica, Waters ............| 295 |...|...J3¢|5€].-.]... +-| Adelaide, Waurn Ponds. 31. —— ferrea, Waters . Beopebo een caed| | 23) be) bee) ben pec| sax see faa |thvea Ke) Een ey 32. —— pocilliformis, sp. “nov... wee] 299 |...) | 33. —— (Lunulites) magna, Woods w.| 295 [SE[S4). 0.1... *% 34. —— magnirostris, MacG. . .--| 296 |X%]...|-]... 35. —— eleyata, Woods.. soeactte eh 5 i 36. Porina coronata, Rss. . 'sk] Adelaide, Bird Rock 37. Lepralia edax, Bush .........ccs0ec0e0--| 297 [ME]. oI SEl- [HE] -oe ee Crag. 38. —— depressa, var., ie een: : 39. —— rostrigera, Sm. . 40. —— escharella, Rémer ...... .e-0e| 298 |...|34]...|.--[---]---|---| Oligocene. 41. —— burlingtoniensis, Waters ..... 299 |... XE/H].- | E/E! ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 280 List of Species (continued). a] Beceeee || feralal V).2) elo é ae | Bid 2 4 &| Allies and Localities. ARAEIES lets $ sis S\s P| als | 2 a lSlslS ie laia & Alsislolsiaia 42, Lepralia subimmersa, WacG......... | 299 Fe 43, —— confinita, sp. NOV.............020+.| 299 Pas 44, Smittia Tatei, 7. Woods .. eevee] 299 ine %\-% |...) Waurn Ponds. 45. —— Landsborovii ............00e000.2-| 300 |34].../% 46. —— reticulata, MacG... Sa ih \* | | 47. ——seriata, Rss. ........ wel SUOMeeat ose Ki 48. —— Milneana, B., v. cosquata, DW. 300 |.../¢ * 49. Schizoporella vulgaris, MOM. Jens es.< 300 |%i% 50. —— simplex, J., var.. eeseceeeeeeses| BOO [SEIS 51, —— phymatopora, Rss. . eeeeeee] BOO |S)... IS EI 52. —— striatula, fF nee Cn AR IC) SIKIK 53. —— fenestrata, Waters .............| B01 |...|... ee 54. —— Cecilii, Aud. . secececscceseree| BOL [ME]. IM 55. —— protensa, sp. nov.. --eef OOL |. 4X] || 56. Mastigophora Dutertrei, Aud....... B01 |sk/XIK) 57. Retepora marsupiata, Sin. . wo -| 302 [2/3]... | HE KELHE 58. Rhynchopora bispinosa, Johnst. -| 302 3K}... |e) | 59. Cellepora coronopus, Busk.. 1.42] 802 |S6/3E]...).../% 60. —— avicularis, Hincks ...............| 303 | KE) | 61. —— costata, fe eee RE NETS: ¥%}...]... |oo=|-Ke]-ee|aee Adelaide 62. —— divisa, SP. NOV. ...........eseeeeere| 303 [M]...].-. eS bo eee Bee Crag ? 63. —— mamillata, Busk ............6....-| 304 |4]...|€! 64. —— albirostris, Sm.. nerersct rece | ONS | Phe ¥| 65. —— pertusa, Sm. ........ serereee| BOD [ELE] | 66. —— ——,, var. ligulata, eee ae 305 |...|... % 67. —— biradiata, sp. NOV. ...............| 306 |...]... x oo tridenticulata, Busk ...........-| 806 |S¢/4¢|4)...|...]...!...| Yorke’s Peninsula. 69. —— fossa, Haswell ..........cccs:1e0e2, B07 MIMAKI KK | 70. ——- ——, var. marsupiata, nov. ...| 307 |...|... | | 71. Lekythopora hystrix, WacG....... a 308 |>k}...|% 72. Cupularia canariensis, Bush .....:...| 308 |3X¢/3<|.../% | 73. Selenaria maculata, Busk ..... 2] B09 KIX Kp eee Poa Bird Rock. | 1, CELLARIA MALVINENsIs, Busk. Salicornaria malvinensis, Busk, Cat. B.M. p. 18, pl. xiii. figs. 1, 2 ; pl. lxv. (67s), fig. 1; ‘Challenger’ Rep. Zool. pt. xxx. p. 91, pl. xii. figs. 1, 5, Cellaria maluvinensis, Waters, Quart. Journ. Geol. Soc. vol. xxxvii. p. 321, pl. xiv. fig. 3. Salicornaria immersa, T. Woods, Corals and Bry. of Neoz. Per. in New Zealand Colon. Mus. & Geol. Surv. 1880, p. 27, fig. 27. There are a few small fragments of Cellarza from the River- Murray Cliffs, and in only one piece is there a zocecial avicularium. This avicularian cell is of the same shape as a Zocecium, but is slightly smaller, with a wide avicularian aperture. Possibly a second species is also represented. C. malvinensis was found by the ‘ Challenger ’ widely distributed in the southern hemisphere in depths varying from 5 to 1450 fathoms. Loc. Living: Falkland Island, South Patagonia, Straits of Ma- gellan (Darwin). Six stations of ‘ Challenger’ Exped., from Ker- guelen, Marion Island, 8. America, Fiji Islands. New Zealand (Hutton). Port Wellington (Miss Jelly’s Coll.). Fossil: Mt. Gambier, Bairnsdale, Muddy Creek, Curdies Creek (Australia). 286 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM Nelson (from Leda marls vi.), Waipukerau, Shakespeare Cliff (Wan- ganui) [New Zealand]. 2. CELLARIA ANGUSTILOBA, Busk; Waters, Quart. Journ. Geol. Soc. vol. xxxviil. p. 260, pl. ix. figs. 28-30. The avicularia are all situated at the edge of the zoarium. The notch noticed in the avicularium of the Mount-Gambier specimens is not distinguishable in the Aldinga fossil. 3. Mempranrpora APERTA, Busk. (Pl. VII. fig. 3.) - Membranipora aperta, Busk, Crag Polyzoa, p. 33, pl. ii. fig. 13. A specimen from Aldinga has the zoarium conical, resembling LInnulites. The opesial opening is about 0:4 millim, long and 0°25 millim. broad, and the avicularia are about the same size. The avicularium has three openings, the upper one large, trian- gular; below this a slit-like opening, and still lower down a semi- lunate opening ; when these last two are broken down, they form a single opening, as figured by Busk. There is one distal rosette plate which is semilunate. This is not the Membranipora aperta of Manzoni (Bri. di Cas- trocaro, p. 9, pl. 1. fig. 4). Loc. Coralline Crag. 4. MEMBRANIPORA CIRCULARIS, d’Orb. Flustrina circularis, d@ Orb. Pal. Frane. p. 305, pl. 602. figs. 11-13. ? Membranipora tuberculata, Busk, Crag Polyzoa, p. 30, pl. i. ree In a specimen from the River-Murray Cliffs the zoarium consists of many layers, forming an irregular subglobular mass, but perhaps the colony commenced on a Cellepora. The opesia are variable, in some cases being quite round, in others subtriangular, with the lower edge straight and rounded, and contracted towards the top; in other cases the opening is more oval. Opesia of average cell 0-20—0°25 millim. long. There are two small avicularia above each opesial opening; but as the zocecia are arranged in quincunx, this makes them appear as if surrounded by six avicularia. The structure of Flustrina baculina, dOrb., and F. pentagona is similar. Loc. Sougé, prés de Vendéme (Loir et Cher), Cretaceous ; River- Murray Cliffs. 5. Mgweranrpora Savarri, Aud. Membranipora ligerensis, @Orb. loc. cit. p. 550, pl. 607. figs. 5, 6. Flustrellaria tubulosa, d’Orb. loe. cit. p. 532, pl. 727. figs. 9, 10. Membranipora subtilimargo, Reuss, Bry. Gist. Ung. Mioc. p. 179 (39), pl. ix. fig. 3. Membranipora Lacroixiz, Reuss, loc. cit. p. 40, pl. ix. fig. 8. 2? Membranipora reticulum, Reuss, Foss. Polyp. d. Wien. Tert. _ p. 98, pl. x1. fig, 25. ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 287 Vaginopora texturata, Reuss, loc. cit. p. 73, pl. rx. fig. 1. Membranipora Savartii, Busk, Crag Polyzoa, p. 31, tay. ii. fig. 6. Biflustra Savartu, Manzoni, Bri, di Castrocaro, p. 38, pl. ii. figs. 17, 17a; Smitt. Floridan Bry. p. 20, tay. iv. figs. 92-95; Busk, Rep. of ‘Challenger’ Polyzoa, p. 67, pl. xiv. fig. 2. Biflustra delicatula, Busk, Crag Polyzoa, p. 72, pl. i. figs. 2 & 4, pl. ii. fig. 7; Manzoni, Bry. foss. Ital. Contr. Il. p. 4, pl. i. fig. 5; MacGillivray, Zool. of Vict. decade vi. p. 28, pl. 57. fig. 2. For further synonymy, see Smitt’s ‘ Floridan Bryozoa,’ to which list probably several fossil Membranipore should be added. I have some rather large pieces of bilaminate Biflustra delicatula from the Crag of Leiston, in which I am unable to find any denticle within the lower margin, and Professor MacGillivray draws atten- tion to the fact that it exists only in two or three of the cells of the Queenscliff specimen, and is altogether absent in those from Queens- land. In the Italian Pliocene fossil species I do not find it, nor does it seem to occur in the Australian or New Zealand fossils that . I have examined ; on the other hand, in a recent specimen, in the Vincularia-form, from Palm Island, it is seen in all the zocecia. Smitt has called attention to the inconstancy of the tubercles in this species; and in a recent specimen from Penang, some zocecia have tubercles while others are without. The recent specimen from Penang has the opesia about 0°3 millim. long and 0-24 millim. wide, which is slightly smaller than in the fossil adnate upon a Rete- pora either from Aldinga, or the River-Murray Cliff. Bzflustra regularis, d’Orb., from Royan, is very closely allied, with rather larger opesial openings. Loc. Senonian of France, Miocene of Austria. Crag and Pliocene of England, Italy, and Sicily. Living: Florida, 29 fathoms ; Queens- cliff (Victoria); Port Curtis (Queensland); Philippine Islands, 10 fathoms ; Penang, &e. 6. MemBranipora RADICIFERA, Hincks; Waters, Quart. Journ. Geol. Soc. vol. xxxvill. p. 262. In a specimen from the River-Murray Cliffs there are small open spaces between the zocecia. 7. Mempranrpora RuyNoHoTA, Busk. (PI. VII. fig. 1.) Membranipora rhynchota, Busk, Crag Polyzoa, p. 33, pl. iu. fig. 7. A specimen from Aldinga is in the Eschara-form. The zocecia have large opesial openings 0°3 millim. long and 0:2 millim. wide. Below the opesia there is a large avicularium, with its opening much prolonged, and with the end very narrow for the acute mandible. The ovicell, with a keel down the centre and slightly depressed at each side, is surmounted by an avicularium. There has been much confusion with this species, as by an over- sight Mr. Busk gave a description of M. mimax as M. rhynchota 288 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM (Q. J. Mic. Soc. viii. p. 125), and the fossil from Bruccoli, which I called Biflustra rhynchota, should be renamed. Loc. Crag. 8. MEMBRANIPORA TEMPORARTA, Sp. nov. (PI. VII. fig. 16.) Although this Membranipora comes very near to several species, I have been unable to identify it with any. The zocecia are very large, with a large opesia, about 0°6 millim. long, whereas in few species is it more than 0*3—0-4 millim. Above each zocecium there are two avicularia with oval openings directed outwards. The ovicell is small, short, and but little raised. The species in most particulars corresponds with JM. pura, Hincks, but that has spines in place of the avicularia. Loc. River-Murray Cliffs. 9. Mempranipora (AMPHIBLEsTRUM) FLeminer, Busk. Membranipora Flemingu, Busk, Cat. B. M. i. p. 58, pl. Ixxxiy. figs. 3-5 (only) ; Hincks, Brit. Mar. Polyzoa, p. 162, pl. xxi. fig. 1-3. A specimen from Aldinga is growing upon a Retepora. There has been considerable confusion with the species, as it was at first made to include forms which have since been separated, but the fossil is undoubtedly Membranipora Flemingi, as defined by Mr. Hincks. It has the six oral spines, an ovicell similar to recent specimens, and sometimes two avicularia below the area, but more frequently there is only one, and this often at the end of a long tubular projection. In some cases this chimney-like avicularium is nearly as long as a zocecilum. Inno recent specimen has the ayicu- larium been found as much elevated, though it is always raised. MacGillivray refers (Trans. Roy. Soc. Vict. vol. xviii. p. 120) with’ doubt to specimens ‘“ seemingly referable to” WM. Flemingu, from Port Phillip Heads, Victoria. | Loc. Recent; European Seas, widely distributed. 10. Memprayipora (AMPHIBLESTRUM) CYLINDRIFORMIS, Waters, Quart. Journ. Geol. Soc. vol. xxxvil. p. 3238, pl. xvii. fig. 74, and vol. xxxvill. p. 263, pl. vil. fig. 13. 11. Mewprantpors (AMPHIBLESTRUM) PARVICELLA, T.-Woods. (PI. VIL fie. 5.) Selenaria parvicella, T.-Woods, Trans. Phil. Soc. Adelaide, 1880, p. 10, pl. ii. fig. 10; Waters, Quart. Journ. Geol. Soc. vol. xxxix. p. 441. Some fragments from the River-Murray Cliffs are better preserved than those from Muddy Creek and Bird Rock; and here we see there was a spine, or process, over the elongate “ avicular (?) cells,” and a broad denticle within the lower margin of the zocecial cells. The dorsal surface is granulated, with a few large pores, and is divided by parallel lines, which apparently radiate from the centre of the colony ; cross-lines, which are very indistinct, divide the dorsal surface into zocscial areas. The lateral rosette-plates form a regular ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA, 289 line along the middle of the lateral walls, and correspond with those of Biflustra delicatula, Busk, with which perhaps this species should be united. Mr. Woods’s description and figures are from the fossil upside down. 12. Mempranrpora (AMPHIBLESTRUM) Micuavprana, d’Orb. Cellepora Michaudiana, d’Orb. Pal. Frang. p. 404, pl. 604. figs. 7, 8, pl. 712. figs. 3, 4. Membranipora permunta, Hincks, Ann. & Mag. Nat. Hist. ser. 5, vol. vil. p. 151, pl. x. fig. 2; MacGillivray, Trans. Roy. Soc. Vict. vol. xviil:,p. 118. _ Membranipora falcata, MacGillivray, Trans. Roy. Soc. Vict. vol. ix. p. 132, The fossil differs from a recent specimen dredged off the coast of Victoria in having the zocecia and also the opesia a trifle smaller. The avicularium of this fossil and of the one figured by d’Orbigny is a little smaller than that in the recent specimens, in which it occurs at the base of an abortive zocecium; at least, this 1s my interpre- tation of a very curious structure, but this does not seem to be Mr. Hincks’s view, and it is well worth further examination. In the fossils the ovicells are simply rounded, without a raised rib; and this is the case in some of the ovicells of my recent specimens, while others have it. Perhaps the recent forms should rank as MW. Michaudiana, var. permunita, on account of the small zocecia to which the avicularia are attached. _ Loc. Fossil: Cretaceous; Le Mans, Le Havre, Tourtenay; Al- dinga (growing on M icroporella elevata). Living: off Curtis Island, Bass’s Straits ; off Victoria (on Adeona), Schnapper Point (MacG.). 13. Mrmprantpora (AMPHIBLESTRUM) TRIFOLIUM, Busk, var. PRo- PINQUA. Lepralia trifolium, MacG. Trans. Roy. Soc. Vict. 1363, 9"; Prod. of Zool. of Vict. decade iv. p. 28, pl. xxxvii. fig. 2. . The fossil from Aldinga has the zocecial avicularia and globular ovicells described by MacGillivray. The aperture (opesia) is about — the same size as that of a Crag specimen of Membranipora trifolium, Busk, in my possession, but it differs in having a zocecial avicu- larium (onychocellarium) and no other avicularia. The zocecia, in shape, are very similar to, those of recent Selenaria maculata, Busk. In the Report on the ‘Challenger’ Polyzoa, Mr. Busk fioures as Amphiblestrum umbonatum (pl. xv. fig. 66) a species or “variety with avicularia, which is closely allied to this. Itis strange that two forms so closely allied as Membr ranipora trifolum, Busk, and Lepralia trifolium, MacGillivray, should have received the same specific name when placed under different genera. The genus Amphiblestrum may be a convenience, but, as at pre- sent defined, it cannot be looked upon as sharply separated, and 290 A. W. WATERS ON CHILOSITOMATOUS BRYOZOA FROM with a large number of species it would be extremely difficult to say whether they should be placed in Membranipora or Amphi- blestrum. We see in A. papillatum, Busk, that it really has a thick border extending inwards, and not a plate, as in Membranipora Rosselvi. As the genus Membranipora is so large, and contains such a variety of forms, it is to be hoped that other characters may be found to separate this genus more definitely. Loc. Living: Queenscliff, Williamstown, and Western Port (MacG.). Fossil: Aldinga and River-Murray Cliffs, 14. Micropora(?) patuta, Waters. (Pl. VII. fig. 4.) Micropora patula, Waters, Quart. Journ. Geol. Soc. vol. xxxvii. p. 326. Steganoporella patula,Waters, Quart. Journ. Geol. Soc. vol. xxxviii. p- 265, pl. ix. fig. 31. A specimen from the River-Murray Cliffs, in the Lepralia-stage, is much better preserved than the one from Curdies Creek or Mt. Gambier, and has below many zocecia a zocecial (?) avicularium, surrounded by an almost circular border, within which is the man- dibular area, also surrounded by a granulated border, which is at the lower end narrow, but at the distal end becomes very broad. The avicularian opening is small and slit-like. Above the oral aperture there is a small ovicellular opening. The ovicell is scarcely at all raised, and would certainly be overlooked if it were not for this small opening; but in some cases the front wall is broken away, aud then the ovicell-chamber is distinctly seen. At each side of the ovicellular aperture there is a depression or opening. A similar supraoral opening has been figured in Membranipora. semiaperta, Reuss, Escharinella muralis, Gabb & Horn, Reptoflus- trina heteropora, G. & H., and Céllepora Mohh, Hagenow. Loc. Curdies Creek, Mt. Gambier, River-Murray Cliffs. 15. Micropora PERFORATA, MacG. Membranipora perforata, MacGillivray, Trans. Phil. Instit. Vict. 1859; Nat. Hist. of Vict. decade i. p. 29, pl. xxv. fig. 2. When speaking of var. clausa, Waters (Quart. Journ. Geol. Soc. vol, xxxvili. p. 505), I pointed out that Monoporella lepida, Hincks, was allied to VW. perforata, MacG., but they must be separated, either as varieties or species, on account of the much more fully developed avicularium of WM. lepida, though the position and direction of the avicularium is similar. From Napier, New Zealand, there are spe- eimens of V. perforata without avicularia, and others in which the small avicularium described by MacGillivray is pretty constant. In many zocecia in these Napier fossils there are several pores, as in cecent WM, lepida, from New Zealand; whereas in the Aldinga fossils it is rare to find more than the two below the aperture. The zocecia of the Australian fossils are very regular; but those from Napier show great variation in this respect, and therefore it is very pro- bable that Steganoporella elongata, Hincks, is only a synonym. ALDINGA AND THE RIVER-MURBAY CLIFFS, SOUTH AUSTRALIA. 291 Aperture about 0-1 millim. wide, which is slightly smaller than that of MW. lepida. Loc. Living: Queenscliff &c., Australia. Fossil: Aldinga, Mt. Gambier (Australia); Napier, and Tanners Run (New Zealand). 16. MonopoRELLA CRASSATINA, Waters. Monoporella crassatina, Waters, Quart. Journ. Geol. Soc. vol. XXXviii. p. 270, pl. vii. fig. 8; ibid. vol. xxxix. p. 435. Lepralia japonica, Busk, ‘Challenger’ Report on the Polyzoa, Cheil. p. 143, pl. xvii. fig. 5. Loc. Living: Cobie, Japan 8-10 fathoms (Busk). New Zealand (from Miss Jelly). Fossil: Napier and Waipukerau (New Zealand) ; Mt.Gambier, Waurn Ponds, Aldinga, River-Murray Cliffs (Australia). 17. Monoporetya sExaneuLaris, Goldf. (PI. VII. fig. 2.) Eschara sexangularis, Goldf.; Hagenow. Maast. Kreide, p. 81, pl. x. figs. 3, 4, 5. Eschara Clarke, T.-Woods, Trans. Roy. Soc. N. S. Wales, 1876, p. 2, figs. iv.—vil. ? Eschara piriformis, Sturt, ‘Two Exped. Interior S. Austr.’ 1833, ii, p. 253, pl. 3. fig. 2. Vincularia maorica, Stoliczka, Bry. Orak. p. 153, pl. xx. fig. 8. Monoporella sewangularis, Waters, Quart. Journ. Geol. Soc. vol. Xxxix. p. 435. Biflustra eacavata, Manzoni, Bri. foss. del Mioc. d’Aust. ed Ung. p. 67 (19), pl. xiii. fig. 14. There are two specimens from Aldinga, both fenestrate. In the one the fenestre are about 4 millim. long, in the other they are 7-8 millim., and in the first there are zocecial avicularia (onycho- cellaria), of the same shape as those figured by Hagenow, but without the great elongation. The avicularian opening is elongate in the centre of the avicularium. In my former paper I pointed out that, although identifying it with Hagenow’s species, I had not found any avicularia in either; and it is interesting to find that this character now justifies the determination. The oral aperture (0-22 millim.) is rather smaller than in the specimens from Muddy Creek &c. ; and in the zocecia surrounding the fenestre, there is not any oral opening, but an elongate slit, much like the avicularian opening. Beissel describes and figures such border cells in his Eschara pulchra, and blind cells are found in Adeona and other Chilostomata. There ‘is also a non-reticulated specimen from the River-Murray Cliffs, which Prof. Tate marked Eschara piriformis, Sturt; but the E. piriformis, Goldf., of the Maestricht beds has much larger zocecia, with very large opesial opening (0°6 millim.) nearly as wide as the zocecium. Some are flat bilaminate expansions, one is flattened and folia- ceous, while others are subcylindrical, and this Vincularia-form no doubt represents the Vincularia maorica of Stoliczka; and now that I have seen these, I consider that the fossil from Curdies Creek might be called var. minima or var. tuberculata. 292 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM Loc. Orakei Bay, New Zealand (in Vincularia-form); Muddy Creek, Bird Rock, Waurn Ponds, Murray Cliffs, Aldinga (reticulated and also a compressed branch). 18. SrEGANOPORELLA MAGNILABRIS, Busk; Waters, Quart. Journ. Geol. Soc. vol. xxxvili. p. 506. From the River-Murray Cliffs there are specimens in the Escharan and Hemescharan forms. In S. magnilabris the cells where division is about to take place are larger than the others, so that the large characteristic cells of Steganoporella are found to be followed by two smaller ones, each of which commences a new row. ‘The same thing is seen in Biflustra delicatula from the Crag, and in other species. - With a cylindrical mode of growth, as in S. neozelanica, there is no frequent multiplication of the rows, and no large cells are found. Mr. Busk, however (‘ Challenger’ Report, p. 76), points out that the operculum of S. neozelanica differs from that of S. magnilabris, which is the case, as the former has numerous irregular bars across the operculum, and four large teeth instead of the numerous small ones; and therefore I agree with him that they must be separated. Loc. Living: see loc. cit. p. 506, and Honoruru, Sandwich Islands (20-40 fathm.) (Busk). Fossil: Miocene; Castelgomberto? Mouille Mougnon (Cant. Vaud); Curdies Creek, Mt. Gambier, Bairnsdale, Batesford, River-Murray Cliffs (Australia); Waipukerau and Petani (New Zealand). 19. SrEGANOPORELLA RozireRt, Aud., var. InpIcA, Hincks. “Steganoporella Rozieri, Hincks, Ann. & Mag. Nat. Hist. ser. 5, vol. vi. 1880, p. 379, pl. xvi. figs. 1, 1a. ; For other synonyms see Waters, Quart. Journ. Geol. Soc. vol. XXxviil. p. 505. In the specimens from the River-Murray Cliffs, the zoarium is in the Vincularia-form, with about eight series of zocecia round the axis. There is a large opening replacing a zocecium, which is appa- rently the aperture of a large elongate avicularium; but from the state of preservation I do not feel sure about this interpretation, and possibly we have here only a broken-down zocecium. There are no other avicularia. | Loc. Living: India, Marion Islands, Holborn Islands, Darnley Islands, Torres Straits. Miocene: Sollingen. Bairnsdale, River- Murray Cliffs. 20. Crrerremva paprara, Moll. (non d’Orb.). For synonyms see Hincks, Brit. Mar. Polyzoa, p. 185, and Waters, Quart. Journ. Geol. Soc. vol. xxxvii. p. 265. The specimen from the River-Murray Cliffs has eight ridges on each side, a suboral pore, avicularia with a wide base but elongate, scattered among the zocecia, ovicell globose, about two thirds as wide as the zocecia; oral aperture 0:09 mm. wide. ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 293 Loc. Living: European seas, Madeira, Florida, Bass’s Straits. Fossil : European Eocene, Miocene, Pliocene, and Postpliocene, and Mt. Gambier. 21. CRIBRILINA FIGULARIS, Johnst. Lepraha figularis, Johnston, Brit. Zooph. ed. 2, p. 314, pl. lvi. fig. 2. Oribrilina figularis, Hincks, Brit. Mar. Polyzoa, p. 196, pl. xxvi. figs. 5-7. Cribrilina philomela, Busk, var. adnata, Busk, ‘ Challenger’ Re port on the Polyzoa, pt. xxx. p. 132, pl. xxii. fig. 7. . A specimen from the River-Murray Cliffs has characteristic zo- cecial avicularia (onychocellaria), which correspond most nearly with those figured for C. figularis, var. fissa, Hincks (loc. cit. fig. 8). This, like var. adnata, has numerous costz (nine on each side) ; more of the front is covered with coste than in Mr. Hincks’s figures, but not quite as much as in Mr. Busk’s. Oral aperture 0°13 mm., which is about the same as in the Australian species. Loc. Living: British, French, and Mediterranean seas; Capri, 40 fathoms ; off Marion Islands, 50—75 fath.; Heard Islands, 75 fath. Fossil: River-Murray Cliffs, Crag (Bell). 22. CRIBRILINA TERMINATA, Waters. Cribrilina terminata, Waters, Quart. Journ. Geol. Soc. vol. xxxvil. p.o20, pl. xvii, fie. 6S, vol. xxxviui..p.,507,, pl. xxi. fig, 6, and vol, xxxix, p, 456, pl. xii. fie. 17. A specimen from the River-Murray Cliffs has two or three minute avicularia above the oral aperture, and the zocecial avicularia are narrower than the one figured from Muddy Creek (U.c. vol. xxxix. plaxis fig, Lf). Loc. Fossil: S.W. Victoria, Bairnsdale, Muddy Creek, and the River-Murray Cliffs. 23. MucronELia MuUcRoNATA, Smitt; Waters, Quart. Journ. Gecl. Soc. vol. xxxvil. p. 328, pl. xvii. fig. 66, vol. xxxvill. pp. 266 & 507, and vol. xxxix. p. 436. The mucro supports an avicularium directed forwards. It occurs in Eschara- and Hemeschara-form. 24, Mucronetta niripa, Verrill, Discopora nitida, Verrill, Amer. Journ. Science, vol. ix. p. 415, pl. vii. fig. 3 (1875). Mucronella nitida, Verrill, Proc. U.S. Nat. Mus. p. 195; Waters, Quart. Journ. Geol. Soc. vol. xxxvill. p. 507. Smittia nitida, Hincks, Ann. & Mag. Nat. Hist. s. 5, vol. vii. p. 159, pl. ix. figs. 5, 5a. Lepralhia reticulata, var. incequalis, Waters, Ann. & Mag. Nat. Hist. ser. 5, vol. iii. p. 41, pl. ix. fig. 3. Smittia trispinosa, Johnst., var. ligulata, Ridley, Proc. Zool. Soc. London, 1881, p. 53, pl. vi. fig. 9. The Murray-Cliff fossil incrusts a Cellepora. It shows consider- able variation in the size of the avicularia ; sometimes they are ligu- Q.J.G.8. No. 163. Y 294 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM late ; on other zocecia they expand considerably towards the extremity. With a form like the present it is difficult to know whether it-should be called Smittia or Mucronella, and the two genera are not sharply defined. Mucronella delicatula, Busk, Chall. Rep. p.156, is, no doubt, closely related ; but the triangular mandible shows that the two forms are not absolutely identical. I have a specimen dredged from the coast of Victoria which has a narrow ligulate avicularium, but I do not think that it ought to be separated from those with a larger avicularium, as the shape is approximately the same. Mr. Busk calls attention to the central denticle being in front of the operculum, as if it were exceptional ; but this is the rule in this family. Loc. Living: Viueyard Sound and Long Island Sound (V.); Africa (H.); Victoria Bank, 8.E. Brazil (82 fath.); Victoria (on Adeona); Naples (W.). Fossil: Crag (W.), Bairnsdale and River- Murray Cliffs. This or a variety fossil from Waipukerau and Napier (New Zealand). 25. Mucronetta coccinea, Abildgard, var. mamr~iaTa, Busk. A specimen from Aldinga incrusteld a Cerithium or allied shell. The surface is smooth or faintly sulcate, with a single or double row of pores round the base. The ovicell is very small and decumbent. The fessil is so badly preserved that it was not readily recognized. Loc. Living: coast of Antrim. Fossil: Crag, Aldinga. 26. Mucronetuia coccinea, Abildgard, var. REsuprnaTA, Manz. Mucronella coccinea, Waters, Quart. Journ. Geol. Soc. vol. xxxvii. p. 266. In well-preserved avicularia it is ae that the mandible was spatulate, but the avicularian opening triangular. Loc. Aldinga; Mt. Gambier. 27. MicroPpoRELLA GRISEA, Lamx., form ADEONA. Adeona grisea, Lamouroux, Expos. Méth. p. 40, pl. xx. fig. 5 Kirchenpauer, “Ueber die Bry. Gatt. Adeona,” Journ. Mus. Honetitey 1579; 1,0, pl. a. 12, Sou. Dictyopora grisea, MacGillivray, } Nat. Hist. of Vict. decade vii. p: 23,.pl. 66: fig. 1, ta, b,6,'4- Dictyopora cellulosa, MacGillivray, Trans. Roy. Soc. Vict. 1868; Nat. Hist. Vict. decade v. p. 37, pl. xlvu. fig. 1, and decade vii. pl. ‘Ixvi. fig. le. ae cellulosa, Kirchenpauer, op. cit. p. 10. Microporella cellulosa, form Adeona, Waters, Quart. Journ. Geol. Soc. vol. xxxix. p. 437. From Muddy Creek there is a fragment spreading out in flabelli- form manner from the base, to which probably a flexible stem was attached. From the range of zocecial variability found in specimens that I have examined, and from the published descriptions, there does not seem to be sufficient reason for separating WM. grisea from M. cellulosa. ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 295 Loc. Living: various Australian localities. Fossil: Muddy Creek. 28. MicroporELta coscrnopora, Reuss, var. MucRoNATA, MacG. Lepralha mucronata, MacGillivray, Tr. Roy. Soc. Vict. 1868. Eschara mucronata, MacG., Nat. Hist. Vict. dec. v. p. 43, pl. xlviii. figs. 6, 7. Microporella coscinopora, Reuss, var. armata, Waters, Quart. Journ. Geol. Soc. vol. xxxvil. p. 331, pl. xv. fig. 25. Loc. Living: Queenscliff and Schnapper Point (MacG.), Port- Philip Heads (A. W. W.). Fossil: Curdies Creek, Muddy Creek, River-Murray Cliffs. 29. MicRoPORELLA VIOLACEA, Johnst., var. rissa, H. | Microporella fissa, Hincks, Ann. & Mag. Nat. Hist. ser. 5, vol. vi. p. 381, pl. xvii. fig. 4. 30. MicRopoRELLA syMMETRICA, Waters, Quart. Journ, Geol. Soc. vol. xxxvil. p. 332, pl. xvii. fig. 83. 31. MicroporELLA FERREA, Waters, loc. cit. p. 330, pl. xvil. fig. 72. 32. MiIcROPORELLA POCILLIFORMIS, sp. nov. (Pl. VII. fig. 8.) Zoarium dome-shaped, 7 mm. diameter, in growth resembling Cupularia. Zocecia suboval, convex, surface covered with large pores, with a raised suboral pore just below the oral aperture. Oral aperture rounded at the distal end, straight below, 0°24 mm. broad. There are two distal rosette-plates, each of which usually has two openings. On the under surface of the colony the area of each zocecium is distinctly marked and is convex. Loc. River-Murray Cliffs. 33. MicropoRELta MAGNA, T.-Woods. (Pl. VII. fig. 7.) Lunulites magna, T.-Woods, Trans. Phil. Soc. Adelaide, 1880, p. 7, pl.i. fig. 6a—6d. Zoarium large (25 mm. diam.), dome-shaped, consisting, in the specimen examined, of one layer of zocecia, slightly elevated along eight lines radiating from the centre; Mr. Woods says, “ In the younger specimens .... irregularly pentagonal; in the older specimens ... . irregularly lobed or sinuated.” On each side of these lines the direction of the avicularia is opposed, being directed diagonally upwards to the right on one side and diagonally upwards to the left on the other side. Zocecia raised, especially near the aperture, with large pores over the surface and a large suboral pore below the aperture. Oral aperture large (0°23 mm. wide), straight on the proximal edge with the corners rounded ; the distal edge of the aperture forms half a _ circle. ‘The true shape of the aperture is sometimes obscured in the older cells. Avicularia large, broad; aperture pointed above, rounded below. I have not had the opportunity of examining the Y 2 296 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM under surface of the zoarium ; but Mr. Woods says, “ Under surface finely radiately ridged, with a narrow slit-like pore at the margin.” Loc. Mr. T.-Woods gives Aldinga and Mt. Gambier. 34, MicroporELLa (DiporvLa) MaentRostRis, MacG. Microporella introversa, Waters, Quart. Journ.Geol. Soc.vol. xxxviii. p. 268, pl. ix. figs. 33, 34. Lepralia magnirostris, MacGillivray, “New or Little-known Polyzoa,’’ pt. 2, Trans. Roy. Soc. of Victoria, vol. xix. p. 134, fig. 6. Specimens from the River-Murray Cliffs grow either in the Hem- escharan form when the dorsal surface is coarsely granulated and has large pores, or in superposed layers with zocecia of the same size as those from Mt. Gambier, but in a better state of preservation; and here the central pore is very distinct and raised, but with a cleft in the upper (distal) part of the raised tube surrounding the pore. This better-preserved material shows that I was misled in supposing that the avicularia were directed inwards; I then attributed the avicularia to the wrong zocecia. Loc. Fossil: Mt. Gambier; River-Murray Cliffs. Living: Port- Philip Heads. : [Since this paper was read, MissJelly has sent me a recent specimen from Port-Philip Heads (Australia). This is in the Hemeschara- form, but the dorsal surface was perhaps attached to a sponge, as it is studded with large erect pore-tubes resembling those on the dorsal surface of Selenaria maculata, and besides these there are calcareous offsets, which are traversed by numerous tubes, and appear to have a sponge-like structure. I hope to make a further examination and sections of these interesting radicles. | This and the last species are very closely allied and should per- haps be united under one name. In both the recent specimen and the one from the River-Murray Cliffs the peristome is more raised than in the one I figured. 35. MicroporELLA ELEVATA, T’.-Woods. (Pl. VII. figs. 6 and 9.) Eschara elevata,T.-Woods, Trans. R. Soc.N.S.W. 1876, p. 2, fig. 10. Microporella elevata, Waters, Quart. Journ. Geol. Soc. vol. xxxvii. p. 330, pl. xvii. figs. 63, 64, pl. xvii. fig. 90. When describing the fossil from Curdies Creek I pointed out the great difference in zocecia from different parts of the same colony, and some well-preserved specimens from the River-Murray Clifts, showing in places the structure given in fig. 63 (Joc. cit.), have in other parts a much more regular and elaborate structure. The peristo- mial region is raised and surrounded by a ridge, with small pores within the area thus formed; down the middle of each zoccium there is a straight ridge which expands at the lower part of the zocecium, surrounding the median pore. On each side of this line there are large irregular openings. There are very curious zocecial avicularia occurring only near the border of the colony with a nearly round aperture divided by a cross har near the lower edge. ALDINGA AND THE RIVER-MUBRAY CLIFFS, SOUTH AUSTRALIA. 297 Loc. Curdies Creek; Mt. Gambier; Bairnsdale ; Muddy Creek ; Spring Creek ; River-Murray Cliffs. 36. Portna cornonata, Reuss. For synonyms, see Waters, Quart. Journ. Geol. Soc. vol. xxxviil. p. 333, to which add :— Eschara gracilis, MacGillivray, Nat. Hist. of Vict. decade v. p. 40, pl. xivii. fig. 3; Busk, ‘Challenger’ Report, Zool. pt. xxx. p. 141, By ex: fiz. 6. Portna gracilis, Hincks, Ann. & Mag. Nat. Hist. 1881, p. 60, pl. iii. fig. 5. Haswellia australensis, Busk, loc. cit. p. 172, pl. xxiv. fig. 9. Before describing Porina coronata from Curdies Creek (Quart. Journ. Geol. Soc. vol. xxxvii. p. 333. I had received from Mr. Haswell specimens of his Myriozowm (Haswellia) australiense, in which the peristome is tubular, often entirely surrounded by openings which are either simple pores or have ayicularian covers. There is great irregularity in these peristomial pores or avicularia, so that very frequently there is only an avicularium below the aperture ; in other parts in the same colony there may be two or three at the side; in others they regularly surround the aperture. Sometimes the peristome is flattened on the distal edge. The central pore (median pore) is usually only a rounded aperture ; at other times in the same colony from Holborn Island (collected by Mr. Haswell) it has a tubular projection; to show an extreme case, I figured from Curdies Creek a very delicate specimen with very marked tubular pores ; and upon reexamination, I find that from such a specimen to the large flat growth there is no break in the series, so that I feel quite convinced that the determinations then made were correct. The opercula of the specimen sent as WM. australiense are slightly smaller than those from typical #. gracilis, but the shape is the same, and so is the attachment of the muscles. As the ridge for the muscular attachment is characteristic, and differs from any other with which I am acquainted, this species may be made a test case, showing that the modern classification is an advance upon that which laid the greatest stress on the mode of growth. In both fossil and recent specimens the pore is sometimes elongate, sometimes round. The fossils from the River-Murray Cliffs, Aldinga, and Adelaide are all either in the form 6, as vertebralis (see Bry. from S.W. Victoria, p. 334), or are a little flattened. 37. Lepratia EDAX, Busk. | Cellepora edax, Busk, Crag Polyzoa, p. 59, pl. ix. fig. 6, pl. xxii. fig. 3. Br maies edax, Hincks, Brit. Mar. Polyzoa, p. 311, pl. xxiv. fig. 7, 7a, 8; Smitt, Floridan Bryozoa, pt. ii. p. 63, pl. xi. figs. 220-228 ; Waters, Quart. Journ. Geol. Soc. vol. xxxviii. p. 270. Cumulipora angulata, Reuss, Septarienthon, p. 63, pl. viii. fig. 12. Zoarium dome-shaped, about 30 millim, diameter, composed of many layers of zocecia. The under surface is cupulate, and the zocecia 298 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM here radiate in uniserial rows from the centre, with the greatest regularity, whereas on the upper suface numerous colonies are seen to start from various points of the surface. The under surface is divided by radiating and bifurcating sulci, and the part between these is raised, and along the ridges there are elevations looking like points of attachment. In this respect the dorsal surface resembles that of Selenaria maculata. Zocecia very little raised, irregularly hexagonal, separated by distinct raised borders with large pores round the edge of the zocecium; small avicularia below the aperture, with the opening rounded or slightly acute, directed down- wards. Oral aperture with the proximal edge nearly straight, the distal edge rounded, formed of more than half a circle, with two contractions inside the aperture near the middle; at widest part about 0°12 mm. wide. Ovicell raised, globular. I have already pointed out that the aperture in recent specimens is larger than im that from the Crag, and both the specimen from Mt. Gambier and this one from Murray Cliff correspond in this respect with those from Florida. In the Australian fosstls no zocecial avicularia (onychocellaria) have been found. Some ovicells show an indistinct area on the front; but this is not distinguishable on all, and the ovicell is more globular than figured by Mr. Hincks. Mr. Busk* refers to finding “the backs of the polyzoan cells usually disposed in parallel rows, much as they are on the concave surface of some Lunulites,” and Smitt seems to have noticed the same thing; it is therefore interesting to find it now ina true Lunaulites-form. 38. LEPRALIA DEPRESSA, Busk, var. Lepralia depressa, Busk, var.—Waters, Quart. Journ. Geol. Soe. vol, xxxviul. p. 509. In a specimen of this variety from Aldinga there are small, eloiian raised, granulated ovicells. 39. LEPRALIA ROSTRIGERA, Smitt. Escharella rostrigera, Smitt, Floridan Bryozoa, p. 57, pl. x. figs. 203-205. A specimen from the River-Murray Cliffs is growing in the Lepralia-stage. The hexagonal zocecia are very little raised and the surface is covered with large pores. The aperture is nearly round, with two lateral contractions; width 0°14 millim. There is usually a small avicularium pointed upwards on one side of the aperture, but seldom on both sides. Loc. Florida, 35—43 fathoms. 40. LepRaLia ESCHARELLA, Romer (in Vincularia-form). Vincularia escharella, F. A. Romer, “ Die Polyparien des Nord- deutschen Tert. Geb.” Paleontographica, vol. ix. p. 6, pl. 1. fig. 1. This is evidently allied to LZ. burlingtoniensis, but the hexagonal zocecia are much larger, and the whole surface is covered with large pores. The oval oral aperture is larger, measuring about 0°3 millim. across. Loc. Oligocene of Lattdorf (Romer), Aldinga. * Crag Polyzoa, p. 59. ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA, 299 41. Lepratia BURLINGTONIENSIS, Waters, Quart. Journ. Geol. Soc. vol. xxxviil. p. 270, pl. vii. fig. 6 42, LePRALIA SUBIMMERSA, MacG. Lepralia subimmersa, MacGillivray, Nat. Hist. of Victoria, Zool. decade iv. p. 23, pl. xxxv. fig. 5. Zoarium in Eschara-form growing as solid lamellate anastomosing fronds. Zoccia subhexagonal, bounded by prominent slightly sinuous lines; surface smooth, with large pores near the border. Oral aperture round above, concave below, with a small oral avicu- larium just below the aperture, sometimes in the peristome. The state of preservation does not allow of satisfactory examination of the aperture. From one broken-down ovicell it is clear that it was entirely immersed. Loc. Living: Warrnambool. Fossil: Aldinga. 43, LEPRALIA CONFINTTA, sp. nov. (PI. VII. fig. 10.) Zoarium in Eschara-form, flat. Zocecia indistinct, surface with a few large pores amd small round avicularia scattered about; oral aperture round above, slightly contracted below, with a tooth on each side. The aperture (0°15—0-16 mm. wide) is surrounded by a round band. The zocecial characters remind us of Myriozowm truncatum, but the cells and aperture are there larger. It is also allied to Leprala crassa, Reuss, and L. varians, Seg. I have some flat bilaminate fragments of a similar recent Lepralia dredged by Mr. Brazier from Piper Island (9 fathoms), but the zocecia are much smaller, with the aperture about 0-12 mm., and the surface is dotted over with numerous small round avicularia. Possibly they should be united, although the more robust character of the fossil makes a considerable difference in the general appearance. Loc. Aldinga. 44, Surrrza Tarver, T.-Woods. (Pl. VII. fig. 15.) Eschara Tatei, T.-Woods, Trans. Roy. Soc. N. 8. W. 1876, p. 3, fig. xv. Smittia Tatei, Waters, Quart. Journ. Geol. Soc. vol. xxxvil. p. 337, pl. xvii. fig. 65, and vol. xxxviii. p. 271, pl. vil. fig. 10, pl. vin. fig. 21. Smittia Perrieri, Jullien, Bull. de la Soc. Zool. de France, p. 19, pl. xvi. fig. 45. There are small flattened branches from the Murray Cliffs; and from Aldinga there is a most interesting colony in which the round branches anastomose and form a reticulate mass. The diameter of the branches is about 3millim. In this specimen there is a peristomial sinus instead of the suboral pore; but this sinus is frequently almost ‘closed in above, and no doubt the function is the same in both cases. Loc. Living: N.W. of Spain, 2108 metres (Jullien). Fossil: Curdies Creek Mt. Gambier, Bairnsdale, Waurn Ponds, River- Murray Cliffs, Aldinga. 300 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM 45. Sarria Lanpsporovit, Johnst. Lepralia Landsborovi, Johnst. Brit. Zooph.ed. 2, p.310, pl. liv. fig. 9. The aperture of the round suboral avicularium is very small, appearing as a point or a sublunate opening. The specimen is in the Lepralia-form. Loc. Living: British seas, Mediterranean, Florida, Australia (H.), Greenland. Fossil: River-Murray Cliffs. 46. Smirrra ReETIcULATA, MacG.; Waters, Quart. Journ. Geol. Soc. vol. xxxvill. p. 272. 47. Smirrra serrata, Reuss; Waters, loc. cit. p. 272, pl. viii. fig. 17. 48. Surrrra Mitweana, Busk, var. comevata, nov. Mr. Busk described in the Crag Polyzoa a fossil as Lepralia Ed- wardsiana (p. 44, pl. v. fig. 2), but this name he subsequently changed to £. Milneana (p. 132). The fossils from Aldinga in general appearance more resemble Mucronella variolosa, but the same main characters are foundin both. In both the Crag and the Australian fossils there is a broad oral plate extending nearly across the aperture, the peristome is thickened and raised, and there is a small avicularium on one side, which usually forms a peristomial sinus, but sometimes in the Australian fossils it is raised and forms amucro. The avicularia are in both in about the same position, but in the Aldinga specimens they are not at all raised, and are rounded at both ends with a wide mandibular opening directed in- wards. In the variety the zocecia are bordered by a thick raised line, and are surrounded by a row of large pores. Loc. The type occurs in the Coralline Crag (B.) and in my eollec- tion from Leiston, Suffolk. The variety is represented by two specimens, one growing on Cellepora tridenticulata, B., and the other on Monoporella sexangularis, Goldf., both from Aldinga. 49. Scu1zoPoRELLA VULGARIS, Moll. Eschara vulgaris, Moll, Seerinde, p. 61, pl. 111. ee 10; Avi. 50. ScHIZOPORELLA SIMPLEX, Johnst. var. ALDINGENSIS. Lepralia simplex, Johnston, Brit. Zooph. ed. 2, p. 305, pl. liv. fig. 4. Schizoporella simplex, Hincks, Brit. Mar. Polyzoa, p. 246, pl. xxxv. figs. 9, 10: A specimen from Aldinga varies from the British species in having no umbo, but we have in many species seen that the umbo is not a constant character, and I have therefore thought 1t advisable to con- sider it only as a variety. There are no avicularia, and the width of the aperture is 0°13 millim. Loc. Living: British and Irish. Fossil: Scotch Glacial deposits. 51. ScurzoPoRELLA PHYMATOPORA, Reuss. Eschara phymatopora, Reuss, Foss. Anth. & Bry.v. ee p. 272, pl. xxii. fig. 1. Schizoporella phymatopora, Waters, Quart. Journ. Geol. Soe. vol, xxxvii. p. 338, pl. xv. figs. 31, 32, and vol. xxxviil. p. 510. ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 301 Myriozoum honolulense, Busk, ‘ Challenger’ Report of Polyzoa, p- 170, pl. xxv. fig. 2. Specimens from the River-Murray Cliffs occur as hollow cylinders of about the same size as those from Bairnsdale. The dorsal surface is divided into oblong zocecial areas. The rosette-plates are at the base of the zocecial wall, with, normally, two distal plates. Loc. Fossil: Bartonian of Val di Lonte & Ferrara di Monte Baldo (Italy); Curdies Creeks; Bairnsdale and River-Murray Cliffs. Living: Sandwich Islands, 20-40 fathoms. 52. ScHIZOPORELLA STRIATULA, Smitt. Gemellipora striatula, Smitt, Floridan Bryozoa, pt. 2, p. 37. pl. xi. fig. 207. The surface of the specimen from the River-Murray Cliffs is smoother than in the Floridan specimens, and the pores are not so distinct ; but the size is the same, with the oral aperture also 0:06 millim. wide, and there is the same characteristic prolongation of the zocecia, with a small round opening at the end. Loc. Living. Florida, 68 fathoms. 53. ScHIZOPORELLA FENESTRATA, Waters. Schizoporella fenestrata, Waters, Quart. Journ. Geol. Soc. vol. XXXVll. p. 399. A fossil from the River-Murray Cliffs has smaller zocecia and a smaller aperture (0-13 millim.) than the one from Curdies Creek, and should perhaps be called var. minor. It has the surface coarsely granular and covered with pores; the aperture is deeply sunk, and there is frequently on one side a little below the aperture an avicularium with a round aperture, which in some cells is re- placed by a very large raised avicularium covering the whole cell. The opening of this avicularium is triangular, with a tooth from the eross bar, and is situated at right angles to the axis of the zoarium. Loc. Curdies Creek; River-Murray Cliffs. 54, ScuizoporELia Crcrii, Aud. Flusira Cecili, Aud. ; Savigny, Egypte, pl. vii. fig. 3, p. 66. 55. SCHIZOPORELLA PROTENSA, sp. nov, (Pl. VIL. fig. 14.) In Lepralia-form growing on Microporella elevata. Zocecia regu- larly placed, hexagonal, slightly rounded, with a row of large pores round the edge, and with subtriangular avicularium directed outwards, on one or both sides about halfway down the zocecium. Aperture (0-2 millim. wide) rounded at the distal end, below straight with a distinct sinus. Loe. Aldinga. 56. Mastrcornora Dutertrer, Aud. Mastigophora Dutertrei, Hincks, Brit. Mar. Polyzoa, p. 279, pl. xxxvil. figs. 1, 2. _ Specimens from the River-Murray Cliffs and Aldinga are of about the same size as these figured by Mr. Hincks, but the ovicells are 502. A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM rather larger, and these are sometimes pressed in on the front, giving the appearance of a round depression ; but perfect specimens seem to be globular. The surface is smooth and the peristome is but little raised. The oval aperture is about 0°12 millim. with six marginal spines. I feel some doubt about this determination, as the nature of the appendages is not distinguishable, and certainly many cells had neither vibracula nor avicularia. Loc. River-Murray Cliffs, Aldinga. 57. RETEPORA MARSUPIATA, Smitt; Waters, Quart. Journ. Geol. Soc. vol. XxXVli. p. 342, pl. xv. figs. 34-36, pl. xvii. figs. 59, 61, 76, 773; Vol, xxxvill. pp. 275, ee and vol. XRXIX.-p- 439, pl. xu. figs. 13 & 21. An imperfectly preserved specimen from Aldinga was sent over by Professor Tate marked “ R. vibicata, Sturt ;” but it is impossible to make specific comparison with the fossils found by Sturt, and this does not seem to be the &#. vibicata of Goldfuss. The ovicell has a double cleft. | 58. RHYNCHOPORA BISPINOSA, Johnston. See Hincks, Cat. Mar. Polyzoa, p. 385, pl. xl. figs. 1-5. _ A specimen from River-Murray Cliffs has a large avicularium raised as a mucro in front of the aperture, and frequently at the base of this on one side there is a smaller avicularium. Loc. Living: British seas; Mazatlan ; Adelaide ; Victoria Bank, off S.E. Brazil, 33 fathoms (Ridley). 59. CELLEPoRA coronopPus, 8. Wood. Cellepora pumicosa, Linn. (non Busk), Syst. Nat. 12th ed. p. 1286. Cellepora coronopus, 8. V. Wood, Ann. & Mag. Nat. Hist. vol. xiii. p. 13; Busk, Crag Polyzoa, p. 57, pl. ix. figs. 1,2,3; Manzoni, Bry. Foss. Ital. Cont. 4, p. 18, pl. i. figs. 18, 19; Waters, Ann. & Mag. Nat. Hist. ser. 5. vol. i. p. 192. Cellepora tubigera, Busk, loc. cit. p. 60, pl. ix. figs. 8-10. Cellepora gambierensis, Busk, Quart. Journ. Geol. Soe. vol. xvi. p- 261 (named only, no description); T.-Woods, Geol. Obs. in S. Australia, pp. 74 & &5; T.-Woods, Trans. R. Soc. Vict. vi. p. 4, pl. i. fig. 3. Celleporaria gambierensis, Stoliczka, Foss. Bry. der Orakei Bay, p. 141, pl. xx. fig. 7. Although this species is reported to be extremely common in Australia, a badly preserved specimen from Aldinga, which was sent over by Professor Tate marked “ C. gambieriensis,” is the first that I have seen, and as the descriptions laid most weight upon the colonial growth, it was impossible to make any comparisons. It grows in solid round branches about 8 millim. in diameter, and anastomoses regularly. The aperture of the zocecia is round, about 0:13-0:20 millim., with a small avicularium, apparently below the mouth. No zocecial avicularia or ovicells have been found on the specimen. ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 303 Stoliczka (loc. ct. p. 142) suggested that probably the fossil was C. coronopus ; and so far as this specimen permits a judgment, I cer- tainly agree with him. Loc. Living: Coasts of Britain and France; Mediterranean. Fossil: Pliocene: Crag; Pliocene of Italy and Sicily; Mt. Gambier (B.) ; Geelong (Wilkinson) ; Orakei Bay (New Zealand); Aldinga. 60. CELLEPORA AVICULARIS, Hincks. Cellepora Redoute, Aud. in Sav. Egypte, pl. vii. fig. 6, p. 64. Cellepora ramulosa, form avicularis, Smitt, Oefv. Kon. Vet.- Akad. Forh. 1867, Bihang, pp. 32 & 194, pl. xxviii. figs. 202-210. Cellepora avicularis, Hincks, Q. J. Micr. Soc. vii. p. 278 ; Ann. & Mag. Nat. Hist. ser. 3, vol. ix. p. 304, pl. xii. fig. 6; Brit. Mar. Polyzoa, p. 406, pl. liv. figs. 4-6; Norman, B. Assoc. Rep. 1868, p. 308 ; Waters, Ann. & * Mag. Nat. Hist. ser. 5, vol. it. p. 193, pl. xiv. ‘figs. LI ae A specimen from the River-Murray Cliffs apparently grew over the stem of some seaweed, and rises into irregular nodulations,. The zocecia are ovate with an avicularium at the side by the lower part of the oral aperture; oral aperture suborbicular, angular at the proximal edge, forming a sinus; large spatulate avicularia dis- tributed over the zoarium. Ovicell globose with large punctures. The size of the cells, apertures, and avicularia is the same as in my Naples specimens. Loc. Living: British seas; Arctic Ocean; Red Sea; Naples; 10 fathm. Fossil: River-Murray Cliffs, ‘61. CELLEPoRA costaTa, MacG. Cellepora costata, MacG. Trans. R. Soc. Vict. 1869, p. 11. Cellepora retusa, Manz., var. caminata, Waters, Ann. & Mag. Nat. Hist. ser. 5, vol. iii. p. 194, pl. xiii. fig. 1. A small badly preserved specimen from Adelaide is growing on Microporella ferrea, W. This has smaller zocecia than a recent specimen from Glenelg, S. Australia, in which the aperture is 0:13 millim., while in the fossil it is only 0-1 millim. In the fossil no ovicells are preserved, and the avicularia do not rise above the zocecia, whereas in the recent specimen the ovicells are the same as those from Naples, and the avicularia, although they turn more in- wards, closely resemble those from Naples. This I believe is related to Lagenipora spinulosa, Hincks. Loc. Living: Wilson Promontory and Queenscliff, Victoria(MacG.); Glenelg, S. Australia (A. W. W.coll.). Fossil: Leithakalk of Nuss- dorf (Vienna) (A. W. W. coll.), Adelaide. 62. CELLEPORA DIVISA, Sp. Nov. The zoarium is subglobular, 6-8 millim. in diameter. The zocecia . are small and irregular in shape, with a small round aperture 0:13 millim. wide, and inside this there is a plate extending about one third across the aperture (fig. 1). There is a central “ pit” round 304 A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM which the zocecia are formed, and in this respect and the shape and size of the zocecia it much resembles C. fossa, Haswell; but no avicularia are found on the colony. I have a small globular colony (4 millims. diam.) from the Crag of Leiston, with the oral apertures of about the same size, and a similar plate directed inwards. This Fig. 1.—Zowcia of Cellepora divisa, sp. n., showing apertures. (Enlarged 25 diam.) Crag fossil has a rostrum below the aperture with a terminal avicu- larium, and has plain globular ovicells. Possibly this is the armed condition of the present species. Loc. Mt. Gambier. 63, CELLEPORA MAMILLATA, Busk. Cellepora mamillata, Busk, Cat. Mar. Polyzoa, p. 87, pl. exx. figs. 3,4,5; Ridley, Proc. Zool. Soc. 1881, p. 54. Cellepora mamillata, var. atlantica, Busk, Chall. Reps Polyzoa, p. 199, pl. xxxv. figs. 4, 5, 13. In a specimen from the River-Murray Cliffs the zoarium incrust- ing a shell is raised into large prominent mamillations. Oral aperture nearly round, flattened below, about 0-18 millim. diameter. Avicularia projecting above the zoccia, with large triangular man- dibular openings on the median line on the internal aspect. The mamillation of the zoarium occurs in a very large number of Ceéllepore and cannot be looked upon as a character of specific value. C. mamillata only differs from C. pwmicosa, Busk, in the shape of the aperture. Loc. Living: Coast of Patagonia; Victoria Bank, S.E. Brazil; Crozet Island, off Bahia; New Zealand (Hutton) ; Victoria (MacG.). Fossil: River-Murray Cliffs. 64. CELLEPORA ALBIROSTRIS, Smitt. Discopora albirostris, forma typica, Smitt, Floridan Bryozoa, p. 70, pl. xii. figs. 234-239. Cellepora albirostris, Busk, Jovrn. Linn. Soc. vol. xy. p. 347; ‘Challenger’ Report on the Polyzoa, p. 193, pl. xxxiv. fig. 7, pl. xxxv. fig. 3. A specimen from the River-Murray Cliffs is dome-shaped, re- sembling Lunulites. The zoccia are round, much raised, and smooth ; below the oral aperture there are small oral avicularia with rounded openings, but I do not find any vicarious avicularia (ony- chocellaria) ; above the aperture there are two spines; aperture ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 300 rounded on the distal edge, becoming wider on the proximal, which is slightly concave 0:14—0°17 millim. wide. In the recent and fossil spe- cimens there are at the two sides of the aperture small teeth, one on each side directed downwards towards the neural wall. The shape of the operculum indicates the presence of such teeth, but they have been overlooked. The dorsal surface much resembles that of C. biradiata, W., and this species, C. albirostris, C. pertusa, and C. tri- denticulata, are no doubt allied. The specimen that I referred to pro tem. as C. i pe (Journ. Roy. Micr. Sos. vol. ii. p. 392, pl. xv. figs. 6, 8), is C. albirostris, and grows round the stalks of seaweed, rising into ridges with zocecia on each face of the ridge. These have no oral spines, fre- quently the rostrum bifurcates, and ovicells surmounted with small avicularia are supported by the rostrum. Smitt refers to the Floridan specimens sometimes having two spines and sometimes being without; and as this is made a leading distinction between C. albirostris and C. hastigera, I should certainly feel inclined to unite them, for in each colony of C. albirostris there is great varia- tion in the size and form of the rostral process. We see in this species and C. tridenticulata how little importance we should attach to the mode of growth; and among specimens picked up at the same time near the Semaphore, Adelaide, as being the same species, we have found that although they most closely resembled one another in general appearance, they represent Hetero- pora crevicorms, d’Orb., Cellepora albirostris, and C. tridenticulata. Loc. Living: Florida, 25-35 fathm.; Sydney (Sm.); Heard Islands, 75 fathm. (B.); Semaphore, Adelaide (A. W. W. coll.). Fossil: River-Murray Cliffs. 65. CELLEPORA PERTUSA, Smitt. Discopora pertusa, Smitt, Floridan Bryozoa, p. 72, pl. xu. figs. 240, 241. A specimen from Aldinga is irregularly subglobular; diameter 4 to 7 millim. In the shape of the zocecia and of the large oral aper- tures it corresponds with the Floridan specimens ; but in the fossil there are no avicularia, and from Smitt’s figures the avicularia only seem to occur on some of the zocecia. Oral aperture 0°28 millim. Loc. Florida, 35-60 fathm. 66. CELLEPORA PERTUSA, Sm., var. LIGULATA. The zoarium consists of hollow cylindrical branches. The zoccia are ovate, elongate, irregular, with a rounded aperture nearly straight below and slightly contracted at the sides; there is a very minute avicularium below or to the side of the aperture, and besides this there are frequently small ligulate or spatulate avicularia on the zocecia, and here and there an elongate spatulate vicarious avicularium. ‘The oral aperture is 0°12 millim. I feel much doubt about any determination of this form, but in calling it a variety of pertusa the similarity in most points is indi- 306 | A. W. WATERS ON CHILOSTOMATOUS BRYOZOA FROM cated, but the minuteness of the aperture and the avicularia on the front of the zocecia distinguish it. Loe. River-Murray Cliffs. 67. CELLEPORA BIRADIATA, sp. nov. (PI, VII. figs. 11, 12.) In a specimen from the River-Murray Cliffs the zoarium is conical, mamillated, in diameter about 20 millim., and has the general appearance of a large Lunulites. The zoarium is formed by many superposed layers of zocecia. On the dorsal surface there are radiating lines, and when the outer surface is broken away, the walls of a double row of zocecia are seen, and each such double row is separated from its neighbours by septa (fig. 11). Zocecia irregular, subglobular, raised, with the oral aperture rounded on the distal edge, nearly straight on the proximal, forming more than a semicircle, 0-12 millim. wide. Below the aperture, a little to one side, is a small raised avicularium, with the mandibular opening forming a nearly equilateral triangle. In one specimen there are two spatulate avicularia, and sometimes three rudimentary teeth can be distinguished in the oral aperture; but this is excep- tional. Ovicells subglobose, broader than high, smooth, resembling the ovicells of Cellepora ramulosa, L., as figured by Hincks, Brit. Mar. Polyzoa, pl. lii. fig. 8. This and C. compressa, Busk, C. tridenticulata, B., and C. albi- rostris, Sm., all seem closely related. 68. CELLEPORA TRIDENTICULATA, Busk. Cellepora tridenticulata, Busk, Journ. Linn. Soe. vol. xv. p. 347 ; ‘Challenger’ Report on the Poly zoa, p. 198, pl. xxix. fig. 3, plexxxy. fen 117: From the River-Murray Cliffs there is a solid dome-shaped oily formed of many layers, measuring about 25 millim. in diameter, and in a colony from Aldinga the zoarium commenced in a dome shape, then spread out to about 10 centim. in diameter and grew into a solid mass 10 centim. high. The zocecia are irregular, immersed, with the oral aperture straight below, rounded at the distal end, forming a little more than half a circle, and a little way down the aperture on the proximal edge there are three narrow teeth directed forwards. Below the oral aperture there is a small rounded avicu- larium, and there was a spine on each side of the aperture. Oral aperture about 0-2 millim., from which it can be seen that in the fossil it was larger than-in the specimen described by Mr. Busk; but recent specimens from the Semaphore, Adelaide, correspond with the fossil. On the under surface the elongate hexagonal shape of each cell is visible, and there are projections for attachment. Out of several fossil specimens I have only found two with a vicarious avi- cularium (onychocellarium), and in this case it was spatulate, as figured by Mr. Busk. In recent specimens sometimes the avicularium is very small, at others it rises into a large rostral process, aud occasion- ally there are four teeth in the oral aperture. ¢. tridenticulata and C. honolulensis, B., are very closely allied. ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 9307 Loc. Living: Off Cape York, lat. 10° 30’ S., long. 142° 18' E., 8 fathm. (B.); Semaphore, Adelaide CAL, W.). Fossil : Aldinga, River-Murray Cliffs (dome-shaped and incrusting); Yorke’s Penin- sula (irregular cone-shaped) ; Waipukerau (New Zealand), 69. CeLLEPorA Fossa, Haswell, Waters, Quart. Journ. Geol. Soc. vol. xxxvil. p. 343, pl. xviii. fig. 89, and vol. xxxviii. p. 275. From the River-Murray Cliffs there is a specimen about 25 millim. in diameter, with the one surface, which may be called the under surface, flat; the other is slightly rounded. On the flat surface there are about forty well-marked pits and a few smaller ones, Fig. 2.—Zocecium of Cellepora fossa. (Enlarged 25 diam.) Mr. Haswell, in a ‘“‘ Note on a curious instance of Symbiosis ” (Proc. Linn. Soc. N. 8. Wales, vol. vii. 1882), refers-to his discovery of small red Actinids lodged in cylindrical pits in recent Cellepora, and he attributes these pits in C. fossa to a similar parasite. It is therefore extremely interesting to frequently find similar pits in fossil Cellepore. Mr. Busk refers to a perforation two thirds through C. tubulosa, a fossil from Australia, which, however, cannot be identified, as the description only takes cognizance of the mode of growth. The straight edge of the aperture is irregularly rough, but there are no teeth, Loc. Living: Holborn Island. Fossil: Curdies Creek, Mt. Gane bier, River-Murray Cliffs, and Aldinga, 70. CeLLepors Fossa, Hasw., var. MARSUPIATA, Nov. Zoarium subglobular (6 millim. diam.), with a central pit as in C. fossa. In the typical C. fossa, the avicularium is very large, often nearly as large as the oral aperture (fig. 2), so that in badly pre- served specimens the appearance is of one large round aperture with a bar across. In the present variety the avicularium is much smaller, with the avicularian chamber raised, forming a kind. of pouch withasemicircular aperture (fig.3). Surface granular. The oral aperture (0'1—0:12 millim.) is narrower than in C. fossa but is pro- portionately longer ; inside the aperture directed downwards, towards the interior of the zocecium, there is a tooth on each side of the aperture, and sometimes these teeth are continued as a plate round the proximal part of the aperture. In a few cases faint traces of 308 A. W. WATERS ON CH1LOSTOMATOUS BRYOZOA FROM such teeth can be detected in the typical C. fossa, but this is excep- tional. Loc. River-Murray Cliffs. Fig. 3.—Zoecium of Cellepora fossa, var. a (Enlarged 25 diam. ) 71. LexyrHopora HystrIx, MacG. Lekythopora hystrix, MacGillivray, ‘“ Descriptions of New or Little-known Polyzoa,” pt. iii. p. 194, Trans. Roy. Soc. Vict. vol. xix. pl. i. fig. 6; also pt. viil. p. 8, pl. 11. fig. 6 (advance copy). In the growth and the shape of the cells this so much resembles various Cyclostomata that until sections were prepared I did not recognize that it was a Chilostoma; and even after careful examina- tion the fossil remains very incomprehensible, and further study of recent specimens is much to be desired. ‘The state of fossilization is not favourable for studying the minute structure. The zocecia, which are subtubular, open only on one side of the zoarium, and are erect and often more or less in bundles, giving the appearance of Frondi- pora. The small opening on the side of the aperture which MacGillivray describes as an avicularum, is only distinguishable in a few cases. On the front of the zoartum there are a number of globular mamillations, sometimes with a small opening in the centre. These much resemble the enlargements on the front of the cell which Professor MacGillivray describes as ovicells; but these enlargements in the fossil are usually entire, with comparatively large pores on the surface. ‘The solid under surface of the zoarium has a few irregularly scattered large-sized pores. 72. CUPULARIA CANARIENSIS, Busk. Cupularia canariensis, Busk, Q. J. Micr. Soc. vol. vil. p. 66, pl. xxiii. figs. 6-9 ; Crag Polyzoa, p. 87, pl. xii. fig. 2; Manzoni, Foss. Ital. Contrib. i. p. 10, pl. i. fig. 17; Bri. foss. del Mioc. d’Aust. ed Ungh. p. 24, pl. xvii. fig. 56. . Membranipora canariensis, Smitt, Floridan Bryozoa, pt. 2. p. 10, pl. ii. figs. 69-71. Specimens from Aldinga have larger zocecia and larger opesial openings than some recent specimens from Princess Charlotte Bay. In the recent one the sulcate structure of the under surface is very marked ; but upon careful examination faint cross-divisions can also be distinguished, thus separating the dorsal surface into zoecial ALDINGA AND THE RIVER-MURRAY CLIFFS, SOUTH AUSTRALIA. 309 divisions, while in the fossil the dorsal sulci are not very marked, and there are but few pores in each quadrangular division; again they are more numerous in the Charlotte-Bay example. The dif- ference between this and C. guincensis and C. stellata consists in the lamina not extending up to the distal border ; but this is a vari- able character, and probably all three should be united under one name. Loc. Living: Madeira and Canaries; Princess-Charlotte Bay (sent by Mr. Brazier); Florida, common, 10-44 fathm. (Sm.). Fossil: Miocene—Austria and Hungary. Pliocene, Crag—Hills of Pisa, Castelarquato, Asti, Mt. Mario, Rhode Island; Tortonian and Saharian of Reggio (Calabria) (Seg.) ; Aldinga. 73. SELENARIA MACULATA, Busk. Selenaria maculata, Busk, Cat. Mar. Polyz. p. 101, pl. cxvii.; Waters, Quart. Journ. Geol. Soc. vol. xxxix. p. 440, pt. xi. figs. /, 9, and 12. A specimen from the River-Murray Cliffs is about 6 millim. in diameter, and is exactly similar to specimens from Muddy Creek and Bird Rock. The dorsal surface is divided by radiating ridges, between which there are single or double rows of large pores. Another specimen from Aldinga (sent over as Lunulites rutella) has smaller zocecia and very few vibracular chambers, and on the dorsal surface there are, instead of the large pores, long erect tubes, which may serve for attachment. Besides the species named there is a small cylindrical fragment of what I believe is Lepralia (Onchopora) immersa, Haswell ; but with so small a piece, imperfectly preserved, I cannot feel sure of the determination. The collection also contains a Membranipora from the River-Murray Cliffs which belongs to the M.-spinifera group, and another with oval opesia and a small avicularium above the opening, which might be M. levata, Hincks. Upon reexamining the Mt.-Gambier collection I find that a specimen which I thought was Retepora rimata, W., is R. jack- somensis, Busk (‘ Challenger’ Report, p. 125, pl. xxvii. fig. 4). These two species are very closely allied, but the avicularia differ in shape. A further study as to the range of variability of R. jack- soniensis would be of great interest. EXPLANATION OF PLATH VII. Fig. 1. Membranipora rhynchota, Busk. The zocecia on the left have ovicells; — those on the right are without. Monoporelia secangularis, Goldf. From specimen fig. 13. Membranipora aperta, Busk. . Micropora patula, Waters. . Membranipora parvicella, T. Woods. . Microporella elevata, T.-Woods ; showing marginal avicularia. . Microporella magna, T T.-Woods. Q.J.G6.8. No. 163. Z ID OUR o9 bo > 316 ON CHILOSTOMATOUS BRYOZOA FROM ALDINGA, ETC., S. AUSTRALIA. Fig. 8. Microporella pocilliformis, sp. nov. 9. Microporella elevata, T.-Woods ; drawn from the same colony as No. 6. 10. Lepralia confinita, sp. nov. 11. Cellepora biradiata, sp. nov. ; dorsal surface. 12. Ditto, natural size. 13. Monoporella sexangularis, Goldf. ; natural size, 14. Schizoporella protensa, sp. nov. 15. Smittia Tatei, T.-Woods ; natural size. 16. Membranipora temporaria, sp. nov. Discussion. Mr. EtHeriper said the author had done valuable service in de- scribing Polyzoa from various countries, and this contribution would doubtless prove a valuable addition to our knowledge. A ane f XL. PL VOL Oe. Vol. Geol. S Quart. Journ Geo West & Sons et imp. OSTRACODA. IRBECK TA U = OSTRACODA. NS Quart.Jdourn. Geol. Soc Vol. XLE Pl IX. eects Lessurss mene a4 savapre pete ae 22 bets ce atl PURE EC he S| ar Geo.West & Sons del. lith et imp. NN at a ON THE OSTRACODA OF THE PURBECK FORMATION, ole 29. On the Osrracopa of the Purseck Formation ; with Nores on the WALDEN Species. By Prof. T. Rupert Jonzs, F.RS. F.G.8., &. (Read May 13, 1885.) fPriates VIII. & IX.*] ConTENTS. Page §I. Tapecdaoton Ue daigauecle sects catia s'ac duet tae MMMM Rese tte ane ae waters: 311 § II. Ostracoda of the Purbeck Formation.—Sources of Information ... 312 Sir C. Lyell’s woodcuts, and the Diagrams at the Museum of BEACHIEAD GeOlO Ry os. name ace sar pte eee easton anal dah nce 312 In, BOWES S DWOCLGLUBES ...cn.cveccugeeemmnnee es meena tenes nee haa 314 Vertical Sections (Geological Survey) at Durlston Bay, Wor- barrow Bay, Mewps Bay, and Ridgway Hill ..................... 315 H. W. Bristow’s, J. H. Austen’s, and O. Fisher’s Lists of Pur- [25 ESC eR ee oe ey Si: DMN RE sce 2 Seaioee ger tia 315 Fitton and Sowerby in Fitton’s memoir (Trans. Geol. Soc. ser. 2, vol. iv. 1836), and Dr. Fitton’s specimens in the Geological RIC ay 8 WENO UTE tte cae dis tite dentin lain amc junsasagecsemetas = hassades 315 Specimens in the Museum of the Geological Society, Museum of Practical Geology, and British Museum, and communicated FG SLUT SRE Te SP = ee eer Se ee 317 § ITT. Ostracoda of Wealden and reputed “ Wealden” strata ............ 317 immer a ane. Wunmker Species’ \- 2.45.0. 95ei6 , Aha ewas cat «seed len dees 318 Shotover and Netherfield specimens............. Gaetan Sta, aaa 320 Symatyrs@h CYPACH AUSONE 0. cecasscnsenscncnaeterdvnterasdchiens 321 §IV. Catalogue of definite localities and horizons in the Purbeck Formation, WILE, LetE SPEGIes: 133s5....c0cfasciculata. making up the rock. Casts of Cyrene full of Cypride. The rock a mass of Cypridz. 197. Ladydown. See Fitton’s ‘ Memoir,’ &c., pp. 262, 272. fasciculata. “Lady Down. Miss Benett. 9674.” Geol. Soc. fasciculata. “Lady Down in Tisbury. Miss Benett.” With Fish- Pismeulate remains (Sauropsis). Geol. Soe. : ; “Between Dallard and St. Catherine’s Ford. cae ‘ \ ap oe Cypridea granulosa ( fasciculata) is particularly characteristic of this division of the series, and Metacypris Forbesvi is also peculiar to it. Ill. Ostracoda from the Lower-Purbeck Beds. I. Dorser. § 1. Portland. 389. “Purbeck stone, Portland.” Fitton. Geol. Soc. | bononiensis. Marked as containing “C. faba” (=C. valdensis). + ansata. A white limestone. purbeckensis. § 2. Durlston Bay. 366 & | “ Durlston Bay, Isle of Purbeck. Bed No. 9 of Lower 368. Purbeck t. Soft grey Cypris-shales.” purbeckensis ||. Horace B. Woodward, July 1884. t This is the only instance in which I have found Cypridea valdensis in the Pur- beck beds. Some doubtful specimens, however, may be mentioned as occurring in black shales from a pit in Archer Wood, near Battle, Sussex, and in ironstone at Poundsford. z { Mr. Bristow’s list in Damon’s new edition. || Cypris purbeckensis, M. P. G. XB¥, is entered in the Catal, Fossils M. P. G. 1865, p. 254, as belonging to the “ Middle Purbeck” (of Durlston Bay ?), together with Ser- pulites and Archéoniscus ; but this, I think, must be a mistake, for this species and the other fossils here mentioned, for by far the most part, characteristically belong to the Lower Purbeck. It is referred to as “ 17 in O.” Qay-G.8. No. 163. 2A 326 PROF. T. R. JONES ON THE OSTRACODA List of Specimens &c. (continued). | Nos. of the speci- mens in T. RB. J.’s | Collection. Locality. Collector or Museum. Species. § 3. Worbarrow Bay. 371. ‘ Worbarrow Bay. Hard slaty limestone with occasional partings of sandy shale. Hard Cockle-beds.” purbeckensis. _H.B.W. July 1884. 375. ‘‘Worbarrow Bay. Brown Ee San uh \ purbec Wes. § 4, Lulworth. B3 Tiilwortli. «ie, See ee { purbeckensis, _bononiensis. In the ‘ Catalogue of Rock-specimens, Mus. Pract. Geol.’ 1862, p. 141, a piece of “ grey slaty limestone” of the Lower-Purbeck Series, “with pale marly clay,” in the “ Soft Cockle-beds,” and con- taining pseudomorphous casts of salt-crystals, is described as having its “ upper and under surfaces...., as well as the casts of crystals .... thickly covered with Cypris leguminella.” Though these little bodies at first sight closely resemble Darwinula leguminella, they are really minute, subcylindrical, oolitic concretions * composing the rock. They stand out whitish on the surfaces, more distinctly than elsewhere, on account of weathering; in the limestone they have a brownish tint, and under the microscope the cementing matrix is calcareous. Mr. Cunnington has shown me a specimen from Chicksgrove (not far from Teffont), which has these oolitic grains interstratified with a dense argillaceous limestone. In a grey marly limestone from Teffont, with chert, and containing fish-remains (in the Rev. W. R. Andrew’s collections), I have seen a thin layer of similar oolitic granules, some botelloid, but most of them round and ovoid. $5. Ringystead Bay. 376. Ringstead Bay. From H. B. W. July 1884. This is )\ a mass of small roundish granules and Cypride, coated more or less with calc-sinter, including also small tubes (Serpule ?). This is comparable with a } purbeckensis. similar Purbeckian bed near Boulogne, see ‘ Proceed. | Geol. Assoc.’ vol. viii. p. 58, and ‘ Bullet. Soc. Géol. France,’ ser. 3, vol. viii. p. 616. § 6. Ridgway. 67. Ridgway Hill. From the Rey. O. Fisher t, Jan. 1883. purbeckensis. 372. ‘‘ Ridgway Hill, Upway. Middle rock. Soft Cypris- : | limestone.” H. B. W. July 1884. PES 373. “Ridgway Hill, Upway.” H. B. W. July 1884. purbeckensis. 380. “Ridgway Hill, Upway. Dense PW. daly 1884 | purbeck ee * This is a different oolite from that of the specimen no. 384 from Ridgway, p. 327. Tt See the Rev. O. Fisher’s “Memoir on the Purbeck Strata,’ &. Trans. Cambr. Phil. Soe. vol. ix. 1855; Nos. 1 and 2 of the Ridgway List. Given also in Damon’s ‘Geology of Weymouth,’ &. 1860, p. 111. OF THE PURBECK FORMATION. See List of Specimens &c. (continued). Nos. of the speci- mens in T. R. J.’s Collection. Locality. Collector or Museum. Species. 384. ‘“Upway, Dorset.” Marly limestone with shell-grit : and coarse oolite. H. B. W. 1885. {? urbecensis. Il. WiLtsHiRe. § 1. Vale of Wardour. Teffont. In the Quart. Journ. Geol. Soc. vol. x. p. 477, the Rev. O. Fisher * refers to the local species from + purbeckensis. the Lower Purbeck of Teffont. Teffont. Specimen in Mr. W. Cunnington’s Collection, namenoby Brot: BH ODES. f 1) ceteaane eeoee ements purbeckensis. 230. Vale of Wardour. Silicified wood with very fine speci- TMCV OL gaeoe cnr teth cute asa venieaters domed center oasis ences purbeckensis. ( purbeckensis. ee Sans V hlev Oke W ALGO Ua hte sccaeee se weteemanctans cneessh sind ooeges 4 bononiensis. \ ansata. 365. Lowest Purbeck Bed tf, lying on the Portland Limestone \ at Oakley (Wockley) Quarry near Tisbury, in the | Vale of Wardour. A block of this is preserved in the Museum of Practical Geology, Jermyn Street. It has been described by H. W. Bristow, in the ‘Catalogue of the Rock-specimens in the M. P. G.’ ord edit. 1862, p. 139; and it has been referred to by | Prof. J. F. Blake in the Quart. Journ. Geol. Soc. | vol. xxxvi. 1880, pp. 190, 200; by Sir A. C. Ramsay, ibid. p. 236, and by W. H. Hudleston, in the Proc. | Geol. Assoc. vol. vii. 1881, p. 174. | hononiensis. ansata. * T have also received from him (Jan. 1883) C. purbeckensis collected at Teffont by the Rev. W. R. Andrews. + Extract from a paper on ‘The Geology of the Vale of Wardour, by Mr. W. Cunnington, F.G.S., read at the Blackmore Museum, Salisbury. (In a letter from Mr. Cunnington, February 1885.) ‘‘ According to Prof. E. Forbes Cypris tuberculata is found only in the Upper Purbecks, Cypris fasciculata in the Middle, and Cypris purbeckensis in the Lower...... It appears that the Upper Purbecks are altogether wanting in the Vale of Wardour.......... “Tn the year 1851 I had the pleasure of accompanying Prof. E. Forbes and other geological friends in a tour through the Vale of Wardour. Passing down a lane between Teffont and Tisbury, I broke off from the rock at the side of the road, a small piece of stone full of Cyprides; and, showing it: to him, he said, ‘ This is Cyprés fas- ciculata;, within a few yards lower down you ought to find Cypris purbeckensis ;’ and, as he predicted, within the space mentioned, I found the very species. The specimens are now on the table...... As this was Mr, Forbes’s first visit to the spot, the incident affords a striking proof of his geological knowledge.” t Possibly the estuarine Portlandian (succeeding the marine Portlandian), or the “precursor of the Purbecks,” Hudleston, Proc. Geol. Assoc. loc. cit. See also Prof. Judd’s remarks on the passage from the Portland into the Purbeck, Quart. Journ. Geol. Soc. vol. xxviii. 1871, p. 223, and Mr. Godwin-Austen’s Section at Swindon, Quart. Journ. Geol. Soe. vol. vi. 1859, pp. 464-467, also Prof. Blake’s, 2b¢d. vol. xxxvi. The geology of the Vale of Wardour has been treated of by Dr. W. Fitton in his memoir “On the Strata below the Chalk,” &c. Trans. Geol. Soc. ser. 2, vol. iv. 1836, and the Purbeck beds of the district are especially mentioned, thus :—Dallard’s Farm, pp. 250, 260; Dashlet, pp. 250, 260; Chicksgrove, pp. 251, 260; Wockley, p. 252; Teffont, pp. 259, 260; Lady Down, pp. 262, 272. See also the Rev. P. B. Brodie’s papers, Proc. Geol. Soc. vol. iii. 1839, 1842, pp. 184, 780; Quart. Journ. Geol. Soe. vol. x. 1854, pp. 475, 482; and especially the Rev. W. R. Andrews’s memoir, Quart, Journ. Geol. Soc. vol. xxxvii. 1881, pp. 248-253, and Mr. W. H. Hudleston’s in Proce, Geol. Assoe. vol. vii. 1881, pp. 161, &e. 2a 2 _ 328 PROF. T. R. JONES ON THE OSTRACODA List of Specimens &e. (continued). Nos. of the speci- mens in T. RB. J.’s Collection. Locality. Collector or Museum. Species. “ Chicksgrove or Wockley. Bottom of the Cap.” With { purbeckensis. Fish-remains. Geol. Soc. | ansata. § 2. Swindon. 364. Swindon. Collected by the Rev. Prof. J. F. Blake*. { Til. BuckineHAMSHIRE. $1. Whitchurch, &e. 363. South Oving, Bucks. [Boron transiens. retirugata. J. F. Blake (Quart. Journ. Geol. Soc. xxxvi. p. 215). ) 2nomeensis. ansata. 234. “Quainton. Western pit. Pendle.” t Fitton, May oe 18, 1834, vol. 15, p. 122” (notebook 2). See Fitton’s | [amamiensis. _ memoir, p. 290. acd. 235. Quainton. Pendle, with “Mytilus, Cyclas parva, and Cypris.” : Fitton. \ ansata. 939. & purbeckensis, 998 | “Whitchurch.” “ Pendle.” Fitton. ‘“‘ May, 1834, vol. 15.” 4 bononiensis. ; ansata. 226. ‘ Whitchurch.” “224.” Fitton’s memoir, p. 289. ansata. 227. Whitchurch? “1527-1053.” “ C. faba.’ Fitton. purbeckensis. tk i : ; bononiensis. * Whitchurch. 1520. Fitton.” Shell-grit with 4 Cyprids called C. faba. Geol. Soc. 2 DEMIS ansata. purbeckensis. “Whitchurch. Fitton. 1522.” Geol. Soc. 4 bononiensis. ansatd. “Pendle. Whitchurch. Fitton.” Geol. Soe. anaee “Pendle. Whitchurch.” With vertebre of fish, an )\ oblong bivalve, and an impression of a leaf (?). + ansata. Geol. Soe. ) Stewkley. M.P.G. Xs2. Catal. Foss. 1865, p. 253. \! urbeckensis. : : bononiensis, See also Fitton’s memoir, p. 291. ansata. In an interesting section of Purbeck and Portland strata t at the farm called the Warren, 1} mile south of Stewkley Church, which I had the pleasure of examining with Prof. A. H. Green in 1862, I noticed a Cypridiferous shale above the true Portland beds, and below a bed with Yrigonia. Unfortunately I have mislaid the specimens then collected. § 2. Hartwell, near Aylesbury ||. The Pit near the Bugle Inn. 172, 176, 178, 179,184,189, 1914. Soft limestones, marls, and clay. purbeckensis. 179, 180, 1914. Soft limestone, marls, and clays..................00008: bononiensis. 179, 189,191. Soft limestones, marls, and clays ..................06 ansata. 1'73.. “Dense ereeniclays: sf 0.5 .scnar~ sana vans nanede Noa ae ae rugulata. 1805 (Grom bly clayey ccce sec ccee apese ater ate meter pees retirugata. * See Quart. Journ. Geol. Soc. vol. xxxvi. pp. 203-207. See also C. Moore’s remarks on. the section and fossils of Purbeck beds at Swindon, Proc. Geol. Assoc. vol. iv. 1879, p. 543, &e.; and further on, p. 330. _t The “ pendle,” a Purbeckian bed, found in both Bucks and Wilts, consists of a white, grey, or creamy limestone, somewhat argillaceous, generally fissile above and solid below, and contains at Whitchurch rounded whitish particles. It has been found to contain, at places, “ Cyprides,” Modiole, Paludina, Cyclas parva, Planorbis ?, and Potamides carinatus. t See also Fitton’s Memoir, p. 291. || The particulars of the sections of this and the following quarries having been partly mislaid, their more perfect exposition is delayed for some future opportunity. OF THE PURBECK FORMATION. 329 List of Specimens &c. (continucd), Nos. of the speci- mens in T. R. J.’s Collection. Locality. Collector or Museum. Species. § 3. Hartwell—Barnard’s Pit (or “ pit at Barnett’s Close”) *. 162,166.) sf crereeeeeseeeeseeceeestececeetessteceseeseeetsees ae gigs I tee Beaybede: retirugata (vay. rereen MELE COPD SS Li Ee UR ee eRe ts Eta arate textilis, Pl. ix. f, 24). § 4. Hartwell.—Bishopstone Pit (on the road between Bishopstone and Stone). Fitton’s Memoir, pp. 287, 297 (‘‘ Horton’s pits” and “Dr. Lee’s pit,” at p. 297). This is the same as pit “no. 200” on the plan of the late Dr. Lee’s property at Hartwell. Blue clay, with fish-scales (Plewropholis). Fitton’s 238, 241, | Memoir, p. 287. Marked “200” on Fitton’s label. | purbeckensis. 245, See also Brodie’s section of this quarry (near Stone), { bononzensis. Proe. Geol. Soe. vol. ili. 1842, p. 781. §$ 5. Hartwell (other pits). : ae. 4 , J bononiensis. Near Aylesbury ; with Mytilus. My Pile: 1 Peer} * bononiensis. Peloy Mexre ye kry Omvenen Perle, in.) fish vote Geode ss sacadeaetb ee sae ansata. [f. 20). Lees (PE ts 247, 255, 260, 261, Sec HeaR 3502. & purbeckensis? L165. PPE He MERON Ea: ao daot Ma ati at Raat edetv sata tte wes bononiensts. Bach | ansata. Museum. ) rugulata (Pl. ix. i Sart OR DIE te ce Tae GE AL ee 195. rugulata (Pl. ix. f. 17 & 18). 256. Seem w meets ewes Cease reese esr sere ser ses SBSeerene SSSeee bononiensts ? ansata? ( bononiensis. | ansata. [f.21-23), 253. “Last Portland bed.” ......... waa nply Bas fdcoAbteetiwdedicweeses 4 revirugata( PL. ix. .| withan Echino- { derm spine. Pest lee _ purbeckensis. ae el Soft limestones and clay (861) -.....5..5...0:.sesessessecees bononiensis, AE A ansata. 360. Soft friable limestone. { bononiensis. 854. Grey clay eB Vea ae Ee Se ARE ESE ee ansata. 357. Friable shale. “Trigonia; next to Portland.”......... bononiensis, rugulata. In the Lower-Purbeck series the characteristic Ostracods are :— Cypris purbeckensis, Candona bononiensis, Candona ansata, as will be seen by reference to the foregoing local lists for Wilts, Dorset, and Buckinghamshire. At Swindon, however, Prof. J. F. Blake found a “ Purbeck” stratum which has yielded two new * «London University Magazine,’ June 1856, p. 103. 330 PROF. T. R. JONES ON THE OSTRACODA species of Cythere, C. iransiens and C. retirugata. Of these, the latter occurs in the lowest Purbeck beds in two of the stone-pits at Hartwell, near Aylesbury, namely the “ Bugle pit ” and “‘ Barnard’s pit.” A variety, or the male form (rugulata), of C. retirugata, occurs both in the last-mentioned quarry and in similar low Purbeck (if not really estuarine Portland) beds in other pits near by. The mingling of what seem to be freshwater with marine species in these lowest strata is a subject of much interest, and will require further attention and close study of the succession of strata. C. transiens has been found also in white, soft, Portland Stone, from Brill in Bucks. IV. Purbeck Beds near Mountfield and Poundsford, Sussex. The overlying Cypridiferous shales near Mountfield contain Cypridea valdensis, Darwinula leguminella, and Cypridea Austeni (?), and belong to the Wealden series; but the limestones that have been brought up from the old pits at Limekiln Wood, near by, contain Purbeck species, thus :— Sey : granulosa, Sow. 63. Light-coloured limestone ...........-....2:--se0eesste< Ve fasciculata, Forbes.) 25, 286, 312, 346. Solid bluish limestone, apparently composed of Cypridz, and showing them as casts and moulds on the WeRilered SURACES 4.0522. .c. basse ewes seas ec: wee eee punctata ? 307. Blue shale, with a thin layer of the small botelloid oolite which is seen in Purbeck specimens from Teffont, &ec. ...... In the zhale, _Dunkeri? Oyster-bed. Ostracods, chiefly casts, weathered out free... Cythere? &c. In ironstone at Poundsford we find Cypridea valdensis (?), Dar- winula lequminella, and insect-remains. Purbeck beds from the Sub-Wealden Boring at Nether field. 390, 411, 412. Dark grey impure limestones, at 85 feet and 96 | punctata, (oe Os (2) 042 eee Pe coe PN i Onno eaten eae rece aR ce with Chara. V. The late Mr. Charles Moore’s Specimens from the Purbeck Beds at Swindon, Wilts. In the ‘ Proceed. Geol. Assoc.’ vol. iv. 1876, pp. 544-546, there is an account of the late Mr. Charles Moore’s discovery of many fossils in the Purbeck beds in the Great Quarry at Swindon; and among the fossils mention is made of four or five species of Cypris. The Rev. H. H. Winwood, F.G.S., has been so good as to look for these fossils in the Bath Museum; and from among C. Moore’s Upper-Oolite collection he has sent me six little glass tubes con- taining Ostracodal valves. On examination, these prove to be similar to other Purbeck species. Thus :— Tube 59. Cypridea punctata, ordinary; and C. Dunkeri, with very strong beak and notch. C. Dunkeri is much more numerous than the other. About 90 altogether. Tube 60. Cythere 1 ‘etirugata and its var. ru cpulata + ; ordinary; about 60. | OF THE PURBECK FORMATION. Sa Tube 61. Cythere retirugata and its var. rugulata, ordinary ; and one Cypris purbeckensis: 20 specimens altogether. In both 60 and 61 rugulata is more common than the other. Tube 62. Cypridea punctata; very large. Numerous; about 80. Tube 62*. Candona bononiensis and C. ansata (both ordinary), 15; and Cypridea punctata (ordinary), only one. Tube 65. Cypridea punctata, ordinary; and C. Dunkeri, like that of tube 59, more numerous than C. punctata ; about 250 of the two together. Certain strata at Swindon containing ‘‘ Cyprides” are described, loc. cit., as freshwater marls and limestones, 10 feet thick, with depres- sions (‘ pipe-like veins”) in them, containing material derived from the Lower Greensand. Further, they are referred to as chalky limestones, in which are one or two darkish bands of earthy, car- bonaceous marls and loose grits, containing mixed marine and fresh- water forms. C. Moore also remarked that “the chalky limestones or marls contain few remains of recognizable character”; but, to- gether with several smaller derived fossils, he got four or five species of Cypris “from the black bands,” or “ earthy carbonaceous marls and loose grits ” (the “ black carbonaceous friable loam,’ Hudleston, op. cit. p. 548). The specimens in the tubes above referred to are (from both internal and collateral evidence) believed to be Mr. C. Moore’s Swindon specimens. These deposits + were referred to the Middle Purbeck, with some doubt, by Mr. C. Moore; and he suggested that Purbeck beds of older date may have been cut into, disturbed, and mixed up with them. Prof. Morris gave his opinion (p. 547) that these beds ‘‘might be the equivalents of the entire thickness” of the Purbeck series (300 feet at Durlston Bay). Either of these suggestions will account for the occurrence of the Lower-Purbeck species :—retirugata, rugulata, bononiensis, ansaia, and purbeckensis in company with Dunkert and punctata. Had fasciculata turned up also, we should have had a fairly representative and complete group. § V. Conciuston. In conclusion there are fourteen species of Ostracoda in E. Forbes’s three divisions of the Purbeck series of deposits. Five of them occur only in the Lower Purbeck. Of the others, six occur in both the Middle and the Upper. Of the fourteen, five go up into the Wealden, from the Middle and Upper divisions only. See the fol- lowing Table (p. 332). Cypridea punctata for the Upper, C. granulosa ( fasciculata) for the Middle, and Cypris purbeckensis for the Lower Purbeck, are especially characteristic. t At p. 548, op. cit., Mr. Hudleston notes that this “black carbonaceous friable loam” becomes further on a bed of Cerithiwm portlandicum in “ dark friable marly grit,” and “that above this bed the regular Portland Limestone comes on again,” “ Purbeck ” and “Portland” conditions inosculating at this spot. Prof. Blake’s interpretation of the section is different. PROF. T. R. JONES ON THE OSTRACODA 332 "OIVYT "saswayoaq -Wnd “9 YA guepunqe uO ‘yooqan Ff KOMOTT OY} JO OYsILoyourvyO ‘yoodan gy STPPIP, 9 ut ATUO punoy ‘sould ur yuepunqy "MOULUMODUN 40 NT ‘yooqan | ‘(TIMEL) punp2vog Oy} UL pur : rey | APPLIAN 9} JO ostojovavyH | ‘spoq UapTeo AA ayy} JO oOMlOs UT yuRpUNqe ‘yooqang oy} UI old oyyeyy ‘OLOY ‘OAV LOTIVIT ‘OLVYT ‘ALVA TOTJCAT "OLVAT “ood -IN_ OPP, Oy} UI 4sesu0.149 . ‘yooqang toddq ony UL yuULpUNge ATTROLYSLAOVORLVYO, ‘purpougy jo UepTVoAA OY} UL JguBpunqe ‘ooqing oy} UL oane Ata —— "SyALVULOY SE “VOOOVUISC) MWOUTUNG AHL LO SALOMMSNO/T) AV TOY J, ‘TA:S eeeeee ‘hunuiay “NX (, WopTVoAA ,,) "OMAN re CELLO, V1) ‘SI[I}XO} “IBA HHeseemeecrereoces eQoy “BIGMSNA “TBA BOOBOSHOOLOGLIDOOUBI Yay, Ve VENATIOA ster nge eae Nace er re CO ‘suersmeay aloyjAO | Deere: aon SaEsUR teteee se serssssesss SOUO/ ‘SISTIOIMOUOG BUOPUBO TK OK Ck OK Ck * eee sn0u “BSOQOTS “IBA venencee ee eeeeneeoe "20Uu ‘BS00{UOA cotersrse ees s90d0 7 ‘stsuayooqind studto ee ge “aEOOTNISA “TRA SA gn ‘now ‘tiseqaoy stad dovqoyy Break a Byjourtundey VNUTMARGET aes “" "20uU “TIAO ISIE, ooWdAG ‘20u “eyetnurvidtionvd xv (soqangr yovenaposey "IBA “(“Mogy) wsoTnuRas -—— been e ee eeeeeneee "Qow ‘Taoy ung, —— ‘ow “eqounlpe “ea meres Cog) vyepnodeqny naan (saquair) Bsoqqis ‘eA eTereratat “-20u ‘strvorysod ‘tA ——— ——— PIERS TIBHDGA (5. olrtelep) eyeyound pees (WopgtiT) SISUOPTRA EEO ‘gorjolr A pue soroodg OF THE PURBECK FORMATION. 333 § VII. AppEnprx. 1. The Ostracoda of the Wealden Formation. Dorset. Upper Weald. Swanage Bay | Cypridea valdensis lager in some beds, (Punfield Cove); Cythere Fittont together in others. Cypridea spinigera, only in one bed and alone. IsuE or WIiGuT. Upper Weald. Grange Chine, W. of Compton... { Cypridea valdensis. Dunkeri. { valdensis. Upper Weald. Compton Bay ...255. caeesenet Cythere Fittont. _ Cypridea spinigera. ( valdensis. (Upper?) Weald. West of Brook Point ............ \ Cythere Fittoni. | Cypridea Dunkeri. valdensis. (Upper?) Weald. Brixton Bayt eat ls we. te ere - Cythere Fittoni. Cypridea Dunkert. (Upper?) Weald. Shepherd’s Chine ...................+. valdensis. (Upper ?) Weald. Cowleaze Chine ............... eee valdensis. valdensis, | Cythere Fittont. Upper Weald. Atioriiold:) “2.2 ction nt aseghereens.© 4 Cypridea spinigera. Dunkert. | Darwinula lequminella. ( Cypridea valdensis. | spinigera. Upper Weald. Sandown Bayqe ee scccscsests staves: 4 —— Dunkeri. | Cythere Fittont. \ Darwinula lequminella. SUSSEX. : Cypridea valdensis. Weald Clay. Pulborough (railway) ............ Crihe : Ties i. Weald Clay? Pallingham, W. Sussex.............-. Fittoni. Weald Clay. Petworth (Sussex marble)............ Cypridea valdensis. Tunbridge- Northland shale-pit, near J ree Wells Sand. Chripp’s farm and Cuckfield... eat Tunbridge- Between Ansty Gate and Slough valdensis. Wells sand or Green, N.W. of Cuckfield ; tuberculata. clay in it. POMIMBAMWELL | 5.0: . oe 0°66 Titanic acid ...... 0°380 Water. of xen 0:540 0:60 0°626 0:200 0-21 0-719 a 100-172 100716 101339 101:201 10144 99°738 I. Analysis by Heddle of an altered diallagic augite of green colour, specific gravity 3:529, from Hart o’ Corry, Cuchullin Hills, Skye (Trans. Roy. Soc. Edin. vol. xxviii. (1879) p. 479). II. Analysis by Haughton of augite from Loch Scavaig, Skye (Dublin Quart. Journ. Geol. Soc. vol. v. (1865) p. 95). III. Analysis by Heddle of greyish green altered diallagic augite from Corry na Creech, in the Cuchullin Hills, Skye, sp. gr. 3°329 (doc. cit.). IV. Analysis by Heddle of brownish-green diallagic augite from Drum-na- Rabn, in the Cuchullin Hills, Skye, sp. gr. 3°335. V. Analysis by Vom Rath of diallage from Skye: see Rammelsberg, Hand- buch der Mineralchemie, Ist ed. (1860) p. 465. VI. Analysis by Heddle of dark-green diallagic augite from Loch Scavaig, Skye, specific gravity 3°321 (Joc. cit.). (Iron estimated as ferrous oxide.) These analyses show that the black augite, which is the most common constituent of the gabbros of the Western Isles has a proportion of ferrous oxide, varying from 9 to 14 per cent., while that of the green variety is only about 5 per cent. The lime averages 20 per cent.; but the proportions of alumina and magnesia are somewhat variable. The black varieties occur usually in crystals, which are sometimes of large size; the green varieties also form © similar crystals but sometimes occur in more or less rounded grains. The rhombic pyroxenes are very frequently present in these rocks, but are in almost all cases subordinate to the monoclinic forms. Owing to the confusion which has arisen with respect to the former group of minerals, it will be necessary to discuss at some length the question of the varieties which they present in the Western Isles of Scotland. The minerals belonging to the group of the rhombic pyroxenes which were first made known by mineralogists, and were described under the names of hypersthene (paulite), bronzite, diacla- site, and bastite, are all, as we shall show hereafter, in a more or less altered condition—the rhombic pyroxenes being remarkably subject to changes of several different kinds. But in the year 1855 Kengott discovered an unaltered mineral of the group, to which he gave the name of enstatite *, and in 1862 Descloiseaux demonstrated that it crystallizes in the rhombic system. Shortly after this period other forms of unaltered rhombic pyroxenes were discovered—proto- bastite by Streng {, meteoric enstatite by Rammelberg § and Story- * Sitzungsb, Akad. Wien, vol. xvi. (1855) 162. t Bull. Soc. Geol. Fr. ser. 3, vol. xxi. p. 135. ¢ Neues Jahrb. fiir Min. &c. 1862, p. 513. § Monatsber. d. Akad. Berl. 1861. OLDER PERIDOTITES OF SCOTLAND. 369 Maskelyne, * amblystegite by Vom Rath‘, and a similar mineral from Mont Dore by Descloiseaux f. The minerals found in an unaltered form at these different localities were at first regarded as being excessively rare. But in 1879 Prof. Fouqué showed that the lavas of Santorin contain in great abundance an unaltered rhombic pyroxene which he referred to hypersthene§. In 1883, Mr. Whitman Cross demonstrated the existence and wide distribution of a large and important class of lavas, distinguished by the presence in them of a rhombic pyroxene which he also referred to hypersthene |}. Inthe same year Mr. Teall _and Dr. Petersen pointed out that certain British rocks from the Cheviot Hills contain the same rhombic pyroxene 4, and these, as shown by the former author, are of especial interest as being of pre-Tertiary age. Subsequent observations have shown these rhombic pyroxenes to be among the most widely distributed of the rock-forming minerals. Much attention was directed to them as constituting an important constituent of the pumice thrown out by Krakatoa during its last great eruption; and they have been found in the lavas of South America, Java and Sumatra, Japan, the Philippine Islands, and many other volcanic districts. Nor are the rhombic pyroxenes less common among the plutonic than among the volcanic rocks. In the Schemnitz district the Ter- tiary diorites and quartz-diorites ** frequently contain a considerable proportion of the rhombic pyroxene, which, as in the associated lavas, has been generally confounded with the hornblende. Teller and Von John have described an interesting series of rocks of the same class from the Tyroltt, and the diorite of Penmaenmawr has been shown by Rosenbusch and others to be an enstatite-diabasett. The rhombic pyroxenes are bisilicates of magnesia and iron (MgO, FeO) Si0,, in which the relative proportions of magnesia and iron may vary to almost any extent. Lime is often almost wholly absent, but appears to be capable of replacing, perhaps to a limited extent, the other bases. It is well known that the colour, the physical properties, and the optical constants of varieties of the augites, the micas, and other similar groups, are modified in the most remarkable manner by the quantity of ferrous oxide or other bases in their composition. But in the group of the rhombic pyroxenes the variations in character dependent on composition are of the most extreme kind. At one end of the series we have enstatite proper, a colourless mineral without trace of dichroism ; but as the magnesia is replaced * Trans. Roy. Soe. vol. clx. p. 204. + Poggend. Ann. (1869), exxxviii. 531. t Manuel de Minéralogie, tome. ii. (1874) p. xviii. § Santorin et ses Eruptions (Paris : 1879). || Bull. U. S. Geol. Survey, no. i. “| Geol. Mag. Dee. ii. vol. x. (1883) p. 346. J. Petersen, Mikroskopische sund chemische Untersuchungen. am Enstatit-Porphyrit aus den Cheviot Hills, (Kiel, 1884). ** See Quart. Journ. Geol. Soc, vol, xxxii. (1876) pp. 292-325. tt Jahrb. k-k. geol. Reichsanst. vol. xxxii. (1882) pp. 589-584. tt Die massigen Gesteine, p. 352. 370 PROF. J. W. JUDD ON THE TERTIARY AND to a greater extent by ferrous oxide, the mineral becomes of a more and more pronounced brown tint with marked pleochroism. With the highest percentage of iron the mineral assumes a very dark colour, and when examined in thin sections exhibits the most startling pleochroism (a, brilliant red; 6, duller red; ¢, bright green). ; There has arisen much confusion as to the names which should be given to the different varieties of the rhombic pyroxenes. Most authors call the non-ferriferous varieties “enstatite,” the more ferriferous kinds “‘ bronzite,” and still more highly ferriferous forms “hypersthene.” ‘Tschermak has proposed that varieties with less than 5 per cent. of ferrous oxide should be called enstatite, those with between 5 and 15 per cent. bronzite, and those with more than 15 _per cent. hypersthene*. The strict application of this rule would, however, necessitate a chemical analysis in each case before the species or variety could be determined. As a matter of fact, no two petrographers are agreed as to the - limits between enstatite and bronzite, and between the latter mineral and hypersthene. Thus the mineral of the andesite of the Cheviot Hills, regarded by Mr. Teall as hypersthene, is, by Dr. Petersen, who carried on his investigations in Prof. Rosenbusch's laboratory, classed as bronzite ft. The similar mineral found in the pumice of Krakatoa is called hypersthene by many authors and bronzite by others. The minerals classed as enstatite, bronzite, and hypersthene respectively by Rammelsberg { do not conform to the rule laid down by Tschermak as to the chemical composition of these varieties. The gabbros and peridotites of the Western Isles of Scotland contain all the varieties of the enstatite group, in both their altered and their unaltered forms; and these permit a careful study of the whole series of minerals. Through the replacement, to a varying extent, of a part of the magnesia by ferrous oxide, very distinct varieties are produced ; but, inasmuch as the crystalline form remains the same, it will be convenient to treat the rhombic pyroxenes like the monoclinic pyroxenes (“augites”), and give them a common name. I think there can be no doubt that the common name for these rhombic pyroxenes should be “ enstatite,” for this was the first wnaltered rhombic pyroxene which was detected and described by mineralogists. I believe that this is also the view taken by Prof. Rosenbusch. As, however, the variation in the relative proportions of magnesia and ferrous oxides in these minerals leads to such startling differences in their appearance and optical properties, it may be necessary to use a number of varietal names—like those employed in the case of the monoclinic pyroxenes—diopside, common augite, and heden- bergite. As the enstatites were till quite recent years entirely unknown to mineralogists in their unaltered forms, a difficulty arises in selecting * Tschermak, ‘ Lehrbuch der Mineralogie’ (1884), p. 436. t See Geol. Mag. Dec. iii. vol. i. (1884) p. 227. + Handbuch der Mineralchemie, 2nd ed. 1875, pp. 382-385. OLDER PERIDOTITES OF SCOTLAND. ‘ 371 appropriate names by which to designate the several varieties. The modifications of the ferriferous enstatites known as bronzite and hypersthene (paulite) respectively, are, as I shall show hereafter, alteration-products, and the structures which characterize them are by no means rigidly confined to varieties of a particular chemical composition. The unaltered crystals of the rhombic pyroxenes differ so strikingly in their appearance and optical properties from those of the same composition in an altered state, that it is misleading to designate them by the same varietal name. Possibly the difficulty may be got over by following the example set by Streng in the case of bastite, and calling the unaltered forms of the minerals bronzite and hypersthene respectively proto-bronzite and proto-hypersthene. Accepting also the ordinary convention, that the name bronzite belongs to the less ferriferous, and the name hypersthene to the most ferriferous varieties, we may then perhaps indicate the chief types of the wnaltered rhombic pyroxenes as follows :— (1) Non-ferriferous enstatite (enstatite proper) containing less than 5 per cent. of ferrous oxide. A colourless or nearly colourless mineral destitute of pleochroism. Hardness 5 to 5:5. Specific gravity 3:1 to 3-2. (2) Ferriferous enstatite (proto-bronzite). With a percentage of ferrous oxide ranging from 5 to 15. Pale coloured, with feeble pleochroism. Hardness about 5:5. Specific gravity 3-2 to 3:3. (3) Highly ferriferous enstatite (proto-hypersthene). With a percentage of ferrous oxide ranging from 15 to 25. Darker coloured, with strong pleochroism, Hardness about 6. Specific gravity 3:3 to 3°4. (4) Excessively ferriferous enstatite (amblystegite). With a percentage of ferrous oxide ranging from 25 to 35. Dark coloured, with intense pleochroism (colours from deep red to vivid blue-green), Hardness 6 to 7. Specific gravity 3:4 to 3:5. While the crystalline forms and the goniometric measurements show no differences in these several varieties, the positions of the optic axes and other characters undergo great modifications ac- cording to their chemical composition. The last named of these varieties of the enstatite group has not received the attention which it deserves. I have recently found that it occurs by no means rarely as a rock-constituent. Not only is it found, both in its unaltered and in its altered state, in the gabbros of the Western Isles of Scotland, but it occurs in the Newer Paleozoic lavas of Forfarshire and in the diorites of western Sutherland *. It is a widely distributed mineral, for I have found it in rocks from Norway, Saxony, southern India, western Africa, and the Solomon Islands, forming an important constituent of gabbros, diorites, quartz-diorites, andesites, and certain interesting ultra-basic rocks, while it appears to be almost always present, * [I am indebted to my friend Mr. Teall for calling my attention, since the reading of this paper, to the rocks of this and several other localities in which the mineral in question occurs. | 372 mn PROF. J. W. JUDD ON THE TERTIARY AND sometimes in considerable quantities, in the so-called trap-granutites, the diallage-granulites, and other similar rocks all over the globe. The analyses which have been made of these excessively ferriferous enstatites are as follows :— 18 II. IIT, Silica wi jake scutes < 49°80 48-2 51°348 A NUSTTRVTI fc Sten oo in 5:05 Ferrous oxide ......... 25°60 28°4 33°924 Manganous oxide ... 52 Magnesia............++- 17-70 16-7 11-092 lime: P .s3e-.saaeeeeeee 0-15 15 1:836 VW ALOR cnceis cits osteoma | 0-500 98°30 100°0 98-700 I, Is the analysis by Vom Rath of the original “amblystegite” of the Laacher See. (Pogg. Ann. exxxviili. (1869), p. 531.) ‘ : II. Is an analysis by Laurent of the dark-coloured enstatite found in cavities of a rock enclosed in the trachyte of the Rocher du Capucin, Mont Dore, quoted by Descloiseaux (Manuel de Minéralogie, tome ii. p. xviii.). III. Is the analysis of the altered form of the same mineral, which will be referred to hereafter as occurring at Loch Coruiskh, in Skye. The analysis was. made by Muir and published by Thomson (‘Outlines of Mineralogy,’ 2nd ed. (1822), vol. i. p. 202. Although Prof. Vom Rath withdrew his name of “ amblystegite ” when he found from Von Leng’s researches that all the planes of its crystals were represented in the enstatite of the Breitenbach meteorite *, yet if it be necessary to have a varietal name for these excessively ferriferous and strongly pleochroic enstatites, it would seem desirable to revive this term rather than to invent a new one. The amblystegites differ from the ordinary hypersthenes in their unaltered state (proto-hypersthenes) quite as strikingly as do the latter minerals from the unaltered bronzites (proto-bronzites), or as these last do from the enstatites proper. In microscopic sections of rocks the wonderfully vivid pleochroism, which gives rise to colours varying from a rich garnet red to a vivid blue-green, is its most striking characteristic, and serves to distinguish it from all other rock-forming minerals. The only other rhombic mineral with characters which at all approach it is andalusite ; but in practice the distinction of these two minerals is perfectly easy. Among the remarkably fresh minerals of the Tertiary gabbros and peridotites it is possible to recognize all the varieties of the enstatite roup. 4 ee the island of Rum, we find a perfectly colourless rhombic pyroxene, occurring in irregular grains with a colourless olivine and the brilliant green diopside already described. In its perfectly fresh condition this enstatite can only be discriminated from olivine, also a rhombic mineral, with the greatest difficulty. The fine striation relied upon for the distinction of the two species is a * Neues Jahrb. fir Min. &c. 1871, p. 642. OLDER PERIDOTITES OF SCOTLAND. 373 result of alteration, and is not found in perfectly fresh forms of the mineral. In some cases | have only been able to verify the presence of enstatite by a micro-chemical method. In thin slices and in the powder of the rock the olivine is attacked by long digestion in strong hydrochloric acid, while the enstatite remains unchanged. In other districts of the Western Isles of Scotland we find more ferriferous varieties of enstatite which must be referred to proto- bronzite and proto-hypersthene. Usually, these are in a more or less © altered condition. In very few cases, so far as I have seen, is the enstatite the principal pyroxenic constituent of the rock, but it is subordinate to the augite. In small patches of these rocks, how- ever, the augite may become subordinate to the enstatite, while occasionally the former mineral may be altogether wanting, the rock thus passing into a norite or hypersthenite. Occasionally the dark colour of the mineral, when seen in the thinnest sections by transmitted light, and its strikingly vivid pleo- chroism, indicate that we are dealing with the excessively pleochroic enstatite, amblystegite (see Pl. XI. fig. 7). That Macculloch was acquainted with the altered forms of the enstatite in these rocks, I have the clearest evidence. A specimen given by Macculloch to the late Mr. Majendie passed into the hands of Mr. Warington Smyth, and by him was placed in the collection of the Normal School of Science and Royal School of Mines. An examination of the optical properties of this specimen shows it to be a rhombic and not a monoclinic pyroxene. Intergrowths of the monoclinic and rhombic pyroxenes occur not unfrequently in the gabbros and peridotites of the Western Isles of Scotland, and crystals of the one mineral are sometimes found enclosed in the other. I have not, however, detected examples of the twin-intergrowths of the two minerals described by Trippke *. The Olivines of the gabbros and peridotites of the Western Isles of Scotland appear, like the associated augites and enstatites, to belong, in some cases, to the most highly ferriferous varieties. Seen in thin sections under the microscope, these olivines are often found to be by no means colourless, like most of the olivine of basalts, but exhibit a yellow tint similar to, but not so intense as, the tint of the fayalite in eulysite. Such deep-coloured olivines are abundant in the Shiant Isles. Some of the olivines of these rocks are perfectly fresh and un- weathered, but occasionally the mineral shows incipient traces of serpentinization along its cracks. Occasionally another kind of change has taken place resulting in the mineral acquiring a yellow tint along its fissures, which causes it to assume the colour and aspect of chondrodite. Similarly altered forms of olivine from the Kaiserstiihl have received the names of “ chusite ” and “ limbelite ”. An analysis of this curiously altered olivine from the summit of Halival in the island of Rum, was made by Dr. Heddle and is as follows (its specific gravity was found to be 3:°327) :— * Neues Jahrb. fiir Min. &ec. 1878, p. 673. Tt Mineralogical Magazine, vol. v. (1884) p. 16. Q.J.G.8. No. 163. 2D 374 PROF. J. W. JUDD ON THE TERTIARY AND Siliea feee ard ss JI eee 38-006 Alumnae. . os... Ue 0-286 Permefoxide 2...) Ao eee 2:933 INEELOUSHORING . . os ’aee eee 18-703 Manecanons oxide: >. 22257 ees 0°100 me Pos. oo eee 0-336 Maonesia “. 2 LEE eee eee 38000 Water 2). - tue Ee eee 1-587 ~ 99-945 This analysis indicates a very ferriferous olivine approaching in composition to the variety known as hyalosiderite. The Spinellids—Among the essential minerals of these rocks are the minerals which have been grouped by Fouqué and Lévy under the convenient name of the spinellids, namely magnetite, chromite, and picotite. These minerals, which are isomorphous, have now been shown to pass into one another, by insensible gradations as the proportion of chromic acid varies*. The first is opaque, the two others more or less translucent and of a brown colour. Magne- tite is the mineral which is usually found in the gabbros; chromite and picotite in the peridotites. Tt may be mentioned that, as has been proved by Dr. Hodgkinson, of the Normal School of Science, all these rocks contain copper. It is probable that nickel and cobalt are also present in varying quantities, as well as chromium, manganese and iron; but in ordinary analyses no attempt is made to isolate the oxides of these metals. Biotite—represented usually by a highly ferriferous and very dichroic variety, is among the most common of the accessory minerals of these rocks ; in some cases it becomes so abundant as to deserve to be regarded as an essential constituent of the rock. Metallic Iron.—By the employment of Prof. Andrew’s method, Mr. J. T. Buchanan has succeeded in proving that some of the iron in the gabbros of the Western Isles of Scotland is in a metallic condition. § 4. Tor CHANGES WHICH THE MINERALS OF THESE RocKS HAVE UNDERGONE AT Great DEPTHS FROM THE SURFACE. The great intrusive masses of the West of Scotland are of especial interest to geologists, inasmuch as they afford us an opportunity of studying the conditions assumed by the same minerals under varying conditions of depth and pressure. The intrusions of basic rocks in Mull, Ardnamurchan, Rum, and Skye were originally of very different dimensions, those of Skye and Ardnamurchan being the largest, that of Mull coming next in size, * Renard, Rep. Voyage H.M.S. ‘Challenger,’ vol. ii., Narrative, “On the Petrology of the Rocks of St. Paul,” p. 10; Wadsworth, Mem. Mus. Comp. Zool. Harvard, vol. xi. (1884) p. 176. OLDER PERIDOTITES OF SCOTLAND. BE while that of Rum is the smallest among the principal volcanic centres. Of still smaller intrusive masses, however, we have many examples, among which may be specially mentioned those of Sarsta Beinn in Mull, and the Shiant Isles, north of Skye. These intrusive masses are fully exposed to our study, even their central portions being laid bare by denudation; and the results obtained by a comparative study, by the aid of the microscope, of examples derived from corresponding portions of masses of different size and of different portions of same mass, are of very great interest. If my interpretation of the geological structure of the district be correct, it is a necessary inference that while the rocks of the Cuchullin Hills of Skye about Loch Coruiskh, and those forming the western extremity of Ardnamurchan, once existed at a great depth from the surface of the voleanoes of which they formed a part, the similar rocks forming the mountain masses of Mull and Rum existed at a smaller depth and under less pressure. Now I shall show that the several minerals of these rocks, when they have formed parts of masses at great depths from the original surface, often exhibit very striking and suggestive differences in their characters from. those which have existed at smaller depths. It will further be demonstrated that a precisely similar series of differences can be traced when the several minerals are followed from the more superficial to the more profound portions of each intrusive mass. We shall describe minutely these changes in the case of each of the minerals forming these rocks. In these Tertiary rocks the question is fortunately not complicated or obscured by alterations which have been set up by weathering action; for, as a rule, the minerals are strikingly fresh and unaltered. The Felspars.—The felspars of the more superficial portions of the intrusive masses, and also those in the smaller intrusions and apophyses, are usually remarkable for their strikingly clear and fresh appearance. Under the highest powers of the microscope they are seen to be traversed by many fine cracks, while a few cavities, some of which contain liquids with moving bubbles, are scattered through them. In such cases it may perhaps be inferred that the cavities were formed during the original development of the crystal, and that the cracks are due to the contraction of the mass during its cooling from its original high temperature. In the felspars of rock-masses which were originally more deeply seated, this perfect clearness seems to be quite lost. Cavities, some of which contain liquid with spontaneously moving bubbles, are present in enormous abundance. Prof. Zirkel has already re- marked on the extraordinary abundance ‘of such enclosures in the felspars of the gabbros of Mull*. What is of especial interest however, is the fact that these cavities in many cases are seen to lie in fissures, or in bands parallel to fissures, in the crystal, and to be connected by minute ramifying tubular processes. In many * Zeitschr. d. deutsch. geol. Gesell. vol. xxiii. (1871) p. 59. ©) Qn2Z2 376 PROF. J. W. JUDD ON THE TERTIARY AND cases, where no fissures can be detected, we find the crowding of cavities along bands similar to those which accompany the actual cracks. The explanation which I would propose to account for these interesting appearances is as follows:—When any part of a crystal is subjected to abnormal strain (and that such strains, re- sulting eventually in the fracture of the crystals, must be constantly set up in rock-masses is evident), then, according to a well-known physical principle, solvent action will be promoted along such bands of strain, and cavities containing liquids will be formed. Subse- quently, and perhaps partly in consequence of the formation of the numerous cavities, actual rupture may take place along this band, which was first a plane of strain, and which, by the solvent action, has been converted into a plane of weakness in the crystal. This explanation also accounts for the fact that the same band of cracks may be found traversing a number of adjacent crystals in a rock. Similar facts have been noticed by Vogelsang, Kalkowsky, Jullyan, Phillips, and other authors (see Pl. X. fig. 2). In some cases the liquid-enclosures are so numerous that the supersaturated solutions in them can be detected by chemical methods. If a crystal full of liquid-enclosures be carefully washed and, after being crushed, treated with distilled water, the liberated sulphates and chlorides will give distinct precipitates with chloride of barium and nitrate of silver. In many cases the enclosures are now seen to be filled up with solid substances, as was pointed out to be the case in the rocks of Brittany by Mr. C. Whitmen Cross * (PI. X. fig. 3). At still greater depths, as m the rocks of the Cuchullin Hills and the western extremity of Ardnamurchan, a more or less complicated avanturine structure is exhibited by the felspar. Minute black rods and plates are seen to be developed along one, two, three, four, or even more planes within the crystal. The planes along which these enclosures are formed appear to be parallel to the macropina-~ coid, the brachypinacoid, the two prism-faces and the basal plane (see Pl. X. figs. 4,5, 6); and the planes exhibiting these pecu- liarities appear to be affected in the order in which we have named them. The dimensions of these brown rods and plates, enclosed in the felspar crystals, vary within very wide limits. Occasionally they are sufficiently large to be seen by the naked eye; usually they are of microscopic dimensions, while they sometimes require the use of the very highest powers to discriminate their forms and characters. In Ardnamurchan and Skye we find examples of gabbros in which the felspars exhibit a brown tint, and in thin section the colour of the crystals is seen to be due to the existence of nebulous masses of foreign materials distributed irregularly through them. The highest microscopic objectives at my command only just serve to partially resolve these nebulous masses into series of rods and plates, arranged along certain planes within the crystal, and only distinguished from those already described by their smaller dimen- sions (see Pl. X. fig. 7). * Min. und petr. Mitth. vol. iii. (1880) p. 374. OLDER PERIDOTITES OF SCOTLAND. ott From these inclusions, which are of such minuteness as only to be imperfectly seen with the highest powers of the microscope, it is easy to make the transition to others which are absolutely ultra- microscopical, but which can be detected by the effect which they produce on the light-waves that traverse the crystal. In this way we are led to the understanding and interpretation of another peculiarity possessed by the felspars in the most deeply seated masses, which is especially worthy of notice. Such felspars not unfrequently display the chatoyant effects so characteristic of some of the labradorite from Labrador, while the felspars formed at less depths never exhibit this peculiarity. According to Breithaupt, the labradorite exhibiting a play of colours has a different density from the varieties without that peculiarity ; and Von Bonsdorf has shown* that while the former has a percentage of silica of 57, the latter has one of only 52. The researches of Reusch7, Schrauft, and many other investigators have shown that this play of colours is due to a series of thin plates, developed along certain planes within the crystal. These plates appear to be of ultra-microscopical dimensions, but by producing interference give rise to the exquisite play of colour exhibited by brachydiagonal sections of the crystal when held in certain positions. Although it is impossible to trace the structure to which this peculiarity is due by means of the microscope, yet the circumstance of its being exhibited only in the felspar of deep-seated rocks is of great significance when considered in connexion with the other phenomena which we have just described. By the study of a large number of examples, it is clearly seen that these changes are quite independent of the passage through the erystals of water from the surface, which produces kaolinization, and sometimes leads to the penetration of serpentinous and other decom- position-products, along lines of fissures into the interior of the felspar erystals. These and other important alterations which have been superinduced in the felspar-crystals of these deep-seated rocks, sub- sequently to their original formation, we hope to discuss in a future paper. The different changes we have been describing, like the analogous ones in the pyroxenes and olivines, are, however, clearly related to the depth from the surface at which the rocks were originally situated, the greatest change being in every case displayed by the most deeply seated rock-masses. The Pyroxenes.—Both the monoclinic pyroxenes (augites) and the rhombic pyroxenes (enstatites) exhibit in a very striking manner the effects of alteration when they form parts of rock-masses orginally situated at great depths from the surface. By the old German miners the name of “Schiller-spar” was given to those mineral substances which exhibit a “Schiller” or sheen, 7.¢. a submetallic reflection when the crystal is held in certain positions. Freiesleben and the early German mineralogists * Jahrb. fir Min. &c. (1838) p. 681. +t Poggend. Ann. vol. exvi. &e. { Sitzungsb. der k. k. Akad. Wien, vol. lx. (1869). 378 PROF. J. W. JUDD ON THE TERTIARY AND adopted the term “‘ Schiller-spar” as the name of a mineral species ; but Breithaupt, Haidinger, and Haiiy, by dividing the Schiller-spars into species like diallage, diaclase, bastite, and hypersthene, showed that they had recognized the fact that many different minerals may exhibit the peculiar reflection of Schiller-spar. It is now recognized that many varieties, both of the monoclinic and of the rhombic pyroxenes, under certain circumstances, may exhibit this peculiar appearance. The different kinds of pyroxene, with the corresponding “Schiller” varieties, may be classed as follows :— Unaltered forms. “ Schiller ” varieties. More altered form. Enstatite proper. Diaclasite ? Tale (?) ’ Enstatires, | Proto-bronzite. Bronzite. Basie Rhombic. , Proto-hypersthene. Hypersthene. \ rar [ See Hypersthene. ae Diopside. , : ieee | Ava eS Ronen Seoaeaee : : | Hedenbergite. seudo-hypersthene. maragdaite, Mc. The ‘Schiller ”-varieties of pyroxenes, when examined in thin sections under the microscope, are seen to owe their peculiar appear- ance to the presence in them of a great number of enclosures, in the form of thin plates or delicate rods, arranged along one or more sets of parallel planes within the crystal. When the crystals are held in certain positions, the numerous enclosures, which exhibit various grey, yellow, and brown tints, and possess a submetallic lustre, reflect the light traversing the transparent portions of the crystal, and by this reflection give rise to the “ Schiller” phenomenon. The crystals of augite like those of felspar exhibit the first traces of alteration along the incipient cracks, whether due to cleavage or other causes, which traverse them. Along these incipient cracks and in bands parallel with them, cavities make their appearance, some of these cavities containing liquids with moving bubbles, while others enclose solid materials (see Pl. XI. fig. 1). While the augites of the superficial rocks contain but few of these enclosures, they become exceedingly numerous as we trace the augite crystals to greater distances from the original surface. It is therefore impossible to doubt that these cavities formed in networks along the incipient cracks of the crystal are, like the similar ones de- scribed in the felspars, of secondary origin. They have probably been formed by the solvent action of the fluids which now fill them, acting under the enormous pressures consequent on their original depth from the surface. Both the green augites (diopside) and the black varieties (common augite) of the Western Isles of Scotland are found, when traced into the more deeply seated masses, to pass gradually into the “ Schiller ” varieties known as diallage and pseudo-hypersthene. That this is the result of a secondary modification is proved by the fact that the alteration of the crystals is seen in many cases to be confined to their outer portions, so that a nucleus of ordinary augite is sur- OLDER PERIDOTITES OF SCOTLAND. 379 rounded by a shell of diallage (see Pl. XI. fig. 3); in other cases the alteration of the angite into diallage is seen to take place along cracks, due to cleavage or other causes, which intersect the erystal (see Pl. XI. fig. 5); in other cases, again, the alteration into diallage is found to occur in irregular patches within the augite, though the cause of the distribution of these altered patches may not be manifest from a study of the thin section. Although the alteration of the augite may be set up along the cleavage-cracks of the crystals, yet the position of the brown enclosures bears no relation to the principal (prismatic) planes of cleavage in the mineral. On the contrary, the enclosures appear to be developed in planes parallel to the orthopinacoid planes, in which only a very imperfect cleavage exists in augite*. In the island of Rum, the augite, though exhibiting the first traces of the development of the structure which is characteristic of diallage, is seldom so far altered as to deserve being called by that name. In the larger igneous masses of Mull, the augite in all the central portions is in the condition of diallage, as was pointed out by Zirkel. Between rocks in which the augite is entirely unaltered, and those in which it is completely transformed into diallage, every possible transition may be found. In the central portions of the largest intrusive masses, those of Skye and Ardnamurchan, the augite exhibits a still further modifi- cation. In addition to the enclosures along the planes parallel with the orthopinacoid, other enclosures make their appearance in planes cutting these at an angle of 873°, or parallel with the clinopinacoid. The ordinary sections in which these two sets of enclosures are seen intersecting one another at different angles, according to the direction in which the sections traverse the crystals, present a singular “ cross-hatched” appearance; but it is easy to trace every gradation from the variety with enclosures developed along one set of planes, to that in which they appear along two sets of planes. Frequently another set of enclosures may be detected as making their appearance along a third set of planes, which appear to be parallel to the basal plane r (see Pl. XI. figs. 4 & 6). It is especially noteworthy that the colour, lustre, and general * The curious augite of the Whin Sill, described by Mr. Teall (Quart. Journ. Geol. Soe. vol. xl. (1884) pp. 647-650) as presenting a foliated structure parallel to the basal plane, not improbably owes its peculiarity, as suggested by Prof. Rosenbusch, to an intergrowth of different minerals, or possibly to lamellar twinning on those planes of ultra-microscopical dimensions. (Se¢ also Vom Rath, Zeitschr. fir Krystall. &e., vol. v. (1881) p. 495.) Prof. Rosenbusch is inclined t> regard the foliation of diallage as connected with the existence of lamellar twinning parallel to the orthopinacoid (Mikroskopische Physiographie, vol. i. p. 803), a view which does not appear to be shared by most other petro- graphers. The enclosures in planes parallel to the orthopinacoid in augite, though the first formed, usually exhibit a tendency to indefiniteness and irregu larity not seen in those parallel to the clinopinacoid and the basal plane. + Tschermak has pointed out that the foliation-planes in diallage sometimes deviate by as much as 15° from the true orthopinacoid, and suggests that this may be the result of pressure. A similar but smaller divergence from sym- metrical development of the foliation planes is said to occur in hypersthene. 380 PROF. J. W. JUDD ON THE TERTIARY AND aspect of the augite-crystals is completely altered by the development Within them of these enclosures. The green and black augite acquires a greyish or brownish grey tint and a submetallic lustre along the planes of foliation. In this condition diallage is exactly analogous to bronzite in the series of rhombic pyroxenes. These characters appear to be intensified by weathering action, which seems to act with great facility along the planes of foliation, giving rise to the formation of laminz of calcite and other _secondary minerals, as was pointed out both by Tschermak and Boricky. Under these circumstances the green variety of diallage has its origin in a partial conversion of the augite-substance into hornbiende, with other accompanying changes. The development of two or three sets of enclosures in mutually intersecting planes causes the crystals of augite to acquire the deep- brown tint and the bronzy lustre of common hypersthene (paulite). In this condition the mineral has received from Dana the name of “‘pseudo-hypersthene.” In its microscopic characters, no less than in its colour and lustre, it exhibits such a striking resemblance to the altered forms of the rhombic ferriferous enstatites (the substance to which the name of hypersthene was originally applied) that we may cite it as a very remarkable example of mimicry in the mineral kingdom. The enstatites, and especially their more ferriferous varieties, exhibit the same development of enclosures along certain planes which is found among the augites. Sometimes one such set of planes is developed, and the result is a mineral identical in character with the bronzites and bastites; at other times two or more sets of such enclosures are developed along mutually intersecting planes, . resulting in an appearance like that of the typical Labrador hyper- sthene or paulite. As already pointed out, such a variety was certainly collected by Macculloch in the Cuchullin Hills of Skye, and the same mineral was probably analyzed by Muir. In the rock of Coruiskh the very highly ferriferous enstatite (ambly- stegite) occasionally occurs in a perfectly unaltered state. It then appears as e mineral of a rich brown colour, which, in thin sections, shows the striking dichroism already referred to, the colours changing from a rich garnet-red to blue-green. In other crystals, however, the commencement of change is exhibited by the development of enclosures along planes parallel to the brachypimacoid (see Pl. XI. fig. 9). The ferriferous enstatites having one set of interpo- sitions developed within them, exhibit the submetallic reflections and the striated appearance under the microscope so characteristic of diallage. It is not surprising therefore that the foliated enstatite (bronzite) and the foliated augite (diallage) have been so frequently mistaken for one another. In many cases a second, third, and even a fourth set of enclosures are seen to be developed within the enstatite crystals, in planes parallel to the macropinacoid, and the prismatic faces (see Pl. XI. fig. 8). We thus get the structure produced which is so well known as being characteristic of the original hypersthene (paulite) OLDER PERIDOTITES OF SCOLLAND. - 381 of Labrador. The development of the additional series of enclosures causes the mineral to assume a much darker brown tint, while the submetallic reflections become less pronounced. It does not, however, appear that the presence of one series of enclosures is absolutely characteristic of the less ferriferous ensta- tites, and that the two or more sets of enclosures are confined to the more highly ferriferous varieties. On the contrary, the same crystal may be altogether free from enclosures in one part, may exhibit one set of enclosures in another part, and thus assume the appearance of bronzite, while at certain points within the crystal a second and a third set of enclosures may appear, and the hyper- sthene structure be produced (see Pl. XI. fig. 5). Other things being equal, however, the bronzite-structure is perhaps more likely to be produced in less ferriferous varieties, and the hypersthene structure in the more ferriferous. It is probably too late now to prevent the use of the terms bronzite and hypersthene for varieties differing in composition, otherwise it would be well if the names could be applied to distinguish these differences of structure. The parallelism between the varieties of the monoclinic and rhombic series of pyroxenes iscomplete. In the one series we have a perfect “‘mimicry ” of the members of the other series :— Common Augite corresponds to Ferriferous Enstatite. Diallage corresponds to Bronzite. Pseudo-hypersthene corresponds to Hypersthene. The slight differences of colour between diallage and bronzite, and between pseudo-hypersthene and hypersthene, are not sufficiently constant to be relied upon for the discrimination of these minerals ; the only certain means of distinguishing between them being the measure of the cleavage-angle, or the determination of the extinction- angle in the sections for indicating their system of crystallization. We have seen that diallage is prone to a further change by the conversion of the augite-substance into green hornblende, and even the separation of calcite along its foliation-planes. By the commencement of this change we get the beautiful green diallage ; while its completion results in the formation of smaragdite, actinolite, or similar amphiboles. The enstatites are still more susceptible to changes of the same kind, but the resulting product is altogether different. By taking up water the enstatite substance of the crystal becomes more or less converted into green serpentinous or steatitic substances. The greater ease with which the enstatites undergo alterations of this kind than do the augites, is shown by the fact that while the diallage of the Hebridean gabbros and peridotites is almost always unaltered, the enstatites associated with them nearly always exhibit the first symptons of decomposition, and are not unfrequently entirely converted into the bastite-modification. The Olivines—A change analogous to that taking place in the felspars and pyroxenes, is found affecting the olivines when they are traced to great depths from thesurface. This change consists in the 382 PROF. J. W. JUDD ON THE TERTIARY AND separation of a black or dark brown, usually opaque, substance, probably magnetite and other iron-oxides, along certain planes within the crystals. But in the olivines the separated material assumes very peculiar and highly characteristic forms. In 1871 Prof. Zirkel, in describing the olivines of the gabbros of Mull, pointed out that they contained great numbers of blackish or brownish needles arranged in curious combinations, of which he gave a drawing*. Prof. Zirkel insisted on the fact that similar ap- pearances are never found in the olivines of basalt, but that they occur in the olivines of many gabbros like those of Volpersdorf, the Valteline, and other localities. He also pointed out the fact that these dark inclusions sometimes become so numerous in the olivine as to render the mineral black and opaque, so that it may be easily mistaken for magnetite, except in very thin sections which have been carefully prepared to illustrate the structure of the mineral. Dana has also pointed out this change of olivine into a black opaque substance resembling magnetite, often exhibiting a fissile structure similar to that of micay, and Wadsworth has described the same phenomenon. The study of a series of specimens which have originally existed at different depths from the surface, in the Western Isles of Scotland, enables us to fully understand and explain this interesting change. This is rendered more easy by the fact that the results are, in this case, not complicated by serpentinization, a totally different kind of change due to quite other causes. : The first appearance of the change in question takes place along those irregular fissures that so frequently traverse olivine-crystals. Along these incipient or completed fissures, when they are examined by the aid of high powers, small stellar-groups of black or deep- brown filaments are seen making their appearance mingled with reticulations of cavities containing liquid or solid substances, like those formed in the felspars and pyroxenes. The stellar groups have much the appearance of dendritic markings (see Pl. XI. figs. 1, 2), and when seen foreshortened, or partially within the range of view of the higher powers of the microscope, present the cha~ racters represented by Zirkelt. Sometimes these star-like bodies become crowded together so as to make the surfaces of the cracks and sometimes also the outer portions of the crystal black and opaque (see Pl. XIT. figs. 3, 4). E Precisely similar appearances then make themselves visible along certain planes within the crystal, which: are certainly parallel to the optic axis, but the more exact crystallographic relations of which I have as yet been unable to determine. With these stellate groups of fibres flat brown plates, like those appearing in the pyroxenes, sometimes appear in considerable numbers. Examples may be found of the gradual conversion of the stellate enclosures into tabular ones, by the filling-in of the intervals between the rays_ * Zeitschr. d. d. geol. Gesell. Bd. xxiii. (1871) pp. 59, 60. + System of Mineralogy, 5th ed. (1875) p. 258. t Zeitschr, d. deutsch. geol. Gesell. vol. xxiii. (1871) p. 59, Taf. iv. fig. 11. OLDER PERIDOTITES OF SCOTLAND. 383 of the star (see Pl. XII. figs. 5a, 5b, 5c). As these inclusions multiply, the crystal loses its translucency and finally becomes opaque, and exhibits by reflected light the colour and lustre of magnetite. As the tachylytes of the Western Isles of Scotland are rendered perfectly black and opaque by the quantity of magnetite- dust which they contain, so the olivines are completely obscured in their characters by the development in their midst of these magnetite-enclosures. What is taken for magnetite in many gabbros is nothing but this greatly altered olivine. That these stellate bodies in the substance of the olivine crystals are really inclusions formed within cavities having a rectilinear outline, is demonstrated when they are examined with high powers of the microscope. ach ray of the star is then seen to end abruptly along a right line, and the limits of the cavities within which they are formed are thus clearly indicated (see Pl. XII. fig. 5c). The curiously varied forms represented by Zirkel are due to portions only of these stellate bodies being within the field of view of the microscope at the time and often being viewed obliquely; but by carefully focussing up and down, their true nature can be readily made out*. In their absolute dimensions these enclosures of the olivine crystals vary between very wide limits, as is the case with the similar bodies in the felspars and pyroxenes; while some of the enclosures can be seen and studied with quite low microscopic powers, others are crowded into a nebulous haze which can only be resolved by the very highest powers. j The Birotites, which are among the most frequent of the accessory minerals in the gabbros and peridotites, exhibit a similar secondary structure to that described in the felspars, the pyroxenes, and the olivines. Tabular enclosures of a deep brown or black colour are developed along the planes of easy cleavage of the mineral, and are sometimes so abundant as to render the mineral almost opaque (seo?) “Xr figs..8, 9). §5. Narcurre anp OrieIn or THE CHANGES WHICH HAVE TAKEN PLACE IN THE MINERALS OF DEEP-SEATED Piutronic Rocks (“‘ ScHIL- LERIZATION ”’). We have seen that alike in the felspars, the pyroxenes, the olivines, and the biotites of plutonic rocks, there is evidence of pro- gressive change taking place at gradually increasing depths. This change consists in the development along certain planes within the erystals of tabular, bacillar, or stellar enclosures, which, reflecting the light falling upon them at certain angles, give rise to the peculiar phenomenon expressed by the term “Schiller.” It will be con- venient to have a general name for this kind of change, and I pro- pose to employ the term ‘“Schillerization” to express it. Thus I shall call diallage and pseudo-hypersthene “ Schillerized augites,” * Zeitschr. d. deutsch. geolog. Ges. vol. xxiii. (1871) pl. iv. fig. 11. Zirkel, Mikroskop. Beschaff. der Min. und Gest. (1873) p. 214. 384 PROF, J. W. JUDD ON THE TERTIARY AND bronzite and the typical hypersthene of Labrador “ Schillerized fer- riferous enstatites.”’ The nature of the enclosures which give rise to the “Schiller” phenomenon of minerals has been investigated by many mineralogists ; but, as might have been anticipated when their minute size is taken into account, the results arrived at are very discordant *. The enclosures vary in colour from grey to yellow, and through various shades of brown to purplish red; while they are sometimes so dark as to be almost black and opaque. In all cases, so far as it is possible to examine such minute objects, they prove to be isotropic. As a general rule, they are found to be infusible, and to resist the action of the strongest hydrochloric and other acids. In form, these enclosures greatly vary. Sometimes they appear .to have very definite outlines, which has led them to be regarded as microscopic crystals of hematite, magnetite, brookite, augite, or other. minerals; but these identifications have not only not been sup- ported, but in many cases have been actually disproved by chemical analysis. Nevertheless the regularity of their forms in the same crystal, and sometimes a wonderful agreement in the angular measures which they give, are very striking facts. In other cases, as for example in the Labrador hypersthene, the tabular enclosures, while presenting perfectly flat and parallel sides, exhibit the most irregular contours along some of their edges, and their forms appear to be quite irreconcilable with the hypothesis that they are micro- scopic crystals. From a consideration of all that has been adduced by other in- vestigators, taken In connexion with my own observations, I am led to the conclusions that the substances forming these various enclosures do not consist of any definite chemical compounds assuming the regular crystalline forms belonging to mineral species, but that they are mixtures of various oxides in a more or less hydrated condition, such as hyalite, opal, gdthite, and limonite; hence their isotro- pism, their variation in colour, and their resistance to the action of acids. All Schillerized minerals on analysis yield a small but notable proportion of water, which is probably contained in these enclosures. The suggestion which seems to me to be most in accord with all the facts of the case, is that these enclosures are of the nature of negative crystals which are more or less completely filled with products of decomposition of the mineral. When these negative crystals are completely filled with foreign substances, the enclosures assume the outlines of true crystals, though they do not, of course, exhibit their optical properties: it is noteworthy that in some cases a corre- spondence between the angles of the enclosing mineral and the inclusions seems to have been clearly made out. But in other cases the secondary products are insufficient to fill the whole cavity * This subject has been especially treated of by Scheerer (Pogg. Annal. Ixiv. 1845) ; Vogelsang (Archiv Neerland. iii. 29, 1868) ; Kosmann (Neues Jahrb. f. Min. &e. 1869, p. 532); Hagge (Mikroskop. Untersuch. iiber Gabbro, &e. 1871); Trippke (Neues Jahrb. f. Min. 1878, p. 676). OLDER PERIDOTITES OF SCOTLAND. 385 of the negative crystals, and occupy irregular spaces within them. In some cases, like that of the olivines, the distribution of these products of decomposition within the negative crystals is partially determined by crystalline forces, and curious dendritic forms, of microscopic dimensions, are the result. That this is really the ex- planation of the dendritic forms seen in olivine, is shown by the fact that the ends of the star-like masses are bounded by straight lines, the sides of the negative crystals (see Pl. XII. figs. 5a, 5b, 5c). It is a very noteworthy circumstance that these negative crystals are formed along certain definite planes within the original crystal. The studies of the so-called ‘“ Aetzfiguren” by Exner, Baumhauer, and others have shown that the surfaces of crystals, and of sections of crystals, are very unequally affected when submitted to the action of appropriate solvents. The peculiar disposition of molecules in a crystal which causes it to yield most readily along certain planes to the mechanical forces applied in scratching and fracture, and which permits the waves of light and heat to traverse it at different rates in different directions, is equally manifested when the crystal is operated upon by solvent agents. We can understand how, under these circumstances, solution is set up along certain planes within the crystal, innumerable negative crystals being formed, while the products of decomposition are deposited within them. The action may be compared to what takes place when a beam from the sun or an electric lamp is passed through a block of ice. The beautiful ice-stars partially filled with water appear to be exactly analogous to the negative crystals formed by solvent action in augite, for example, and occupied by the hydrated oxides which result from its decomposition. Tschermak and others have pointed out that the lines along which solution takes place most easily are not necessarily the edges of cleavage-planes; and it has also been shown that the twinning of crystals modifies the “ Aetzfiguren,” as it certainly does the position of the plane of most easy chemical action, as revealed by the phenomena of Schillerization (see Ante, p. 379). There is one point in connexion with this subject which appears to me to be specially worthy of attention, though, as far as I am aware, its importance has hitherto been very generally overlooked. The “ Schillerization” of dark-coloured ferriferous minerals, like proto-hypersthene and augite, results in the discharge of colour from the substance of the crystal; and instead of a dark green or brown substance, we get a nearly colourless one, within which the innumer- able deeply coloured enclosures are distributed. Now, inasmuch as the chemical composition of the whole crystal is scarcely, if at all, altered by this molecular change, it is fair to conclude that the iron and other oxides which gave the colour to the crystal have been dissolved out and deposited in the substance of the enclosures. That this is really the case, we have, I think, a singularly beautiful proof, The researches of many mineralogists have demonstrated that in the pyroxenes, the micas, and many other groups of minerals, a remarkable relation can be discovered between the proportions of certain ingredients, notably the iron, in different varieties, and 386 PROF. J. W. JUDD ON THE TERTIARY AND certain optical constants, such as the position of the plane in which the optic axis lies and the angle between the optic axes *. The researches by which the optical constants of minerals have been determined have proved that not only do the colour and cha- racteristic pleochroism disappear in the substance of crystals + which have undergone Schillerization, but that the position of the optic axes and the angle which they make with one another are also affected. This remarkable effect of the Schillerizing process is shown if we compare unaltered and altered examples of minerals of the same chemical composition with one another, augites with diallages and pseudo-hypersthenes, ferriferous enstatites with bronzites and hypersthenes. Tschermak even points out that the optical constants of diallage are practically the same as those of diopside +. In the latter mineral ferrous oxide was almost absent from the first; in the former it has been to a great extent removed from the substance of the crystal and collected into the enclosures during the process of Schillerization. § 6. Tur AGENCY BY WHICH THE SCHILLERIZATION OF MINERALS HAS BEEN EFFECTED. In seeking for the causes which have produced in minerals the very remarkable changes which we have grouped together under the name of Schillerization, there are two very important facts which must be borne in mind. Im the first place such changes are quite distinct from those which result from weathering action, or the penetration of water from the surface. Under the influence of this kind of action, felspars are more or less completely kaolinized, and their elements may subsequently recrystallize as zoisite and other minerals ; augites are converted into uralite or directly into hornblende, and olivines and enstatites into serpentine, steatite, and tale. But in the minerals of the rocks we are describing, it is manifest that crystals which do not exhibit the smallest trace of Schillerization may be completely altered by weathering action; and, conversely, crystals which are perfectly fresh and undecomposed may have undergone the most striking effects of Schillerization. In cases where the results of weathering action have been superinduced upon those following from Schillerization, very complicated phenomena may be presented, which it may require much care to unravel. Cases of this kind we shall proceed to consider in the second part of this paper. But the examples of the Western Isles of Scotland are * See for the pyroxenes, Tschermak, Mineral. Mitth. vol. i, (1870); Wilk. Zeitschr. f. Kryst. vol. viii. p. 208 (1884) ; Dolter, Neues Jahrb. f. Min. &c. 1885, vol. i. p. 43. { Itis true that slices of hypersthene viewed witha dichroiscope appear strongly pleochroic. But when examined with a high power, the substance between the enclosures is seen to be nearly colourless, and to exhibit only faint traces of pleochroism. In examining the whole slice of the mineral the light transmitted by the brown enclosures is affected by the intermediate substance, and a general effect of pleochroism is produced, which is not seen in either crystals or enclosures separately. ¢ Lehrbuch fiir Mineralogie (1883), p. 440. OLDER PERIDOTITES OF SCOTLAND. 387 particularly valuable for the purposes of study ; for there the felspars often show no trace of kaolinization, the augites no trace of uraliti- zation or of amphibolization, and the olivines no trace of serpenti- nization ; and yet these several minerals, as we have pointed out, exhibit in the most striking manner the effects of Schillerization. The study of these rocks in the field has clearly demonstrated that the degree of Schillerization of the several minerals can be correlated with the depth from the surface at which the rocks have formerly existed. In the more deeply seated rocks the most perfect Schilleri- zation has taken place, and in those at less depth fewer planes within the crystal have been attacked, all traces of the action disappearing when the rocks have existed near the surface. That the action producing Schillerization is a secondary one is proved in several ways. Itis perfectly true that enclosures are often formed in crystals during their growth, and that, at high temperatures and under great pressures, abnormal crystal-growths frequently arise. In this way it may be suggested that augite might always crystallize with the diallage- and pseudo-hypersthene-modifications, ferriferous enstatite with the bronzite- or hypersthene-modification, and so on. But against the acceptance of this suggestion several very important considerations may be urged. ‘The contents of the negative crystals are evidently products of decomposition, hydrated oxides like chal- cedony, opal, géthite, and limonite. Further, as I have already shown, the action of Schillerization can in many cases be seen to be set up, from the surface of the erystals and along the cracks which traverse it. And, lastly, the enclosures are altogether absent from some crystals in deep-seated rocks, which appear to have escaped altogether from the action which has produced this phenomenon. Schillerization is thus proved to be due to local and not to general causes. On these grounds, then, I think it is impossible to doubt that what are now crystals of diallage were once common augite, that the bronzite and hypersthene are altered ferriferous enstatites, and that the peculiarities of the deep-seated crystals of labradorite and olivine have been acquired since their original formation. Bearing all these facts in mind, it appears impossible to resist the conclusion that the solvent agents which have produced Schillerization are the water and other fluids which have permeated the rock- masses, and that their solvent action has increased with the pressure, that is tosay with the depth from the surface. I need only refer to the classical researches of Daubrée, Sorby, Guthrie, and others, as placing beyond all doubt the fact of the increase of the action of solvents by pressure. When we remember the enormous volumes of steam and other gases given off by great volcanoes during their eruption, and further that these eruptions are continued through geological periods of vast duration, bearing in mind too that the evolution of these gases does not terminate with the violent activity of the volcanic vent, but is equally manifested during the “ Solfatara stage,” and that enormous tracts of volcanic rocks are found altered by surface-emanation of steam, we can well understand how potent must be the influences 388 PROF. J. W. JUDD ON THE TERTIARY AND which are operating simultaneously upon the deep-seated rock- masses below. The circumstance of the crystals of such rocks being full of numerous cavities, many of which contain saturated solutions of the alkaline chlorides and sulphates, or are filled with solid substances like wollastonite and other silica-compounds, and of such cavities also enclosing carbonic acid in a liquid condition, all bear witness to the presence of these solvents and to the potency of their action under pressure. | The study of these deep-seated rocks at different depths shows that the water and other solvents which permeate the whole of the crystals under the enormous pressure attacks certain silica~-compounds more readily than others ; probably the compounds of silica with iron _ and the alkalies are among the first to pass into solution. Eventu- ally the whole of the compound silicates yield to the solvent and are broken up; but this does not take place uniformly through the crystals. In the direction of certain planes within crystals the mole- cules are in a state of less perfect stability with respect to chemical agencies than others, and along these planes the solvents eat out for themselves hollows (negative crystals) which become filled with the hydrated silica, the hydrated ferric oxides, and other products of decomposition. At increasing depths new planes within the crystal become susceptible to the action of solvents, and fresh enclosures are formed along them. ‘Thus, at moderate depths, the only planes along which augite-crystals are attacked by the solvents, and along which they have enclosures (infilled negative crystals) formed, are the planes parallel to the orthopinacoid; but at greater depths planes parallel to the clinopinacoid and the basal plane are similarly attacked. The planes of chemical instability are not necessarily - identical in position with those of imperfect cohesion (cleavage-planes); indeed in many cases, as we have seen, they are wholly different. But in many cases the position of these planes of easy solubility in a erystal are clearly modified by the twinned condition of the erystal. In some cases Schillerization consists only in a redistribution of the matter within the crystals. Thus diallage, as a general rule, differs in composition from augite only by the presence of a per- centage of water which, as we have already seen, is probably combined with the materials which fill the negative crystals. But in many cases the dissolved material may be carried away from the crystal and deposited within the cavities of neighbouring crystals of different species. In this way ferric oxide, probably derived from the pyroxenes, olivines, and magnetite, comes to be deposited within the negative crystals of labradorite. In the end this process of Schillerization must result in the blending together in the most inex- tricable manner of materials derived from different crystallized minerals, and the whole characters of the rock may be completely altered. It has long been known that the faces and cleavage-planes of crys- tals are attacked by appropriate solvents in an unequal manner, so as to give rise to the characteristic forms of two dimensions known as —— lhe. Oo eee OLDER PERIDOTITES OF SCOTLAND. 389 Aetzfiguren. But the Schillerization of minerals consists in the pro- duction by natural causes of Aetzfiguren in three dimensions. It bears witness to the existence of certain planes within crystals along which a greater susceptibility to chemical action exists than in others. It proves that, while often independent of the directions along which mechanical force and the diiferent kinds of radiant energy most easily act, the planes along which the chemical forces operate are modified and controlled by structures like twinning. All these con- clusions are in complete harmony with the results which have been obtained by the study of the Aetzfiguren. The results attained by the observations and reasonings which we have been describing bear the same relations to those obtained by the study of the Aeizfiguren, as the phenomena of cleavage in a crystal do to the observations made on crystal faces by means of the sclerometer. All the changes of which we have hitherto spoken are such as may be traced in their effects by the aid of the microscope ; but the same forces probably lead to other modifications of the internal structure of crystals, which are altogether ultra-microscopical and quite incapable of being detected by direct vision. But as it is well known that light-waves are capable of being interfered with by structures too minute to be discerned by the human eye, so we can readily understand how solution along certain parallel planes within the felspar crystal may lead to the formation of thin plates or layers, probably composed of chalcedonic material, which give rise to the beautiful chatoyant effects exhibited by these minerals when they have been submitted to deep-seated action. We have already pointed out that the alteration in the density and chemical composition of these chatoyant varieties of felspar support the view that they have undergone the kind of change which we have been describing, and that, in the Western Isles of Scotland, this phenomenon is exhibited only by the felspars of what have been the most deeply-seated rock- masses. § 7. VARIETIES oF THE TERTIARY Utrra-sasic Rocks. The Tertiary peridotites and other ultra-basic rocks differ from one another both in their mineralogical constitution and in their structure. Varieties corresponding to each of the rock-species which have been established for the different types of peridotite are easily recognizable in the Western Isles of Scotland. Thus in the Shiant Isles and in the central parts of Rum we find a rock almost wholly made up of grains of olivine enclosing rounded particles of chromite and picotite—a rock which must be classed with the “‘dunites.” In various localities in the island of Rum, and also in the Shiant Isles, we find rocks consisting essentially of olivine and augite, and these must be classed as “ picrites.” Occasionally we find a considerable amount of a more or less ferriferous enstatite, with some picotite or chromite superadded to the ingredients of the last-mentioned rock, and we have then an analogue of “lherzolite.” Some of the veins which intersect the gabbros and peridotites of Rum are wholly made up of a felspar (which, by its extinction-angles, its specific gravity, OQ. 5: G5. Noe 163. 25 390 PROF. J. W. JUDD ON THE TERTIARY AND and its flame-reaction, is proved to be anorthite) and olivine. I was at a loss to find any exact analogue of these felspar-olivine rocks ; but Professor Bonney has pointed out to me that in some varieties of the forellenstein (troctolite) of Volpersdorf, in Silesia, the augite becomes inconspicuous and almost disappears, and we have a rock similar to the Scotch variety which I have indicated. Professor Bonney has found the same rock in an altered state at Coverack Cove in Cornwall*, Other veins and enclosures in these rocks consist of anorthite and augite, and may be classed with the eucrites (see Pl. XIII. figs. 1, 2, 3, 4, 5, & 6). As all of these varieties of the Tertiary ultra-basic rocks are found passing into one another, and into the gabbros and dolerites, by an increase in the quantity of one mineral or by the diminution and disappearance of others, it will, I think, be more instructive to con- sider the varieties exhibited by the rocks of different localities when their microscopic structures are considered than to dwell upon the merely accidental varieties of mineralogical constitution. It may be mentioned at the outset that, as a general rule, the peridotites vary in structure with the gabbros and dolerites with which they are associated. We thus find peridotites of granitic structure, others of granulitic structure, and others, again, of ophitic structure (see Pl. XIII.). The most perfectly crystalline type of these peridotites is found in the valleys in the central part of the island of Rum. A typical example of these rocks collected near the road between Kinloch and Harris is highly crystalline, of a black colour with a few scattered felspar-crystals, and has a specific gravity of 3:18. The olivine of this rock is of a nearly black colour, owing to the abundance of magnetite enclosures it contains; it can, however, be distinguished from the augite by its lustre and its fracture. It is not surprising to find that Macculloch, misled by the unusual colour of the olivine, failed to distinguish that mineral; and, regarding the rock as being wholly composed of augite, he gave toit the name of “ augite- rock.” Thin slices under the microscope show the rock to be essentially made up of large crystals of augite and olivine. Theaugite is of pale greenish or brownish tint by transmitted light, and exhibits very faint dichroism; but its cleavage-cracks, which are well marked, are characteristic of the mineral. Both the cleavage- and irregular cracks of the mineral are marked by bands of enclosures, consisting of cavities, sometimes empty, sometimes containing a liquid with a bubble, but most commonly filled with a solid substance of a reddish brown, sometimes almost black colour. This augite only occasionally exhibits the first traces of a passage into diallage by the development of enclosures in planes parallel to the orthopinacoid. The olivine of this rock is in the most beautifully fresh condition, and seldom shows any trace of serpentinization. It polarizes with * Quart. Journ. Geol. Soc, vol. xxxiii. (1877) p. 909. OLDER PERIDOTITES OF SCOTLAND. 391 the usual brilliant colours, but presents a somewhat curious appearance from the abundant enclosures which it contains, causing it to appear of a dusty grey tint. The numerous fissures which traverse the olivine grains are often stained of a bright yellow colour ; along them are developed numerous cavities which are seen in some cases to be united by a ramifying system of canals, and not un- frequently contain liquids with a moving bubble. In most cases, however, they appear to be filled with brown or black decomposition- products like those in the augite-crystals. Along the same fissures are seen to be developed the curious dendritic stars or networks of a black or brown colour, and these are sometimes present in such numbers as to render the planes of the fissures black and opaque. In addition to these enclosures along the planes of the fissures, other stellar ones make their appearance in prodigious numbers within the sub- stance of the crystal, communicating to it the dusty appearance already described. These are seen to be arranged in a series of planes parallel to the optic axis of the crystal, and the star-like inclusions are often mingled with and pass into others in the form of thin brown or black plates. Among the commonest of the accessory minerals of this rock are felspar, biotite, a ferriferous enstatite (hypersthene), magnetite, and chromite or picotite. The felspar is a plagioclase, which in its altered condition offers a striking contrast to the fresh angite and olivine of the rock. It is full of cavities, and its substance is often seen to have undergone more or less complete conversion into various secondary products. : The biotite, when unaltered, is of a deep brown tint, but is often Schillerized by the development of dark-coloured enclosures in planes parallel to the basal plane. Under these circumstances the substance of the crystals becomes much paler in tint. The ferriferous enstatite (hypersthene) exhibits the usual marked pleochroism of that mineral when undecomposed, but it usually shows a great tendency to serpentinous alteration. The magnetite and chromite or picotite form only a very subor- dinate part of the rock. The latter mineral by its decomposition appears to communicate a very striking chrome-green tint to portions of the rock. Some of the peridotites of the higher mountains in central Rum exhibit afar less perfectly granitic structure, small crystals and granules of olivine being mingled with finely granular augite, as in the porphyro-granulitic dolerites. They resemble such dolerites without their felspar. These rocks have a specific gravity of 3-09. The olivine of these rocks is often more or less darkened by the multitude of black stellar inclusions which it contains. These granular peridotites of central Rum are intersected by veins of many interesting rock-varieties. Among these occur porphyritic peridotites consisting of large individuals of olivine scattered through a granular base of olivine and augite and gabbros, 282 392 PROF. J. W. JUDD ON THE TERTIARY AND with the several minerals sometimes disposed in bands parallel to the sides of the vein. (See p. 359.) One of the varieties of peridotite in the island of Rum is a rock of such beauty as to have attracted the attention and excited the admiration of all visitors to the island *. It is found constituting considerable portions of the mountains of Halival, Haiskeval, and Tralival, and is seen passing everywhere into an augite-gabbro. Different portions of these great mountain-masses appear to vary chiefly in the quantity of felspar which they contain. The felspathic varieties are true augite-gabbros, consisting of a very fresh felspar, often perfectly clear and glassy in appearance, a bright green augite, and an olivine which has undergone the peculiar alteration which makes it resemble in aspect chondrodite. The rock is sometimes fine-grained and at others very coarse-grained, and the mixture of colourless, bright-green, and yellow crystals is very striking. 3 The non-felspathic varieties are picrites and lherzolites, rocks having a specific gravity of about 3-20, the admixture of bright- green augite, and the yellow olivine with more or less enstatite, giving them a very beautiful appearance (see Pl. XIII. fig. 3). The augite of these rocks is usually of a bright emerald-green tint by reflected light, and pale green passing into pale brown by transmitted light. It usually exhibits a very feeble pleochroism. The augite sometimes forms well-developed crystals, but more usually it exists as rounded grains, like those of coccolite. The composition of this diopside, or slightly ferriferous augite, is illus- trated by the analysis quoted on p. 367. This green augite, as well as the pale brownish varieties which accompany it, is traversed in all directions by cracks which are marked by numerous enclosures, which are sometimes liquid- or gas-cavities, but are not unfre- quently filled with dark-brown or black solid materials. These augites exbibit admirable illustration of the initial stage of Schil- lerization. A few scattered tabular enclosures make their ap- pearance along planes parallel with the orthopinacoid, and these in other examples are seen multiplied until the augite becomes a typical diallage. The olivines of these rocks form more or less rounded or oval grains, often enclosing globular particles of chromite or picotite, which are generally black or opaque at their centres, but slightly translucent, and dark-brown in colour at their edges. A very marked feature of these olivines is their yellowish or brownish- yellow tint, so different from that of the mineral in its normal condition. Under the microscope this peculiar colour is seen to be confined to the cracks which traverse the crystals in all directions. The yellow tint is present in cases where not the smallest trace of serpentinization can be detected in the crystal. Along these cracks we find the curious stellate enclosures being developed, and these * See Jameson, ‘ Mineralogy of the Scottish Isles, vol. ii. p. 51; Maceulloch, ‘The Western Isles of Scotland,’ vol. 1. p, 485; Heddle, Trans. Roy. Soc. Hdin. vol. xxviii. (1879) p. 478. OLDER PERIDOTITES OF SCOTLAND. 393 may multiply till they form black bands, traversing the crystal in all directions; lastly similar inclusions, sometimes mingled with brown plates, make their appearance along a series of parallel planes traversing the crystal in the direction of the optic axis, and these increase in number till they communicate a dusty appearance to the crystal. | The accessory minerals of these peridotites of Halival and the adjoining mountains of Rum are as follows :—felspar, a clear variety, crystallizing in forms intermediate between the lath-shaped crystals of basalt and the broad forms common in the massive gabbros, is nearly always present in small quantities, and may increase in abundance till the rock passes into a gabbro; fer- riferous enstatite (hypersthene), which, when it occurs with the granular variety of augite, also assumes similar granular forms, but is at once distinguished by its colour, its remarkable pleochroism, and its extinction in positions parallel to the vibration-planes of the crossed nicols; biotite occurs but rarely, while magnetite and chromite (or picotite) are universally present. It appears as though the opaque magnetite passes by insensible gradations into the trans- lucent and deep-brown chromite or picotite. The last, but by no means the least interesting, of these Tertiary peridotites of Scotland which I shall notice, is that which occurs in the Shiant Isles to the North of Skye; it exhibits the most beautiful example of the ophitic structure in these rocks. The igneous rocks of these islands, as pointed out in my previous paper *, form a great intrusive sheet 500 feet in thickness forced between strata of Inferior-Oolite age. The vertical columns of this intrusive mass constitute, as Macculloch has pointed out, one of the most imposing spectacles in the British Islands. The columns, 500 feet long and from 4 to 6 feet in diameter, form a range of inaccessible precipices rising directly from the sea. _ Owing to the rising of a storm, I was compelled to render my visit to these little-known islands shorter than I could have wished, and consequently I had an opportunity only of tracing the relations of the igneous to the sedimentary rock-masses, and of collecting the fossils from the latter. I was not able to devote any time to deter- mining the relations of the different varieties of igneous rocks to ' one another. As many varieties of the rocks as possible were, however, collected from different parts of the island by myself and a friend, Dr. Taylor Smith +, who accompanied me. The rock of this great intrusive sheet was classed by Macculloch as an “ augite-rock,”’t the augite being by far the most conspicuous mineral in it. A careful study of the large series of specimens brought from the islands shows that about one half of them should be classed as ophitic dolerites, and the other half as peridotites. But every specimen collected shows such variations owing to the * Quart. Journ. Geol. Soe. vol. xxxiv. (1878) p. 677. + I am greatly indebted to Dr. Taylor Smith for allowing me to study the whole of his specimens in connexion with my own. { Western Isles of Scotland, vol. i. p. 439. 394 PROF, J. W. JUDD ON THE TERTIARY AND increase or decrease of felspar in different parts of the rock, that I can scarcely doubt of there being constant and insensible passages in the rock-mass from the felspathic dolerite to the non-felspathic peridotite. The structure of the dolerites is exceedingly interesting ; nowhere in the British Islands am I acquainted with more beautiful illus- trations of the ophitic structure ; the very similar dolerite which forms the great intrusive sheet at Portrush in Ireland comes nearest to it. The fractured surfaces of the rock exhibit the broad faces of black crystals of augite, occasionally interrupted by the enclosed felspar crystals. Under the microscope the augite, which by transmitted light is of a rich brown tint, 1s seen to form great crystals, the continuity of which is indicated by the persistency in direction of the cleavage-cracks, and by their uniform tint when viewed by polarized light. Within these broad crystals of augite are enclosed innumerable rectangular crystals of plagioclase felspar and rounded grains of olivine. In the accompanying peridotites the felspar almost completely disappears. In some varieties, which may be classed as picrites, we find a number of broad crystals of augite which enclose nume- rous grains of olivine (see Plate XIII. fig. 4). In other cases the grains of olivine become so numerous as to make up the mass of the rock, and augite appears only occasionally in their interspaces. The latter variety may be classed with the dunites. Under the microscope, the rich brown augite of the Shiant-Isles rock exhibits gas- and liquid-cavities along its planes of fracture and strain; but these are seldom filled with solid material, and the tabular inclusions producing Schillerization are, so far as my expe- rience goes, never present in them. The augite of these rocks is seen in some cases to pass into paramorphic hornblende. The olivine of these rocks is a very interesting mineral. In the thinnest sections it exhibits a distinctly yellow colour by trans- mitted light. This colour is nearly as intense as in the fayalite of the eulysite of Tunaberg, for an opportunity of studying which I am indebted to Mr. Thomas Davies, of the British Museum. This colour of the olivine is so marked and persistent that I can scarcely doubt of our having a highly ferriferous olivine associated with the dark ferriferous augite of the rock. As a rule, the minerals of the Shiant-Isles rocks are remarkably fresh and un- weathered, but the olivine in some of the specimens, which were for the most part collected from fallen blocks washed by the sea, exhibits a very partial serpentinization. Enclosures with solid matter of black colour, and others containing liquids and gases occur along the planes of fracture; but the black stellate enclosures are rare. Occasionally, however, black or dark-brown enclosures are seen encroaching from the fracture-planes along planes parallel to the optic axis of the olivine grain, and so crowded together as to render the crystal black and opaque. In addition to the non-felspathic rocks, which we have classed as OLDER PERIDOTITES OF SCOTLAND. 395 dunites, lherzolites, and picrites, we have the felspathic rocks which must be assigned to the troctolites (anorthite-olivine rocks) and the eucrites (anorthite-augite rocks). The troctolites (forellensteins) in all cases exhibit intergrowths of felspar-crystals, forming a mass through which single grains or groups of grains of olivine are irregularly distributed (see Pl. XIII. fig. 5). Except in the perfectly fresh and unaltered condition of the minerals of which they are composed, and in their finer grain, these rocks exactly resemble in structure the well-known forellen- stein of Volpersdorf. The eucrites (anorthite-augite rocks) exhibit both the granitic and granulitic types of structure. An interesting example of the latter variety is illustrated in Pl. XIII. fig. 6. The mass of basic and ultra-basic rocks in the island of Rum, which covers an area of from eight to ten square miles, and rises into a number of mountains varying from 2000 to 3000 feet in height, is made up principally of the minerals anorthite (or a felspar closely approximating in composition to that species), augite, and olivine. When all three are present, as is most frequently the case, we have an olivine-gabbro; when the first disappears we get a picrite, when the second is wanting we have a troctolite, and when the third is absent a eucrite. When both the first and second are wauting the dunites are formed; and the addition of the less abun- dant minerals, the enstatites, the biotites, and the spinellids, gives rise to lherzolites and other varieties. All these forms are found passing into one another by the most insensible gradations, and it would be possible, though, I think, most inexpedient, to propose names for other curious mineral combinations which occur here. The Shiant Isles offer perfectly similar examples of transitions between these different types of basic and ultra-basic rocks. Parr II. THE PaLmozo1c PERIDOTITES AND ALLIED Rocks. So far as is at present known, there are no peridotites of Mesozoic age in Scotland. The numerous masses of more or less altered ultra-basic rocks which are found scattered about the country, appear to have been formed during the Paleozoic epochs ; but some of them may be of Archean age. Certain of these old peridotites can, how- ever, be proved to be of the age of the Old Red Sandstone and the Carboniferous. At first sight the Palzczoic peridotites of Scotland appear to present the most striking contrast in their characters with those which we have been describing as belonging to the Tertiary epoch. But the more carefully we study these rocks, the more distinctly is if seen that the differences between the older and younger rock- masses are not essential but accidental ones,—the result of al- terations which have taken place during the enormous periods of 396 PROF. J. W. JUDD ON THE TERTIARY AND time which have intervened between the eruption of the older and younger rocks respectively. In the Tertiary peridotites the several minerals, olivine, enstatite, augite, picotite, &c., are perfectly fresh and unweathered; but in the Palzozoic rocks these minerals are represented, in most cases, only by their pseudomorphs ; and it requires the most careful study to determine what was the nature of the original rock. When this is done, however, we are impressed by the conviction that in minera- logical constitution, as well as in structure, these Paleozoic perido- tites present us with examples of all the varieties found among the Tertiary peridotites. It may be convenient to apply distinct names to some of these much altered igneous rocks, just as it is admissible to term the indurated argillaceous sediments shales, while we call the less altered rocks clays. But it is a fact which cannot be too strongly insisted upon that when due allowance is made for the effects of alteration, operating during the enormous intervals of time which have separated the eruption of the Paleozoic and Tertiary peridotites, the agreement in all the orginal and essential characters between the rocks be- longing to these widely separated periods is of the most complete character. § 1. ALTERATION oF THE MINERALS IN THE PaL#ozorc PERIDOTITES. The most striking fact concerning the Paleozoic peridotites is that, as a rule, the whole of the original minerals of the rock have been converted into their pseudomorphs. The bulk-analysis of the rocks shows that they differ in composition from the Tertiary peri- dotites by the addition of water, and the diminution, to some extent, of the silica and certain of the bases. The olivines have been con- verted into serpentine ; the enstatites are often represented by the same mineral or by steatite; the augites have become hornblendes, and the felspars have similarly been changed to zoisite and other minerals. These changes are of a totally different kind from those which we have'seen to affect the minerals in the more deeply seated eruptive rock-masses of the Tertiary period. Whether previously in their typical form, or in a more or less Schillerized condition, these minerals of the Paleozoic peridotites are equally affected by changes of a totally different character and origin. In some cases the change consists in the addition of water, and the conversion of an anhydrous silicate into a hydrous one. In other cases, the change appears to be a purely molecular one, the conversion of an unstable mineral into a stable one. That these changes are produced at moderate dielanves from the surface where the minerals are affected by the percolation of atmo- spheric waters there cannot be any doubt. By the study of a suffi- ciently large series of specimens it can be shown that the changes in question have reached their maximum in those cases where the exposure of the rocks to atmospheric influences has been greatest, while more deeply seated portions of the rock remain comparatively ‘ lord OLDER PERIDOTITES OF SCOTLAND. 397 unaltered. Morcover, the change is, in many cases, seen to be set up from the surfaces or fissures of the minerals to which percolating atmospheric waters can most easily find access. It will be instruc- tive to study the changes which the several minerals are found undergoing, under these circumstances, in the Palaeozoic peridotites. Olivine is the mineral in the peridotites which undergoes change most easily, and in almost every case it is found converted into serpentine ; indeed it is quite rare to find examples of the un- altered olivine in these Paleozoic rocks. The occurrence of unmis- takable pseudomorphs of serpentine after olivine, and the occurrence of particles of unaltered olivine in the midst of the serpentine masses, afford abundant evidence, however, of the fact that the serpentine is for the most part altered olivine. When the olivine has undergone the changes described in the first part of this paper, and as a consequence contains stellate, tabular, and irregular enclosures of magnetite and other oxides, these are sometimes seen to persist after the hydration of the enclos- ing mineral. But the conversion of the olivine into serpentine, as is well known, is usually accompanied by a separation of magnetite, the silica: combined with the iron of the original mineral being pro- bably to some extent carried away in solution. In many cases it appears to be impossibie to separate the mixed oxides formed during the Schillerization of the olivine from those liberated during its serpentinization. The Rhombic Pyroxenes (Enstatites) undergo change much less rapidly than do the olivines. This is shown by the fact that in ‘rocks which have originally consisted of olivine and enstatite, the former mineral is often entirely changed to serpentine, while the latter remains comparatively unaltered. The change which the enstatites undergo seems to vary in different cases. Mr. G. H. Williams has described an interesting example of the direct conversion of a ferriferous enstatite (hypersthene) into a brown hornblende*. But of this kind of change I have not found any examples among the numerous enstatites of the Scottish rocks. On the contrary, the change in the mineral appears usually not to be a simply molecular alteration, but to.be the result of hydration. Thus in the enstatite-basalt of a dyke at Carroch in Forfarshire, the fine crystals of highly ferriferous enstatite are found passing along their edges and fissures into a green ‘substance undi- stinguishable from that found in similar situations in olivine crystals, and in some cases the whole crystal is converted into this substance. Again, in the serpentine dyke of the same district, the central and least altered portion consists of serpentine crowded with enstatite erystals, but in the more altered portions of the same mass, the enstatite is seen to pass into serpentine 7. * Amer. Journ. Sci. 3rd ser. vol. xxviii. (1884) p. 262. t According to my own experience, the rhombic pyroxenes are generally converted into a serpentinous material, while the augites pass into a uralitic substance or directly into hornblende; and I would venture to suggest that the crystals which Mr. Williams describes as changing into hornblende, in the passage referred to, may be pseudo-hypersthene, and not true hypersthene. 398 PROF. J. W. JUDD ON THE TERTIARY AND When the enstatite has been previously Schillerized, the charac- teristic enclosures often persist after the serpentinization of the material in which they are enclosed. We may thus sometimes infer the former existence of a particular mineral in a rock by the presence of the characteristic enclosures of the mineral in the midst of its alteration-products. The Monoclinic Pyroxenes (Augites) usually undergo only the molecular change by which they pass into hornblendes. Thus crystals of the dark brown ferriferous augite of the Shiant-Isles rock are seen passing into dark-brown hornblende with the charac- teristic pleochroism and cleavage of that mineral. It is worthy of notice, as pointed out by Williams *, that in these cases of the con- version of a pyroxene directly into hornblende the principal planes of the two minerals are parallel, and even the planes of twinning of the original may persist as such in the altered form 7. When augite has been submitted to Schillerization before altera- tion the results are of a very different kind, as is so well seen in the saussurite-gabbros or wurlitzites. By the collection of the iron of the mineral into the enclosures a substance is left which has the composition and optical properties of diopside, and this is altered into the green varieties of hornblende known as smaragdite and actinolite, while the separated iron-oxides crystallize by them- selves. On the alterations by weathering of the felspars and other acces- sory minerals of the peridotites it will not be necessary to dwell in detail, as they are not essential minerals of the peridotites. § 2. Varieties oF THE PaLmozorc PERIDoTITES. Of all the varieties of the peridotite which we have described as occurring among the intrusive rocks of Tertiary age, representatives are found among the more or less altered Paleozoic igneous masses. Rocks like the dunites, which are composed almost entirely of olivine, are by hydration converted into serpentine, and some of the very pure serpentine masses of Scotland were in all probability originally dunites. But since enstatite, as we have already seen, is, like olivine, also converted into serpentine, though somewhat more slowly, masses of pure serpentine may be formed by the hydration of olivine-enstatite rocks like lherzolite. Admirable examples of such altered olivine-enstatite rocks have been described by Professor Bonney as occurring not only at the Lizard in Cornwall but at Colmonell in Ayrshire . My own exami- nation of slices taken from this serpentine leads me to conclusions * Amer. Journ. Sci. ser. 3, vol. xxviii. p. 264. + In some eases this conversion of augite into hornblende takes place directly, the dichroic hornblende appearing, as it were, eating into the non-dichroic augite. But in other cases the whole augite crystal appears to be converted into uralitic and fibrous hornblende, and this may change subsequently into eommon hornblende. t Quart. Journ. Geol. Soe. yol. xxxiy. (1878) p. 769. OLDER PERIDOTITES OF SCOTLAND. 399 identical with those arrived at in this paper concerning the rocks in question. An equally striking example of a rock of the same class occurs in Forfarshire, near the town of Kirriemuir. This rock’ was described in the year 1825 by Sir Charles Lyell, after studying it with the assistance of Dr. Buckland, as a mass of serpentine forming a dyke which intersects the Old Red Sandstones and contemporaneous volcanic rocks of the district *. In 1875 I had the advantage of studying this mass of serpentine under the guidance of Sir Charles Lyell. The dyke of serpentine can be traced running for a length of at least 14 miles, in an H.N.E. and W.S.W. direction, near the southern foot of the Grampians, and parallel to that range; it is well exhibited in several deep cavities, cut by streams descending from the mountains, especially those of the Carity, the Prosen, and the South Esk. The dyke varies in width at different points from 100 to 300 vards; it encloses “horses” or masses of the rocks traversed by it, and is itself intersected by other intrusive rocks. It produces marked alteration on the rocks which it traverses f. At its sides the rock is a mass of serpentine, traversed by nume- rous veins of chrysotile and exhibiting no evidence of the minerals of which the rock was originally formed. But towards the centre, crystals of ‘‘ Schiller spar” make their appearance, and the serpen- tine gradually passes into a hard crystalline mass which Lyell com- pared with the rock of the Cuchullin Hills, and called hypersthene- rock. Studied by the aid of the microscope, this central and least weathered part of the dyke is seen to be made up of serpentine, clearly pseudomorphous after olivine, and containing large crystals of a ferriferous enstatite in a more or less advanced stage of alteration into bastite and serpentine. In some portions of the central mass of the dyke the ferriferous enstatite prevails almost to the exclusion of the olivine, and we have a rock strikingly resembling the bronzite- rock of the Kupferberg, near Bayreuth, and of St. Stephan in Upper Styria (see Pl. XIII. fig. 7). This is a type of rock which has not, I believe, been hitherto recognized in the British Islands. As we trace the rock outwards from the central mass, the alteration becomes greater, till at last all traces of the individual enstatite- erystals disappear, and we have a serpentine in which no vestige of the original mineral constituents of the rock can be distinguished. Among the dykes which intersect the great serpentine-mass, I found one to consist of a coarse dolerite or augite-gabbro, while another is a very beautiful example of a hypersthene- (ferriferous enstatite) dolerite. . The serpentines with altered bronzite, from the neighbourhood of Aberdeen ¢, are also altered olivine-enstatite rocks. When the older peridotites contain a considerable proportion of * Edinb. Journ. of Sci. vol. iii. (1825) p. 112. + Tam much indebted to Leonard Lyell, Esq., F.G.S8., of Kinnordy, for several interesting series of specimens which he has sent me from this district, t See Heddle, Mineralog. Mag. vol. v. pp. 4-6. 400 - PROF, J. W. JUDD ON THE TERTIARY AND augite, this mineral remains enclosed in the serpentine, or is con- verted into hornblende. In the latter case we have a rock of the same class as that described by Professor Bonney, from North Wales and the Lake district*, as hornblende-picrite. Two examples of such altered picrites have been described 1 in the neighbourhood of the Firth of Forth. The picrite which forms an eminence on the S.W. of the island in the Firth of Forth was discovered by Mr. Adie, and described first by Dr. A. Geikie 7, and subsequently by its discoverer een A Wal?) rock may be classed with the picrites, though it sometimes contains a, not inconsiderable proportion of felspar. It is an interesting cir- cumstance that the olivine of this rock 1s sometimes only slightly serpentinized. The augite is sometimes quite intact, but is some- ‘times seen passing into brown hornblende. Some of the hornblende of this rock, however, may be original. The association of augite, hornblende, and biotite in the rock is of the closest kind, but it is difficult to say whether this association, in certain cases, should be interpreted as due to intergrowth or to paramorphic changes. I have been kindly suvplied by Mr. T. Waller, of Birmingham, with the following analysis of this beautiful rock :— STULTCH Reeaetans tetra lor aiet Menai ata ahs Mie BOuee ACLUTTNTT GUS) tees reckich al 6 itera aatte lamest 9°7 Merrie OXAGC petits Mann Mane an 3°4 Rertousnoxider eer, siadrie der 70: HLA etd eu ee Pee a a 4°] INI A fern S1SU I ay SNe eR Ae ee NOND Hiy Oe ZH) Soda (with trace of potash) .... 0:8 OsSOn WO MEAOI a Le. ee yep fcr cae 14-0 99°7 As leucoxene occurs among the alteration-products in the rock, titanic acid is certainly present; it was not, however, specially determined in the analysis, and it has therefore been included in part with the silica and in part with the alumina. The specific gravity of this rock is 2°81. The picrite of Blackburn, near Bathgate $, which has also been described by Dr. A. Geikie, resembles that of Inchcolm in its mineralogical constitution, but is of especial interest to geologists on two grounds. If the interpretation given of the relations of this rock be a correct one, it affords an example of an ultrabasic rock occurring as a lava-stream, and at the same time illustrates the possibility of the heavier minerals in a lava sinking to the bottom of it, so as to cause the lower portions of the stream to be of more basic character than its upper part. There is one of the older peridotites of Scotland, however, which * Quart. Journ. Geol. Soc. vol. xxxvii. (1881) p. 137, and xxxix. (1883) p. 254. + Trans. Roy. Soc. Edinb. vol. xxix. (1880) pp. 507, 508 t Cole’s Studies in Microscopical Science, vol. i. (1882) p. 45. § Trans. Roy. Soc. Edinb, vol. xxix. (1880) pp. 504-507. OLDER PERIDOTITES OF SCOTLAND. 401 presents so many peculiar characters that it appears to me to be worthy of special description. In some respects it appears to differ from any rock of the class that has previously been described. § 3. Tur ScyELire (ArtTERED Mica-HornBLenbDE-PicritTE) oF CAITHNESS. This rock is of so remarkable a character and affords so many striking illustrations of the principles enunciated in the foregoing pages, that a detailed description of it seems to be called for. It occurs as a boss rising above the thick mass of glacial gravels on Achavarasdale Moor, situated in the Reay country in the west of Caithness, near to where that county borders on Sutherland. It appears first to have attracted attention about fifteen years ago, when Sir Robert Sinclair and Mr. Tait noticed its peculiar appearance, and brought specimens of it to Thurso to submit to the late Robert Dick. Mr. David Gunn, of Thurso, and Mr. John Gunn, of Dale, near Halkirk, have taken much interest in this peculiar rock and its surroundings, and have sent specimens of it to different museums and to geologists in various parts of the country. To the former gentleman J am indebted for a carefully constructed plan, showing the dimensions and positions of the singular rock-mass, with a series of specimens taken from different parts of it; to the latter I am under the very greatest obligation for specimens of the material in the best state of preservation and for much valuable information collected with much care and patience. The boss of highly glittering rock, which is said to rise about 10 feet above the general level, is about 9 yards long from 8.W. to N.E. and about 73 yards broad from N.W.to8.E. It issurrounded by a mass of disintegrated fragments derived from the same rock, which extends over a nearly circular area about 25 yards in diameter; excavation to the depth of 5 feet in this disintegrated material failed to reach the solid rock. The bright silvery scales so abundant in the rock and the soil derived from it, together with the covering of grass with which it is clothed, make the boss a very conspicuous object in the midst of the heath-covered moor. Prof. Heddle states that the rock which surrounds the boss on all sides is a ‘‘syenitic gneiss ;” but owing to the thick covering of drift- gravel the actual junction between the two rocks has not been reached in any of the excavations that have been made. Carefully selected specimens of the rock were sent to Mr. Hugh Robert Mill, B.Sc., F.1.C., and by him were submitted to chemical analysis in the laboratory of the University of Edinburgh. J have that gentleman’s permission to publish the results which he obtained. Three more or less complete analyses of the rock were made, giving the following results : — 402 PROF. J. W. JUDD ON THE TERTIARY AND I. TI; ELE. SL) eee oe Be De cates c 41-74 42-17 42-04 Total iron as ferric oxide ...... 11°58 10°36 10°92 Ala. co ee eee ec icens ot 3°08 3°97 3°48 Magnesia (..cereer eee ce tens. n00- 26°83 30°65 INE), oe re niet oe sie Sek 4°75 3°77 Manganous oxide ................+. “70 ‘ Soda and potash ...............00 4°85 1-90 Water and carbonic acid......... 7°78 7:19 767 IRELEGHS ONGC. 5.5.cs2.-0c-s5) a Re 38:0 Alumina 9022. Sas. 2k ae eet ley) Tron oxide calculated as ferric oxide 4-5 JOTONE co oh eer tin RCERMR Soynk n 5:0 GIGASET separa Sane Re tie ae 24-0 VCR ie AE aie cp eae. oo aa 6:5 404 PROF. J. W. JUDD ON THE TERTIARY AND It will be observed that this analysis differs from that of biotite, the only uniaxial mineral which suggests itself for comparison, by the low proportion of ferric oxide (which is only to some extent compensated for by the higher alumina-percentage), by the large proportion of lime and water, and the probably low percentage of the alkalies. Under these circumstances it became necessary to make as accurate an examination of the optical properties of the mineral as was possible, and in doing this I had the great advantage of the advice and assistance of Mr. L. Fletcher. Flakes of the mineral were mounted in Canada balsam, and examined by means of a microscope constructed by Nachet, of Paris, on the pattern described by MM. Fouqué and Michel Lévy*. This microscope has the great advantage of permitting the interference-figures, exhibited by the polariscope with the converging system of lenses of Bertrand and von Lasaulx, to be examined even with the highest powers. We found in this way that not only was the mineral practically uniaxial, but that even when compared with other so-called uniaxial crystals, like the Vesuvian meroxene, for example, the interference- figures indicate an excessively small axial angle. ‘The only mica with anything like so small an axial angle which we were able to find was a remarkable pale-coloured, silvery biotite from Easton, in Pennsylvania, which does not appear to have been analyzed, though its optical characters have been described by Blake7. In the determination of the other minerals in the rock, far less difficulty was experienced. The most abundant constituent of the rock, as seen in thin sections under the microscope, was found to be a green hornblende. In the | greater part of the rock the characters of this mineral were clear and unmistakable. By transmitted light its colour is a very pale green, and its pleochroism, though distinct, was by no means vivid. Basal sections afforded the means of measuring the angle of the principal cleavages as exhibited in well-marked cleavage cracks, and left no doubt as to the species of the mineral, and this is confirmed by its extinction-angle. In many places the hornblende is very clear and fresh-looking, and free from inclusions of all kinds except the grains of magnetite scattered through it. But in places this pale green mineral exhibits traces of the peculiar tabular inclusions of diallage, and in such portions of the crystals the extinction-angle indicates that we are dealing with an augite rather than with a hornblende. The conclusion to which I am led by the study of a large series of preparations of this rock is, that the mineral was originally augite, that it was by Schillerization converted into diallage, and that subsequently this diallage was amphibolized. In many slices of the rock, however, the mineral is a perfectly clear and , fresh-looking hornblende, and exhibits no trace of its secondary origin. Enclosed in the hornblende, and often penetrating into its fissures, * Minéralogie Micrographique (1879), p. 27. t+ Amer. Journ. Sci. vol. xii. (1851) p..6. OLDER PERIDOTITES OF SCOTLAND, 405 is a dark-green serpentine. Examined with high powers of the microscope, this serpentine is seen to be filled with black and brown enclosures, some rod-like and stellate in form, others of a tabular character. Sometimes these inclusions are arranged in one set of parallel planes only; in other cases they lie in two sets of planes intersecting one another. There can be no doubt that much of this serpentine is pseudomorphous after olivine; but some of it may replace enstatite. The micaceous mineral presents very different conditions in different portions of the rock. Most frequently it appears to have been changed into a creamy yellow, amorphous substance, which by polarized light shows all the characters of an alteration-product ; but in the fresher examples of the rock it exhibits the peculiar outlines and the strong basal cleavage of a mica. From ordinary biotite, however, it is distinguished at once by its pale colour, a faint buff-yellow, and its feeble pleochroism, which is, however, sufficiently well marked to be unmistakable. In places the fresher part of this mineral is rendered black and almost opaque by the abundance of tabular inclusions which it contains; these appear to be arranged in planes parallel with the basal plane, that is to say in the direction of the principal cleavage. The distribution of these inclusions is strikingly local, some parts of the mica crystals being almost entirely free from them, while in adjoining portions they have become so frequent as to entirely destroy the translucency of the crystal. Small grains of magnetite are found scattered through all the minerals of the rock; but of accessory minerals there are only a few traces. Very rarely indeed could any minerals be detected which might be regarded as u'teration-products of felspar. By drawing, with the aid of a camera-lucida, the outlines of the crystals in a section of the rock, and cutting out and weighing the fragments of paper representing each mineral, an estimate was formed of the proportions which the several minerals bore to one another in the rock. The operation, repeated in the case of a number of sections, so as to afford a good general average, gave the following percentages :— Hornplende.". .'. 2205 2208'S MermeHlane t's mene. 22-0 Miferedmieay’ . 6). Usa. 2 18°5 Magnetite and accessory : 1:0 UMMC ERISO neice es This result appears at first sight very different from what might be expected from a macroscopic inspection of the rock, which would lead one to regard the conspicuous mica as the predominant con- stituent. But minerals with a strong cleavage like mica are very apt to make a much greater show on fractured rock-surfaces than their actual abundance in the rock entitles them to do. The microscopic structure of the rock is a very marked one. The hornblende-crystals enclose rounded grains of serpentine and crystals Q. J Gas. No. 163. 2F 406 PROF. J. W. JUDD ON THE TERTIARY AND of mica. The hornblende occupies precisely the same relation to these minerals as the augite does to the olivine in the peridotites of the Shiant Isles. The structure of the scyelite is therefore distinctly ophitic. The study of this rock leads to the conclusion that, in spite of the clear and fresh appearance of most of the minerals of which it is made up, they are all of secondary origin. The hornblende is a paramorph after augite, some at least of which had been previously converted into diallage. Very similar hornblende occurs in some examples of the picrite of Schriesheim, and this rock exhibits, as Professor Bonney observes, TIES gradation from augite to hornblende # cay cecute serpentine of the rock clearly replaces olivine, and in some cases probably enstatite also, as is indicated by the peculiar nature of the enclosures, which often persist and retain their form after the hydration of the enclosing mineral. Whatever the micaceous mineral should now be called, it appears to have been originally a highly magnesian biotite, that is to say an approximately uniaxial mica. Its pale colour and feeble pleochroism appear to be clearly related to the low percentage of iron which it contains. Another peculiarity in this micais probably thereplacement of much of the alkalies by basic water. How far these peculiarities of the mineral are original, and how far they are of secondary origin, it may be difficult to determine. The abundant tabular enclosures in the mineral point to the conclusion that Schillerization, or the dis- solying-out of the iron and its collection into the hollows of negative crystals, has gone on to a considerable extent. It was probably at the first a biotite, very rich in magnesia and poor in iron, with the potash largely replaced by basic water; but some of the iron and the alkalies have not improbably been removed during the process of Schillerization. That such biotites with a low percentage of iron not unfrequently occur in the ultra-basic rocks is highly probable. I have found a mica similar to that of the scyelite in several altered peridotites, among others some varieties from Schriesheim. The mineral may easily be mistaken for an altered enstatite, from its optical properties. Dr. Heddle has analyzed a mineral occurring in the serpentine of Milltown, Glen Urquhart t, which appears to be analogous to the biotite of the scyelite. The mineral is stated to be pale green or nearly white in colour, to have a specific gravity of 2°781, and to be associated with large pale crystals of hornblende. The analysis is as follows :— * Quart. Journ. Geol. Soc. vol. xxxix. (1883) p. 256. [Professor Cohen has recently pointed out that the mineral formerly taken for diallage in the Schriesheim picrite is really hornblende (Neues Jahrb. fur Min. 1885, vol. i. p. 242). + Trans. Roy. Soc. Edinb. vol. xxix. (1880) p. 18. OLDER PERIDOTITES OF SCOTLAND. 407 SIGE) fo. |... 2 Seg ans « 40°307 ja JTL 016 a! od coc’ ce 12°582 Remade oxide.’ .’ yee. 3S 1°809 IREBEDUS OX1GG. . — 2 eee cas. < 3°O00 iManbanous oxide’ 72.2 a+ 0:384 MC. Soa |. x se ee 7-581 Mrevesta, oS i a eeeeeeee ere 21-000 OUISI s . ce lo ee 6°561 POGd) cs ea. Ses Cee 0-953 Water. oto i ae 5°730 100-250 The small proportion of the iron-oxides and the quantity of lime suggest a resemblance to the mineral of the scyelite. This pale- coloured mica is said to pass into a lustrous brown variety of ordinary biotite, containing 4°913 per cent. of ferric oxide and 19°802 of ferrous oxide. Nowhere perhaps would it be easy to find a better example of the different changes to which the minerals of igneous rocks are subject. If our interpretation be correct, the scyelite was originally a picrite with well-marked ophitic structure, made up of augite, enclosing and intercrystallized with grains of olivine, with some enstatite, to which was added a considerable quantity of a highly magnesian biotite. The first change to which this rock was subjected was clearly due to deep-seated action, and resulted in the conversion of a part, at least, of the augite into diallage, in the development of tabular and other enclosures in the olivine and enstatite, and in a similar change in the biotite. Subsequently to this, and under totally different conditions, a new set of changes was brought about in the rock. The augite was converted into hornblende, the olivine and enstatite into serpentine, and the mica became more or less hydrated, losing in some parts of the mass its physical and optical properties. Yet during all these changes the form and relations of the original minerals were not destroyed, and in the later alterations the structures produced by the first set of changes were so far spared as to admit of our deci- phering the history of this singular rock. SuMMARY oF RESULTS. From the observations described in the preceding pages, it appears that many rock-forming materials may be made to assume new and unfamiliar aspects by the development of enclosures along certain planes within their crystals. In this way the augites are converted into diallages and pseudo-hypersthenes, and the ferriferous enstatites into bronzites and the varieties to which the name of hypersthene was originally applied ; similarly, olivine passes into a black, opaque, fissile mass, which has frequently been taken for magnetite, and the felspars acquire avanturine and chatoyant characters. For the process 2H 2 408 PROF. J. W. JUDD ON THE TERTIARY AND by which this change has been brought about, the name of “ Schilleriza- tion” is proposed, and diallage and common hypersthene are shown to be Schillerized forms of augite and ferriferous enstatite respec- tively. In the case of some minerals, and notably the rhombic pyroxenes, the altered forms are much more familiar to minera- logists than the unaltered. The enclosures which exist in these Schillerized minerals, giving rise to their peculiar colour, lustre, and sheen, are of the nature of negative crystals, more or less completely filled with products of decomposition, such as hydrated silica and hydrated ferric oxide. When these isotropic mixtures fill the whole cavity of the negative crystal, the enclosures appear to have definite crystalline forms ; - in many instances, however, they form patches with more or less irregular outlines, partially filling the hollow of the negative crystal ; and sometimes the crystalline forces have come into play and have caused them to assume “ dendritic” forms within the cavities where they are deposited. These negative crystals, with their contents, vary greatly in size, from objects visible to the naked eye down to such as can only just be recognized by the highest powers of the microscope, while there are probably others which are ultramicro- scopic in their dimensions. The production of the Schillerized condition in minerals is shown to be related to the depth at which the crystals have originally existed in the great central cores of the Hebridean volcanoes. The Schillerized forms of the minerals are only found in deep-seated intrusive rock-masses ; but the converse of this statement is not true, for in deep-seated rocks this change is sometimes evidently local, and some of the crystals may have altogether escaped it. The degree = of Schillerization increases also with the depth at which the rock has existed. An efficient agent for the production of this Schillerization, that is the formation of negative crystals and their more or less complete infilling with decomposition-products, is pointed out in the solvent action of heated water and other fluids acting under great pressure. This solvent action takes place most readily along certain planes within the crystal, and these directions of greatest susceptibility to chemical action differ from those of easiest fracture (cleavage-planes) ; the positions of such planes are perhaps also dependent to some extent on twin-structure, facts for which we were prepared by the closely related phenomena of the Aetzfiguren. We have here, in fact, the phenomena of the Aeizfiguren seen in three dimensions—that i is to say, displayed in a solid instead of on a surface. In some cases the secondary products contained in the negative crystals seem to be derived from the mineral in which the hollows occur; in other cases, as in the felspars, it is clear that they must have been, in part, brought from outside the crystals affected. The partial solution of minerals which results in the formation of negative crystals within them often brings about great changes in the colour, in the pleochroism, and in the positions and relations of the optic axes of the original crystals. It is probable that the iron- OLDER PERIDOTITES OF SCOTLAND. 409 silicates are among the first to be attacked by the solvent agents, and the products formed by their decomposition are the first to be de- posited within the negative crystals. To the same cause, the presence of water and other liquids under pressure, we must assign the formation of a network of cavities along fissures of the crystals of rock-forming minerals, these cavities containing, in some cases, liquids with bubbles, and in others solid substances which have crystallized within them. While these networks of cavities sometimes lie along actual ‘fissure-planes in the crystal, in many other cases they form bands traversing the crystal where no actual rupture can be seen to have taken place. These bands of cavities probably indicate portions of the crystal which have been in a condition of intense strain, along which, according to a well-known physical law, solvent agencies operate with greater force than elsewhere. The same band of enclosures (marking a plane of strain) is often found traversing a number of adjoining crystals in a rock. The change by which certain felspars acquire their beautiful play of colours is analogous to that by which the avanturine appear- ance, or Schiller, is acquired; but the former alteration appears to be an ultramicroscopic one. It probably consists of the development of thin plates of hydrous silica in a set of parallel planes within the erystal. Like the Schiller structure, it is characteristic of minerals which have formed parts of deep-seated rocks. . The twin-lamelle found in most plagioclase felspars appear not to be necessary and originel structures of the crystals, but to have been developed in them by strain, like the similar twin-lamelle in the rock-forming calcites. While some of these twin-lamelle are probably produced by the stresses and strains set up during the cooling of a crystal after its first formation, as was illustrated ex- perimentally by Foerstner, others among them are clearly of long subsequent date to the consolidation of the rock, and have been developed by the mechanical forces which have affected the whole rock-mass leading to the formation of cracks in the crystals which compose it. By Schillerization the most striking mimicry of one mineral by another may be produced. Thus the first stages of the Schillerization of the monoclinic and rhombic pyroxenes are diallage and bronzite respectively, minerals which have been constantly mistaken for one another; by a further change the same minerals may in turn pass into pseudo-hypersthene and true hypersthene, minerals which present the most striking similarity in their colour, lustre, and also in their general aspect, when viewed in thin sections, and can only be distinguished by their optical properties. All the minerals, whether in their normal’form or in their Schil- lerized condition, may be converted into their pseudomorphs; and this change is not always a molecular one only (paramorphism), but is sometimes accompanied by hydration due to the action of water penetrating from the surface or by other changes in their compo- sition. Under such conditions augite is converted into hornblende, A410 PROF. J. W. JUDD ON THE TERTIARY AND enstatite into bastite, and olivine into serpentine. These changes, which are quite distinct in their nature and their origin from Schillerization, may be greatly modified, however, by the alteration, due to deep-seated action, which the minerals have previously un- dergone. As diallage is only an altered form of augite, it is impossible to maintain as a separate class rocks whose only distinction is the presence of that variety. Hence, as many petrographers have admitted, it becomes difficult to accept the mineralogical distinc- tion between gabbro and diabase. The name gabbro is so con-. venient, that its retention is advocated for all the most perfectly holocrystalline (granitic) varieties of basic rocks, whether the augite is in its normal condition or its Schillerized form (diallage). The - name diabase may be more conveniently employed for altered forms of dolerite. In many cases the process of Schillerization has resulted in the conversion of the olivine into a black and opaque substance, often mistaken for magnetite. Many of the gabbros supposed to contain no olivine in reality have their olivine in this curiously altered state. The class of the olivine-gabbros is much larger than is usually supposed, and the group of gabbros without olivine is proportionally restricted. It has been shown that in the Western Isles of Scotland there exists a series of ultra-basic rocks of Tertiary age which exhibit all the essential features of the ultra-basic rocks of pre-Tertiary age, and like them may be classed under the varieties of dunite, lherzolite, picrite, eucrite, and troctolite. These rocks are most intimately associated with the gabbros and dolerites of the district, an | association which finds an exact parallel in the case of their older representatives. The study of the remarkable changes which the minerals of these rocks undergo, as they are traced to successive depths from the original surface, is greatly facilitated by the fact that, in consequence probably of the late period of their eruption, they have suffered but little from agents acting from the surface. In many cases the felspars exhibit no trace of kaolinization, the augites are fresh and show no signs of uralitization, and the olivines are not in the least serpentinized ; thus the changes which are due to the action of deep- seated waters are not in the least degree complicated with, or concealed by, alteration of a totally different character and origin. But in the masses of peridotite of Paleozoic age which are scattered about Scotland quite opposite conditions prevail. The dunites are converted into serpentine-rock, the lherzolites into bastite-serpentine, the enstatite-rocks into bastite-rocks, and the augite-picrites into hornblende-picrites. But, in all these cases, a careful study of the altered materials shows that originally they were identical in mineralogical constitution and in structure with the peridotites of Tertiary age. In the scyelite of Caithness we have a very interesting example OLDER PERIDOTITES OF SCOTLAND. 411 of an ultra-basic rock of a new and hitherto undescribed type. It was originally a mica-picrite with strongly marked ophitic structure, and exhibits evidence of some of its minerals having undergone Schillerization ; but at the present time all the original minerals are represented by their pseudomorphs—augite by hornblende, olivine ~ and enstatite by serpentine, and biotite by a curious hydrated form of that mineral. The recognition of certain characters in the rock-forming minerals as being original and essential, and the distinction of such from other characters which are secondary and accidental, is of the highest importance to the petrographer and geologist, and not less so to the mineralogist. Rightly studied, these minerals are capable of furnishing the geologist with evidence not only concerning the mode of origin of the rocks of which they form a part, but also of the changes which they have undergone since their first formation. The study of the minerals included in the crystalline rocks is not less important. than that of fossils in the sedimentary rocks. And to the mineralogist the study of the secondary characters of minerals, and of the causes which have produced them, is equally necessary. Researches of this kind, indeed, can scarcely fail in the end to reduce many so-called mineral species to the rank of accidental, though still highly interesting, varieties. But of still greater impor- tance is the recognition of the fact that the investigation by the aid of the microscope of the processes by which minerals have acquired their several characters, and the consequent tracing of the evolution of mineral species and varieties, is calculated to raise mineralogy from its present rank as a merely classificatory science, to infuse it with new life, to open out to it new realms of research, and to invest it with a higher importance than is at present accorded to it in the family of sciences. EXPLANATION OF PLATES X.-XIII. Puate X. [Norz.—Some of the details of these figures can only be distinctly seen by employing a low-powered magnifier. | Fig. 1. A crystal of felspar from a gabbro-vein traversing dunite at Scuir na Gilean, Isle of Rum, viewed by polarized light with a magnifying- power of 35 diameters. This crystal admirably illustrates the con- clusion that the lamellar twinning must be regarded as a secondary character of the plagioclase felspars. A large portion of the crystal is quite free from any trace of the lamellar twinning. The crystal is traversed by a number of cracks, and between the cracks, lamellar twinning is seen in some cases to be developed. An examination of the relations between the fissures and the lamellar twinning is con- clusive as to the non-existence of many of the twin-structures before the formation of some of the fissures which traverse the crystal. This section also illustrates the manner in which lamellar twinning is frequently developed along two different sets of planes in plagio- clase felspar, and that these two sets of twinnings sometimes inter- sect one another. The way in which these twin-lamelle are found starting irregularly at certain points in the crystal, and dying away 412 Fig. 2. PROF. J. W. JUDD ON THE TERTIARY AND in the untwinned portions, like the similar twin-structures artificially produced in calcite, is also seen. Some of these twin-structures may have been developed by the strains set up in the cooling-down of the crystal, others were probably induced by the movements in the rock- mass which produced the fissures in the crystals that built it up. (See pages 364-366.) Section of felspar in troctolite from Halival, Isle of Rum. Magnified 225 diameters. This crystal exhibits the jirst stages of alteration in the felspars. It is traversed by numerous cracks, and along these, as well as in other parts of the crystal, many liquid- and gas-cavities have made their appearance. Some of these cavities, which are of considerable size, are particularly interesting from the fact that they are seen by their regular forms to be negative crystals. In some cases the infilling of these cavities with solid substances has clearly commenced. (See pages 375, 376. . Section of felspar from the olivine-gabbro of Loch Coruiskh, Isle of Skye. Magnified 225 diameters.. This felspar is in a more advanced state of alteration. The cavities lying along lines of fissure or strain are much more numerous and are in almost all cases filled with dark- coloured products of decomposition. In addition, we see the first traces of very minute dark-coloured tabular enclosures (negative crystals filled with decomposition-products) making their appearance along one set of parallel planes within the crystal. (See page 376.) . Section of felspar from the olivine-gabbro of Ardnamurchan. Magni- fied 225 diameters. This section shows bands of cavities, some of which are partially filled with solid materials, and two series of tabular enclosures (infilled negative crystals) arranged in two sets of parallel planes which intersect one another nearly at right angles. (See page 376.) . Another section of felspar from the same rock as the last, showing the enclosures arranged in two sets of planes, as in the former example, with the addition of a third series intersecting them. This section is also magnified 225 diameters. (See page 376.) . Section of felspar from the olivine-gabbro of Loch Coruiskh. Magni- fied 225 diameters. This shows irregular enclosures filling cavities which lie along cracks and scattered irregularly through the crystal ; also tabular enclosures arranged along no less than jive different intersecting planes in the crystal, namely, two pinacoidal, two pris- matic, and one basal. The first four are seen in section, the last in plan. Besides these there are cloudy patches in the crystai, which the highest powers employed are only partially capable of resolving into similar but much more minute enclosures. (See page 576.) . Section of an excessively altered crystal of felspar from the olivine- gabbro of Ardnamurckan. Shown with a magnifying-power of 225 diameters. The whole of the felspar exhibits a rich brown tint from the abundance of foreign enclosures which have been developed in it. These enclosures form nebulous-brown patches, which, with the very highest powers of the microscope, can only be partially resolved into irregular solid particles lying in cavities of the crystal, and tabular or bacillar enclosures, filling negative crystals and developed along a number of planes within the felspar. In other portions of the section, the enclosures are sufficiently large to be rendered visible by the power employed. A further concentration of the decomposition- products has taken place in places, leading to the formation of dendriti- form accumulations of the iron-oxides, &. Although the crystal is so greatly altered, the characteristic lamellar twinning can be observed in certain portions of it with the aid of the polariscope. This lamellar twinning has evidently influenced the action of the solvent forces in eating out negative crystals along certain planes, and in infilling them with decomposition-products. This example affords an easy transi- tion to the chatoyant felspars, in which the secondary structures are ultra-waicroscopical. (See pages 376, 377.) OLDER PERIDOTITES OF SCOTLAND. 413 & Puate XI. Fig. 1. Fissures and incipient fissures in the very fresh brown augite of the ophitic dolerite from the Shiant Isles, showing the development of a reticulation of cavities along the lines of fracture and strain within the crystal. Most of these cavities are empty, or contain liquids in which bubbles may sometimes be discerned; but a few of them appear to be filled with solid substances. These cavities are very minute; they are eee seen with a magnifying-power of 500 diameters. (See page 378.) 2. More altered brown augite from the picrite of central Rum. The cracks and bands indicating strain are more numerous than in the last example, and are marked by lines of cavities of much larger dimensions, the cavities being in almost all cases filled with solid decomposition-products which are dark-coloured and opaque. The section is shown as displayed by a magnifying-power of 75 diameters. (See page 378.) 3. Two crystals of augite from the olivine-gabbro of Loch Coruiskh, Isle of Skye, showing the conversion, to a different extent in the two cases, of this mineral into diallage. The action by which enclosures are developed along planes parallel to the orthopinacoid is clearly seen to be set up from the outer surface of the crystal. The central parts of the crystal have all the characters of ordinary augite, while the peripheral portions are converted into true diallage. The objects are figured as seen with a magnifying-power of 50 diameters. (See page 379.) A. Crystal of true diallage (foliated augite) from the olivine-gabbro of - Beinn More, Isle of Mull. At one end of the crystal the develop- ment of another series of enclosures along the clino-pinacoid has commenced, converting the crystal into pseudo-hypersthene. Seen as magnified 100 diameters. (See page 379.) 5. Portion of crystal of augite from the olivine-gabbro of Loch Coruiskh, Isle of Skye. This example shows that the development of enclosures takes place most abundantly along lines of cracks and in their imme- diate vicinity. ‘Two sets of enclosures are in course of development in this case—one parallel to the orthopinacoid, and the other parallel to the clino-pinacoid. Seen with a magnifying-power of 75 diameters. (See page 379.) 6. Structure of the pseudo-hypersthene from the olivine-gabbro of Loch Coruiskh, Isle of Skye. Represented as seen with a magnifying- power of 225 diameters. Two sets of enclosures are seen in section, lying in planes nearly at right angles to one another. A third much less perfect series of enclosures, with irregular outline, is ex- hibited lying probably parallel to the basal plane. (See page 380.) 7. Crystal of highly ferriferous enstatite (amblystegite) from the olivine- gabbro of Loch Coruiskh, Isle of Skye. The crystal exhibits only the first traces of Schillerization. It exhibits the very strong pleo- chroism and the rhombic extinction characteristic of the species to which it belongs. Cavities filled with solid enclosures are developed in great numbers along the lines of crack, and a few tabular en- closures are developed along one set of parallel planes, so that the mineral is seen to be passing into the bronzite-modification. The crystal is shown magnified 30 diameters. (See page 380.) 8. Crystal of altered ferriferous enstatite, enclosing both felspar and diallage, from the olivine-gabbro of Loch Coruiskh, Isle of Skye. ‘The crystal is slightly serpentinized in places. This crystal exhibits the bronzite-modification over the greater part of the section, one very conspicuous series of enclosures, seen in section, being well developed in it; but here and there a second set of enclosures, also seen in section, and a third, viewed in plan, are also exhibited. The crystal therefore illustrates the transformation of the bronzite- modification of enstatite to the hypersthene-modification. Mag- nified 100 diameters. (See page 380.) 414 PROF. J. W. JUDD ON THE TERTIARY AND Fig. 9. Section of a crystal of typical hypersthene from Labrador, seen with:a magnifying-power of 30 diameters. Three sets of tabular enclosures, which are of extraordinary dimensions, are seen in this section, two in section and one in plan. One set of enclosures, seen in section, 1s very persistent over the whole area; a second, nearly at right angles, is developed along certain bands, probably of strain; and the third, seen in plan, are also crowded along the same lines. ‘The en- closures seen in plan have often one straight edge (due to the limits of the negative crystals in which they are developed); but on the other sides they are irregular in outline, owing to the secondary materials of which they are formed not entirely filling the negative erystal. The material of the crystal in which these enclosures lie has lost nearly every trace both of colour and of pleochroism. (See page 380.) Puate XII. .Fig. 1. Represents the surface of a crack traversing a crystal of olivine in the gabbro of Halival, Isle of Rum, as seen with a magnifying-power of 225 diameters. The irregular cavities sometimes contain a liquid and bubble, and at other times are empty; more usually, however, they are filled, to a greater or less extent, with dark-coloured, solid materials which appear to be decomposition-products. By the use of very high powers and special means of illumination fine reticulating tubules can be detected uniting many of these cavities. (See page 382.) 2. Shows the surface of a crack traversing an olivine crystal in the picrite of central Rum. In addition to cavities filled with decomposition- products, we find a beautiful dendritic network of magnetite and other oxides, spreading itself over the surface of the crack. The object is shown as it appears with a magnifying-power of 100 dia- meters. (See page 382.) 3. Portion of crystal of olivine from the picrite of central Rum, magnified 50 diameters. Showing enclosures along cracks filled with solid substances, as in fig. 1; dendritic ramifications of magnetite over the planes of cracks, as in fig. 2; and, in addition, numerous en- closures in negative crystals arranged in a series of parallel planes: traversing the crystal. (See page 382.) 4. Very large and beautiful examples of the stellate bodies lying within the negative crystals in olivine, from the picrite of Halival, Isle of Rum. Magnified 75 diameters. In the crystals on the left, the stellate en- closures are viewed in plan and their forms are well seen; in the crystal on the right they are greatly foreshortened. When the plane of the section is at right angles to that of the plane parallel to which the negative crystals lie, the enclosures appear as fine dark lines. ‘This section also shows the lines of cavities filled with solid substances passing along cracks in the olivine-crystals. (See page 382. 5. A ee of examples of very fine and large stellate enclosures in olivine from the picrite of Halival, Isle of Rum. Magnified 225 diameters. (See page 385.) 5a. Illustrates the first stage in the formation of the stellate enclosures in the negative crystals in olivine. The ramifying rods of magnetite &c. are assuming a radiate arrangement, but have not united with one another. 5b. Shows a very large and perfect stellate enclosure ; the edges have not extended to the limits of the negative crystal, and therefore are not bounded by regular lines. 5¢. Shows two stellate enclosures, the growth of which has been interfered with by the sides of the negative crystal. They also illustrate the tendency of the stellate enclosures to pass into tabular ones by additional deposits between the rays of the star. 5d. Illustrates the effects of foreshortening on the apparent forms of these stellate enclosures. OLDER PERIDOTITES OF SCOTLAND. 415 Fig. 6. Crystal of olivine, with magnetite developed along the cracks and in- vading the substance of the crystal. In addition stellate enclosures of magnetite &c. are making their appearance in negative crystals arranged in a series of parallel planes traversing the crystal. From the troctolite at the top of Halival, Isle of Rum. Crystal shown magnified 100 diameters. (See page 383.) 7. Portion of a crystal of olivine in which magnetite has been developed along the cracks to such an extent as to render black and opaque nearly the whole crystal. Portions of the olivine-substance, partially converted into serpentine, remain here and there in the midst of the mass. From the olivine-gabbro, Beinn More, Isle of Mull. Shown magnified 50 diameters. [In the same rock many of the olivine- crystals are seen rendered altogether black and opaque by the de- velopment of magnetite particles in them.] (See page 383.) 8. Crystal of biotite cut at right angles to the basal plane, and showing Schillerization along the planes coinciding with those of the principal cleavage; from the scyelite of Loch Scye, Caithness. Seen as mag- nified 50 diameters. (See pages 383 and 405.) 9. Two thin flakes of the same biotite, lying parallel to the plane of easy cleavage of the mineral, magnified 100 diameters. The enclosures are seen to be more or less regular plates, very similar to those found in the hypersthene of Labrador. ‘wo grains of magnetite are also seen enclosed in the same crystal. (See pages 383 and 405.) Prater XII. Varieties of the Ultra-basie Rocks of Scotland. All the sections are repre- sented as seen with a magnifying-power of 30 diameters Fig. 1. Olivine rock (dunite) of the»Shiant Isles. Consisting of a mass of granules of clear olivine, only rarely showing faint signs of serpenti- nization. A few scattered particles of brown augite, of anorthite, and of magnetite (or chromite) are scattered among the olivine-grains which make up the bulk of the rock. The olivine is clear and almost entirely tree from enclosures of secondary origin. In the form of the olivine-grains this rock resembles the dunite of St. Stephan in Upper Styria; but in the perfect freshness of the olivine it finds its analogue in the typical dunite of the Dun Mountain, near Nelson, New Zealand. (See page 394.) 2. Porphyritic olivine rock (dunite) from the flanks of the mountain of Scuir na Gilean in the Isle of Rum. The rock consists of an aggre- gate of minute olivine-grains with a little augite, through which larger crystals of olivine are scattered. These larger crystals exhibit the dusty appearance produced by the development of numerous stellate and tabular enclosures in negative crystals, and lying in two inter- secting sets of planes within the crystal. The olivine is quite free from any trace of serpentinization. (See page 391.) 3. Olivine-augite-enstatite rock (lherzolite) from the top of Halival, in the Isle of Rum. ‘The structure of this rock is intermediate between the granitic and the ophitic. The olivine forms rounded grains con- taining a few large stellate enclosures, and is often enclosed in the augite or enstatite; the augite is bright green in colour, and is not improbably a chrome-diopside, and the enstatite,is a ferriferous one (proto-bronzite or proto-hypersthene), of a rich brown colour, with very marked pleochroism. Scattered through the rock are a few grains of chromite or picotite. Felspar is only present as a rare and accessory ingredient of the rock. The augite and the enstatite show slight traces of Schillerization. These two minerals cannot be distin- guished in the drawing. (See page 392.) 4, Ophitic picrite (augite-olivine-rock) from the Shiant Isles. The rock is made up of very large crystals of deep brown augite, which enclose numerous rounded grains of olivine, while these latter, in turn, enclose rounded grains of chromite or picotite. The minerals of this 416 PROF. J. W. JUDD ON THE TERTIARY AND rock are free from all traces of Schillerization. The crystals of sete aby so large that one fills up the whole field of view. (See page 394, Fig. 5. Anorthite-olivine-rock (troctolite) from the top of Halival, in the Isle - of Rum. ‘The rock, which constitutes a vein traversing olivine- gabbro, consists of a mass of interlacing anorthite-crystals, through which are scattered grains and aggregates of grains of olivine. The olivine is crowded with large stellate inclusions, and its outlines and cracks are rendered black and opaque. Except in the freshness of its minerals and in its finer grain, this rock exactly resembles the forellenstein of Volpersdorf and the Hartz. The scale on which the minerals are developed is, however, somewhat smaller. Sections of the Scotch rock would resemble that of Volpersdorf if the former 3059 magnified three times more linear than the latter. (See page 5. 6. Anorthite-augite-rock (eucrite) from Halival, in the Isleof Rum. This rock, which also forms veins in the olivine-gabbros, consists of a mass of interlacing anorthite-crystals, perfectly unaltered, through which are distributed granular particles of an augite of a green colour, which is more or less perfectly converted into diallage by Schilleri- zation. In some parts of the rock, a ferriferous enstatite is added to the two principal constituents, and this mineral sometimes prevails almost to the exclusion of the augite. This eucrite is of a decidedly granulitic structure, but other rocks of the same mineralogical con- stitution are coarse-grained and distinctly granitic in structure. (See page 395.) 7. Altered, ferriferous-enstatite-rock (bastite-rock) from Carrock Den, For- farshire. This rock occurs in the midst of a great dyke of serpentine which traverses the Old-Red-Sandstone strata; it is made up of an aggregate of ferriferous-enstatite-crystals in a somewhat altered condition, the whole being traversed by cracks filled with serpentinous material. Except for the amount of alteration the rock has under- gone, it exactly resembles the “bronzite-rock” of Kupferberg in | Bavaria, and of St. Stephan in Upper Styria. (See page 399.) 8. Mica-hornblende-picrite (scyelite) from an intrusive mass near Loch Scye, in Caithness. A number of grains of olivine, now converted into serpentine, are enclosed in crystals of pale green hornblende (seen in the lower left-hand part of the slide), paramorphic after augite, and of a highly magnesian biotite (seen in the upper right- hand part of the slide). The biotite is, in places, darkened by nume- rous inclusions arranged parallel to the basal plane, or in the direc- tion of the principal cleavage. (See pages 401-407.) Figs. 1-6 are from Tertiary rocks. Figs. 7 & 8 are from Palzozoic rocks. Discussion. Mr. Ruriry said that the points raised in the paper were so numerous that it became very difficult to discuss. The twin- structure in calc-spar was probably produced by pressure; but with regard to triclinic felspar the case seemed different; and he felt doubtful whether all twinning could be developed by pressure ; for, if so, the same structure would be produced in orthoclase. Besides, twinning usually occurred in two directions in the tri- clinic felspars—namely, parallel to the basal plane and to the brachypinakoid. If due simply to pressure, why should it not some- times occur parallel to the macropinakoid? The proposed term OLDER PERIDOTITES OF SCOTLAND. 417 Schillerization might prove useful, but he questioned whether some of the results attributed to it might not be due to weathering. Mr. Baverman felt the same difficulty that had been alluded to by the previous speaker in entering upon the discussion of this paper. He remarked that the twinning of triclinic felspars was not an essential peculiarity, as he had seen specimens in which it was absent; but he considered the origination of twinning from pressure unproyved, as there was no difference of cohesion in diffe- rent directions sufficient to produce twinning. Twinning is espe- cially well seen in albite crystallized freely in druses in mineral veins. Pseudostructures of lower symmetry in boracite &c. are due to change of structure produced in cooling, and quite distinct from twinning in felspars. Rey. E. Hiiz said that all banding that he had observed in igneous rocks, glass, &c. varied gradually from point to point when due to pressure, and thus differed from that described by the Author. Mr. Huptzston remarked that magnesian rocks were very mysterious. Their peculiarities are perhaps due to chemical com- position. Gabbros are always found associated with serpentine and olivine rocks. He inquired whether Schillerization might not be due partly to change of structure arising from something inherent. As a case of change resulting from original peculiarity of compo- sition, he quoted the analysis.of a rock lately described by Mr. Teall, which showed an amount of magnesia unusual for a non- olivine dolerite. There was no mineral in that rock to absorb so much magnesia except the augite, which must have possessed an exceptional composition, and consequently an inherent tendency to change: such inherent tendency might help to explain the phe- nomena of Schillerization. He further commented on the alterations stated to have taken place in depth; for some Schillerized rocks, e.g. bastite, are hydrated forms. Prof. Hueuss asked how far the relations of the rocks in question to one another and the conditions of depth &c. could be considered well established. In the example exhibited he thought the vein called gabbro was due to alteration along a joint, of which he saw traces on the back of the specimen in the divisional plane which ran almost through the middle of the vein. It looked like a vein along a faulted joint, and might be of any age later than the olivine rock and subsequent to the jointing and faulting, and there- fore not belonging to deep-seated conditions. The Presrpent congratulated the Author on haying, as he said, driven another nail into the coffin of the classification of igneous rocks by their geological age. He had always believed that the altered peridotites of the Apennines were of Tertiary age. In all cases that he had seen, the gabbro and peridotite were quite independent rocks; but he had seen picrite pass into diorite. He himself had always found gabbro the newer rock, evidently deep- seated ; for the crystallization was coarse even in small veins. He also doubted whether plagioclastic twinning was due to pressure ; for itis found in rocks not much pressed, such as lava-streams. 418 ON THE TERTIARY AND OLDER PERIDOTITES OF SCOTLAND. He thought the mystery about magnesian rocks was artificial. He suggested that the presence of diallage in deep-seated rocks might be due to hydration owing to depth, because the water could not escape. Amphibolization is well illustrated in the gabbro.of Corn- wall, when diallage is converted into hornblende at the surface. The AvurHor, in reply, said he did not mean to assert that mechanical strain produced twinning, but only develops it where the tendency already exists. It has been shown that this structure is induced by pressure in calcite, and, if so, the same change is possible in the plagioclase felspars. The case is similar with leucite and boracite, in which, however, the twinning disappears on the mineral returning to the original temperature of its formation. The - result of twinning in orthoclase is seen in microcline, and Lehmann refers microcline-structure in Saxony to pressure. Hypersthene was always, until lately, studied only in altered forms. Schillerized forms are produced by deep-seated hydration, weathered forms by hydra- tion near the surface. In reference to the alleged association of diallage and magnesian minerals, he stated that several varieties of augite pass into diallage. In answer to Prof. Hughes he said that the veins in the specimens referred to are irregular injection- veins. ON THE STRUCTURE OF THE AMBULACRA OF ECHINOIDEA. 419 31. On the Srructure of the AMBULACRA of some Fosstz GENERA and Species of Rrevrar Ecuinoipea. By Prof. P. Marrin Duncan, M.B. Lond., F.R.S., F.G.8. (Read April 29, 1885.) CoNTENTS. I. Introductory Remarks.— II. General Remarks on the Structure of Ambu- lacra.—III. Descriptions of the Ambulacral Plates of some Genera and Species, and the necessity for the Introduction of Diplopodia, McCoy, and a new Genus, Plesiodiadema.—lV. Conclusions relating to the types of Ambulacra.—V. De- scription of the Figures. I. Inrropuctrory REMARKS. Tux characters of the ambulacra of the Echinoidea have always been considered of primary importance in the classification of that great division of the Echinodermata. The details of the structures of the ambulacra of the regular Echinoidea have been long known in the instance of the Cidaride, in some of the Salenidz and Echinometride, and in many genera of Kchinide. ; The study of the structures ied to the separation of the groups of genera with simple plates and one pair of pores to a plate from those having compound plates with three or more pairs of pores. Cidaris has been acknowledged as the type of the first group, and, thanks to the elaborate investigations of Lovén *, Strongylocentrotus may be considered the type of the other series. In a monograph on the fossil Kchinoidea of Sind, by the author and Mr. W. Percy Sladen, F.G.S., there is a description of two species of Celoplewrus from the Oligocene, and the illus- trations which accompany the work fully explain that there is a type of ambulacral plate which departs from the received idea regarding the intimate structure of plates with triple pairs of pores f. Subsequently some researches by the same authors proved that the Arbaciade and the recent Diadematide had their ambulacra con- structed on a plan hitherto unobserved, and which separated the groups distinctly £. Having obtained a knowledge of the characters of the recent forms, the study of the corresponding details of the fossil species became tolerably easy. The results of this study are now offered to the Society. I have to thank the executors of the late Dr. T. Wright, F.R.S., for permitting me to examine and draw what was necessary from the beautiful specimens in their charge. I am also very glad to have the opportunity of thanking the authorities at the British Museum and at the Museum in Jermyn Street for allowing me to study the collections. In the majority of fossil regular Echinoidea the pairs of pores of * Lovén, Etudes sur les Echinoidées, 187 4, p. 19. t ‘Palzontologia Indica,’ ser. xiv. fasc. iv. pl. xxxix. (1884). + Journ. Linn. Soc., Zool. vol. xix. pp, 25 and 95 (1885). 420 PROF. P. M. DUNCAN ON THE STRUCTURE OF the ambulacra can be readily observed ; but the separations of, or the sutures which unite, the edges of the plates are usually not to be seen. Many weathered specimens of Oolitic and Cretaceous species show all the details of the ambulacra; and when they are im- © perfect or slightly confused, the knowledge of the position of the plates in the modern allies of the fossil forms renders the action of reagents almost invariably successful in distinguishing them. But it is not possible to make out the limits of the ambulacral plates in some specimens, and usually these forms are the most perfect in their state of preservation. Weathering and the action of Lovén’s reagent, alcohol mixed with glycerine, assist the investigation of the fossils, and most liquids which permeate the plates and evaporate rapidly will assist in the investigation of recent Echinoidea. II. General REMARKS ON THE STRUCTURE oF AMBULACRA. An ambulacrum extends from the actinal edge of a radial (ocular) plate to the edge of the peristome; it is composed of a number of plates which are placed in two rows or zones on either side of a vertical or median line, and each row consists of plates located in succession from the radial plate to the peristome. The plates of one row are united by suture with those of the other, and the junction occurs along the median line, the extremities of the plates being more or less angular. The plates of one zone are not on an exact level with those of the other, for the angle of one plate fits into the reentering angle which exists between two of the opposed plates. The edge of each plate in contact with the inter- radium is also more or less geometrical, but 1t may be rounded off in shape, instead of angular. The plates in each row are united actinally and abactinally with other plates. These unions are by suture. Each plate has a poriferous zone, and the rest forms part of an interporiferous area; and there is a pair of pores toa plate. In well- preserved specimens the pair of pores is encircled by a raised dish- like structure called a peripodium, and the pores are never placed quite transversely or horizontally, but more or less obliquely, so that the pore nearest the median line of the ambulacrum is on a lower level than the other; that is to say, the inner pore is adoral to the other and is called the adoral pore. ‘This pore is in contact, in the young Echinoid, with the line of division between two con- secutive plates, and notches the edge of the peripodium ; but it may become distant from the suture during growth. In the Cidaridx all the plates are primaries, and each has its pair of pores. A primary plate is one which reaches from the poriferous zone to the median line or vertical suture, and which comes in contact there with others of the opposite zone. In the Cidaridz the plates in- crease in number by developing just at the actinal edge of the radial plate, and one plate is formed after another. At the peristomial end of the ambulacrum there is a corresponding THE AMBULACRA OF FOSSIL ECHINOIDEA. LAT separation of successive plates, so as to produce the characteristic plating around the mouth seen in recent forms of Cidaris. In the other families of the regular Echinoidea the addition of new plates also occurs at the edge of the radial plate; but there is a crowding of the plates more or less at the peristome, and the oldest plates there gradually become absorbed at the very edge. So that with the growth of the whole test in height there is a superabundant growth of the ambulacral plates, and, as Lovén has well shown, there is a downward or actinal movement of the ambulacral plates from the radial plate to the peristome. This movement is compli- cated by the fact that the ambulacral plates are all growing with the rest of the test, and enlarging in all directions at the surface. Moreover the growth-rate of some plates is greater than that of others, and those which carry tubercles appear to have a greater growth superficially than others. Consequently irregular pressure is exerted by these plates on their neighbours, and the result is very remarkable. Again, the movement of the plates above the ambitus of the test, although comparatively free, is of necessity diminished near the peristome, in consequence of the more or less rigid state of the peristomial region incident to the position of the auricles of the jaws and their processes. It is to these different facilities for and oppositions to a regular and symmetrical growth that the varied shapes and characters of the ambulacra and their plates are due. It is an interesting and highly suggestive truth that all the regular Echinoidea should have their most radially situated plates in the form of the simple primaries of the Cidaride ; but at different distances from the radial plate modifications begin to be seen, and they are characteristic and of generic and specific value. The modifications which were known and which had been care- fully described by Lovén before the publication of the “ Fossil Echi- noidea of Sind,” in the ‘ Palzeontologia Indica,’ ser. xiv., were those which characterize the Echinidz and some other forms, such as Stron- gylocentrotus (fig. 1). In these the growth-pressure develops com- Bis, b>, pound plates by jamming and uniting the original primaries; moreover - the part of the primary remote from the poriferous portion is often - prevented from growing, or is absorbed by the growth-pressure. The result is the formation of demi-plates which do not reach the median line. Moreover the downward growth and the other varieties of growth-expansion cause combinations of several plates, and produce compound geometrical forms made up of three, four, five, and even * For the explanation of this and the following figures, see pp. 451, 452. Q. J.G.8. No. 163. 26 4992 PROF, P. M. DUNCAN ON THE STRUCTURE OF more plates, all more or less departing from their original shape. Growth near the unyielding peristome produces shifting of the pori- ferous parts of plates, and hence the apparent confusion of the pairs of pores in that region in so many genera. It must be understood that the confusion is only apparent, for Lovén has explained it, and no additional pairs of pores intercalated there during growth. The physiological importance of the ambulacra to the Echinoid cannot be over-estimated ; for the peripodia support the prehensile or motor tentacles, and in the Arbaciade and the Diadematide the tentacles which are above the ambitus have a non-prehensile and branchial function. The number of tentacles placed within a given ~ area is therefore of classificatory as well as of physiological im- - portance, and this number bears a definite relation to the number, kind, and shape of the plates which constitute the ambulacra. The Echinoidea with the simplest ambulacra are found in the lower Secondary deposits, and it is advisable in the present inquiry to commence with the description of some of the earlier forms of the Diadematide. It is proposed to consider the genera Hemipedina, Wright, Psewdodiadema, Desor, Pedina, Agass., Stomechinus, Desor, Hemicidaris, Agass., Diplopodia, McCoy, and Cyphosoma, Agass. Ill. Descriptions oF THE AMBULACRAL PLATES oF THE GENERA HemIpepina, PsevpopiApDEMa, PEprna, StomEcHiNus, HEMIcIDARIS, Dretopopia, AND CypHosoma. Tur NuEcEssITY FoR 4 NEW GENUS, PLESIODIADEMA. Genus Hemrpepina, Wright, 1855. The diagnosis of this genus will be found in the ‘Monograph of the British Fossil Echinodermata,’ Pal. Soc. Lond. 1855, p. 143. Dr. Wright made the following remarks concerning the affinities of this genus with other genera :—‘‘ Hemipedina is related to Pseudo- diadema in having the pores unigeminal and the tubercles per- forated ; but it is distinguished from Pseudodiadema by the absence of crenulations from the summit of the bosses. It is related to Pedina in possessing perforate and uncrenulate tubercles ; but it is distinguished from that genus in having the pores unigeminal, Pedina having the pores trigeminal asin Hchinus. The elements of the disk are likewise more largely developed. Hemipedina is related to Echinopsis, but is distinguished by the narrowness of the ambulacral areas, the general depressed form of the test, the shape of the mouth- opening, and the deep decagonal lobes of the peristome (that of Echinopsis being almost deprived of incisions), together with the ‘ greater size and development of the elements of the apical disk.” In the drawings of a species of Hemipedina, Dr. Wright noticed the long slender needle-shaped spines with fine longitudinal stria- tions. He states, moreover, that the optic pore is in the centre of the radial plate. Hemipedina Jardinii, Wright, has a considerable series of low and ; a THE AMBULACRA OF FOSSIL ECHINOIDEA. 423 broad primaries near the radial plate, and extending far towards the ambitus, and each plate is united by a separable suture to the plates situated apically and actinally. At the ambitus three primaries are seen to form a compound plate geometrical in figure, and their separability is at an end. There are triple plates of this character down to the peristome. Taking a compound plate at the ambitus (fig. 2) as the example, it appears that it is Fig. 2 (see p. 451). broader than high, and that the pairs of pores, three in number, are either straight or in a very slight curve. Two lines of suture cross the compound plate, and they indicate the edges of the primaries which have united to form it. One line is between the aborally situate plate and the middle one of the combination, and it passes from the adoral pore of the aboral pair inwards to cross the base of the tubercle apically to the mamelon, and thence it passes on to the median suture of the compound plate or, as it is called, the vertical suture or edge. This line is very faintly curved with the convexity towards the tubercle, or it may be straight and cross the flank of the boss. The other sutural line is between the middle plate and the adoral plate, and it is in contact with the adoral pore of the second or middle pair; thence it crosses the adoral flank of the boss actinally to the mamelon and reaches the vertical suture with or without a curve. The aboral plate of the combination is a low and broad primary which includes a small portion of the boss, and the adoral plate is of the same configuration as the other. The middle plate is rather the largest, and is a well-formed primary which carries much of the boss of the tubercle and all the mamelon. The sutural lines between the, plates constituting the compound plates are in some instances decidedly curved, with the convexity placed towards the mamelon; but this condition is replaced nearer the peristome by quite straight lines. The formation of the almost rectangular primaries in the combination resembles a simple appo- sition of Cidaris-like plates, and it is interesting to notice this primitive type merging gradually into the fully developed one, in which, as in the ancient and modern Diadematoids, the curving of the sutural lines is coincident with an enlargement of the middle plate towards the median line at the expense of the plates above and below, these plates then departing from the shape of those of the Cidaride. HemipepiIna BowrrBanrri, Wright. There are some fine examples of this species in the Museum of the . 262 494 PROF. P. M. DUNCAN ON THE STRUCTURE OF Geological Survey, Jermyn Street, and in most the number of single primary plates near the apicai end is very striking, indeed almost leading to the idea that all the parts of the ambulacrum are made up of them. But there are one or two compound plates preserved. In one of these, near the peristome, the triple nature is evident, and the line of suture between the middle and adoral plates is curved, and passes from the adoral pore of the middle pair towards the mamelon of the tubercle and thence to the median or vertical suture, the con- vexity of the curve being directed apically. In another specimen the line of suture between the middle and the aboral plate is seen, and it is curved, with the convexity towards the mamelon. Hence these compound plates are on the Diadematoid type, and it may be presumed ’ from the phenomena presented by the recent species of Diadema that growth-pressure has changed the shape of the original primaries. In one of the specimens in the Museum there are four plates and four pairs of pores in one of the compound plates, and it appears, but not very satisfactorily, that the additional plate is a low primary. This is not without its significance; for a similar structure is seen in allied genera*. Hemipedina marchamensis, Wright, from the Coral Rag, is a fine form belonging to a section of the genus which has numerons primary tubercles in rows on the interradia. There is a specimen in the British Museum (no. 75923) which shows the shape of the triplet of plates which combine to form a geometrical plate near the ambitus. The compound plate is broader than high, and there is a space between the tubercle and the median or vertical suture (fig. 3). The direction of the sutures between the Fig, 3 (see p. 451). three plates indicates their shape, especially as the whole compound plate is contained between an aboral and an adoral transverse suture. she The pores are rather oblique, and the adoral pore of the first pair is on the suture which unites the first and middle plates. The line of this suture is, from the interradium to the adoral pore, and thence with a curve, convex adorally, up the flank and over the top of the boss of the tubercle apically to the groove at the base of the mamelon, and then down the slope to the edge of the boss to reach the median suture at a short distance from the aboral and inner angle of the compound plate. This first plate is therefore a low primary resembling the corre- * With regard to Hemipedina Bowerbenkii, Wright (op. cit. p. 145), illus- trated on plate ix. of the Monograph already noticed, it must be observed that the figure 2 6 cannot be correct. It represents the pores as if they were turned upside down, and the adoral pore, or that which is furthest from the inter- radium, as aboral to the other in position. THE AMBULACRA OF FOSSIL ECHINOIDEA. 425 sponding plate of amodern Diadema. The middle plate is lowest at the centre of the tubercular area, for it is nipped in by the curved edge of the first plate and also by an aboral curvature of the third plate. But further towards the median line the middle plate, after carrying the mamelon, expands, and is in relation with much of the boss and the greater part of the compound plate. The third plate has its aboral edge curved apically, and it is a low primary, for the suture between it and the middle plate reaches the median suture just abactinally to the adoral and inner angle of the compound plate. The resemblance of these plates to those of the typical and recent Diademata is exact. Perhaps the most striking species of Hemipedina is H. tuberculosa, Wright (op. ct. p. 164), on account of its resemblance to a Hemz- cidaris without crenulation, and with an unusual number of small secondary tubercles in the interradia. It is a beautiful form, and is even more Cidaris-looking than Hemicidaris. The ambulacral plates, however, do not always remain as simple primaries; for towards the ambitus, where the tubercles increase in size rather suddenly, there are three pairs of pores evidently in relation to as many plates which have combined to produce a geometrically shaped compound plate (fig. 4). The triple pairs may arch very slightly: Fig. 4 (see p. 451). around or be straight at the edge of a great tubercle, which nearly covers the entire plate. The peripodia, which are only slightly oblique and broadly elliptical in shape, are not so crowded as they are in Henucidaris; but they impinge upon the outer flank of the tubercle, and in some specimens their relation to the plates which their pores perforate can be appreciated. Taking the first tubercle above the ambitus, it will be noticed to be situated apically to a decidedly large one, and to be separated from it by more space than exists between the other tubercles placed in succession towards the peristome. The three peripodia are in a slight arc, and the most adoral is slightly nearer the tubercle than the others. The tubercle is a broad, low cone, with a well-developed mamelon surrounded by a decided groove. Careful observation proves that the adoral pair of pores has the adoral pore on a line with a transverse suture which separates the combination to which this poriferous plate belongs from the next plate in actinal suc- cession. And on the adoral flank of the tubercle, and nearer the base than the groove around the mamelon, is a line which can be traced from the adoral pore of the peripodium which is the middle one of the triplet, over the slope of the boss to the median line of the ambulacrum. 496 PROF. P. M. DUNCAN ON THE STRUCTURE OF The line is that of the suture between the lower and middle plates of the compound plate, and it limits the lower plate aborally and the middle plate adorally. As this suture reaches ‘the median line, and as the transverse suture below also does this, the lower or adoral plate of the triplet is a more or less rectangular primary. On looking at the apical and inner part of the tubercle a line may be seen passing along the side of the base of the tubercle and going obliquely upwards, or aborally, to the vertical or median suture. This line is to be traced over the boss aborally to the mamelon to the adoral pore of the first pair of the triplet. It is the suture which separates the aboral (or first) and the middle plates of the triplet; and as it reaches the median line, the plate above it, or the first of the series, is a primary, highest at the poriferous zone and low at the median line. This first plate is bounded aborally by the transverse suture which adorally limits the plate placed immediately abactinally, and which does not form part of the compound tubercle-bearing plate under consideration. The shape of the middle plate of the combination is determined by the direction of the suture of the edge (adoral) of the first plate and of that (aboral) of the third plate. The plate expands in the direction of the median line aborally, and, moreover, is covered by the mamelon and by much of the boss. The structure of the tubercle-bearing compound plate immediately adoral to the last is very simple. The tubercle nearly covers the whole plate, except the narrow poriferous zone, and the peripodia are rather oblique and in an arc, so that the third is nearer the median line than the first of the triplet. The course of the sutures from the adoral pores of the peripodia is the same as in the simpler forms of Pseudodiadema and of the modern Diademata. All the plates of the compound one are primaries, and the middle one is the largest: it is covered by the mamelon and by most of the tubercle near the median line, as well as by that portion of the boss which lies on a transverse line with the second peripodium. The suture at the adoral edge of the first plate crosses the boss to the vertical suture with a slight convexity directed actinally, and the suture at the aboral edge of the third plate crosses the boss in the same manner, but the convexity is directed apically. Hence the middle plate is expanded towards the median line, low at the part where the mamelon is, as it were, nipped in between the first and second plates, and not so low at the poriferous part. The first plate is lowest in vertical measurement at the vertical suture, and so is the third plate. The transverse suture which bounds the compound plate adorally is in contact with the adoral pore of the third pair. There are no demi-plates in this species, and the compound plates are different in construction from those of Hemicidarvs. Genus PsEeupoprapEmMA, Desor. Desor (‘ Synopsis,’ p. 63) gives a short diagnosis of this genus, and classifies it in his group of Oligopores, that is to say in a division of THE AMBULACRA OF FOSSIL ECHINOIDFA, 427 the regular Echinoidea, the forms of which have three pairs of pores only to each ambulacral plate. Test of moderate or small size. The tubercles are of the same size in both areas, and are crenulate and perforate. The tubercles either only form two-rows in the interradia, and may be without secondaries, or they may be arranged in four or even six rows. Poriferous zones simple. Spines smooth or faintly striated. Range from the Lias to the Cretaceous inclusive. Desor notices that the forms thus diagnosed were termed, in the ‘Catalogue Raisonné,’ “ Diadema,” and were placed alongside of the recent species which bear that generic appellation. But besides being smaller than the modern forms, there is the character of the latter which relates to the spines to be considered, according to Desor. He reminds us that the spines in the modern species of the genus Diadema are verticillate in their striated ornamentation. Under the belief that this distinction was of great classificatory im- portance, he separated the species which are found fossil, as belonging to the genus Pseudodiadema, and took two species as typical of two divisions of the genus—Pseudodiadema hemisphericum (Cidarites pseudodiadema of Lamarck, or Diadema pseudodiadema, Agass. & Desor) and Pseudodiadema mamillanum, Romer. ‘The first he con- sidered represented the group with several rows of secondary tubercles in the interradia; and with the latter he associated all the forms with only two rows of tubercles in an area. It will be noticed that in the diagnosis Desor did not find a place for certain species which have been admitted since, and which have a doubling of the pairs of pores in the region above the ambitus. McCoy had separated the species with doubling of the pairs near the apex from Deadema, and had founded the genus Diplopodia for them. Wright, however (op. ct. p. 109), adds to the generic cha- racters of Pseudodiadema, ‘“ the pores in one section are unigeminal throughout, and in another section they are bigeminal in the upper part of the zones.” The same author states that Pseudodiadema differs from Diadema in having solid spines, with a smooth surface, the sculpture, in most cases, consisting of microscopic longitudinal lines. He also remarks that the genus differs from Cyphosoma in having the tubercles always perforated. The necessity for allying Cyphosoma and thus adding te the confusion is a consequence of admitting forms with doubling of the pores into the genus Pseudodiadema. Wright noticed the genus Diplopodia, and remarks as follows in placing it on one side :—‘‘Cwteris paribus, the crowding together of a greater number of pores in a zone is, at most, a sectional, and can never form a stable generic character, inasmuch as it is subject to great varia- tion in the diplopodous species themselves, and is, moreover, often only an adult development.” Having studied the morphology of the ambulacra of the recent Diadematide (Journ. Linnean Soc., Zool. vol. xix. p. 95) I was greatly impressed with the results of a careful examination of many forms of the allied genus Pseudodiadema. I came to the conclusion 498 PROF. P. M. DUNCAN ON THE STRUCTURE OF that the whole subject of the classification ought to be reinvestigated, the morphology of the ambulacra being considered of primary im- portance. It became easy, after the examination of weathered speci- mens, to decide that whilst some recognized species of Pseudodiadema were evidently Oligopores and closely allied to the modern Diadema, others were Polypores, having sometimes as many as five or six pairs of pores to an ambulacral plate. Again, some species are allied to the recent forms by having the optic pores at the actinal margin of the radial plate, and by having decided branchial cuts and even tags arising from the cuts. Moreover the structure of Cyphosoma being known to me, I could hardly consent to so close an alliance as Dr. Wright suggested between it and Pseudodiadema. . Pseudodiadema hemasphericum is well drawn by Bone in Dr. Wright’s Monograph of the Brit. Foss. Echinodermata, pt. 1, 1855, plate viil. The shape of the radial plates and the position of the optic pore at the very margin of the plate are clearly indicated, and the drawing of an ambulacrum (fig. 1 d) shows the relation of three pairs of-pores to each tubercle-bearing plate. The exact relation of the pairs is not shown ; for the specimen was so perfect that no sutures probably were visible. But in the British Museum there is a specimen (No. 23329) from Malton, named, as of old, Diadema pseudodiadema, and the lines of the sutures may be seen here and there. In the great majority of the ambulacral plates there are three pairs of pores. ach pair is in a primary plate, and the three pri- maries have become fused, as it were, into a geometrical compound plate (fig. 5). ! Fig. 5 (see p. 451). The first or aboral pair of pores of this compound plate has its adoral pore in contact with the adoral suture of the low broad primary plate which forms the first or apical portion of the com- pound plate; and this suture is directed to the median or vertical suture in a course which is somewhat curved, the convexity being adoral. The suture crosses the boss of the tubercle just abactinally to the mamelon. The pair of pores which belongs to the middle plate of the combination has its adoral pore in contact with a suture that unites its adoral edge with the aboral edge of the third plate. The direction of this suture is towards the median suture, and it has a path from the interradial end of the poriferous zone to the adoral pore just noticed, and thence with a curve directed apically, THE AMBULACRA OF FOSSIL ECHINOIDEA. 429 reaching the boss adorally to the mamelon. The course is then to the median suture, and the termination is close above the adoral and inner angle of the compound plate. The middle plate is low at the poriferous zone, nipped in vertically at the boss, where it includes the mamelon, and expanded towards the median line. The adoral plate of this combination has an arched aboral edge and is a low and broad primary, smaller in vertical measurement at the median line than at the poriferous part. The pairs of pores are in peripodia, and the amount of arching is slight. This description would suffice for a compound plate near the ambitus of a recent Diadema. But the fossil form has some compound tubercle-bearing plates at or just below the ambitus, which are polyporous ; for there are distinctly four pairs to a compound plate, and not three only (fig. 6). Fig. 6 (see p. 452). There are therefore four plates in the combination, and all are not primaries, there being a small demi-plate (6) amongst them which does not reach the median line. The aboral or first plate (a) of the set resembles the corresponding plates of the combination already described, and is a low and broad primary with the adoral edge bent actinally. The second plate (6) is a demi, and it reaches a little way up the tubercle, andis bounded aborally by the edge of the first plate, and adorally by part ofthe suture of the third plate in its path to reach the median line. Part of the third plate (a’) has the shape of the middle plates of the combinations in which there are only three pairs of pores, but it is rather lower, and the fourth plate (a'') resembles the adoral plates of the triple compound plates. The second plate is the relic of a primary which has undergone absorp- tion owing to that growth-pressure which is so easily traced in some recent forms of Diadematide. The recent species of Diadema do not, however, present this phenomenon, and there are no demi- plates in them. _ The simplest form of fossil Diadematid is a species which, had it doubling of the pairs of pores close to the peristome, would fall within the specific diagnosis of Pseudodiadema depressum, Agass. The specimen in my possession was obtained by Prof. J. Morris, M.A., from the Cornbrash of the Chippenham district. It has nearly straight rows of pairs of pores, the outer pores being larger than the inner. There is but slight obliquity of the pores, and the pairs are not close. There are three pairs to each tubercle-bearing compound plate, and the three plates are primaries of the true Dia- dema type (fig. 7). The commencement of the compound plates is very close to the radial plate, and there are only one or two solitary 430 PROF. P. M. DUNCAN ON THE STRUCTURE OF uncoalesced primaries, Near the peristome the simplicity of the compound plate persists, and there is no crowding of the pores. An Fig. 7 (see p. 452). interesting structure exists in the form of a tag, which, as in the recent Diademata, passes up from the branchial cut by the side of the ambulacra. So far as the test is concerned, or rather that part which remains, the apical system being deficient, there is no distinction to be made between this species and a recent Diadema. There are many species included in the genus Pseudodiadema by authors which have the simple triplet arrangement of pores just noticed, and the peristomial crowding never amounts to a dis- placement of pairs or the production of demi-plates. I have been able to examine many of the forms described by Dr. Wright, thanks to the courtesy of his executors. The type of this group existed from the Inferior Oolite, if not from the Lias, to the Cretaceous age inclusive; and it is a matter of great interest to have been told that hollow, striated, and verticillate spines were found in the Chalk and drawn by Mr. Bone. The Pseudodiademata with simple triplets form, therefore, one distinct type or group. The Pseudodia- demata, having also occasionally an additional pair of pores belonging to a demi-plate, belong to a closely allied section or subgenus or group. The next type to be considered, the third group, is one in which there are never less than four plates and four pairs of pores to a compound plate, and of which Pseudodiadema mamillanum already alluded to, is an example. In most of the specimens of this series there is barely any trace of the divisional sutures to be seen in those plates which have the greatest number of pores; but an instance of a form clearly pre- senting all the necessary structures to view from which a drawing can.be made is in Dr. Wright’s collection*. Having examined the specimen, it is evident that a compound plate at the ambitus has no less than five primary plates entering into its composition, and that the next above or aboral compound plate has four (fig. 8). The pairs of pores are in slight arcs, the peripodia are well developed and often occupy nearly or quite the whole height of the poriferous area of the plate on which they are placed. The adoral pore of a pair is always in relation with the suture between its plate and that * Pseudodiadema Michelini, Agass. THE AMBULACRA OF FOSSIL ECHINOIDEA. 431 which is placed immediately actinally. The tubercle of the com- pound plate is large, and there is some space between it and the median suture. Fig. 8 (see p. 452). PW Se PR wD oO Taking the compound plate above the ambitus, first of all, for descriptive purposes, there are to be noted four plates and four pairs of pores in peripodia. The actinal or fourth plate (no. 4) is a low and broad primary having a convexity directed aborally, so that the plate is low in the poriferous zone and at the median line of the ambulacrum, and much higher midway where it reaches across the adoral part of the base of the boss. The next plate situated abactinally (no. 3) is the largest of all in the compound plate, and assimilates in shape to the middle plate in the triplet of a Diadema ; it is iargest near the median suture of the ambu- lacrum, is nipped in on the tubercle, and is somewhat higher at the poriferous zone. ‘The adoral pore of its pair is in relation with the suture between its adoral edge and the aboral edge of the plate just described. The abactinal edge of the plate now under descrip- tion crosses the boss and the centre of the mamelon, and then passes towards the median line, with an abactinal and inward path, so as to give a curved appearance to the suture which joins this plate to the one immediately above. ‘The third plate from the adoral edge, or no. 2 of the compound one, is a long or rather broad, low primary, the actinal edge of which corresponds with the abactinal ~ curved edge of the plate just described. So this third plate has a bent actinal edge, and this is indicated by the suture. The abactinal edge of the plate is also curved, and with the convexity directed actinally, and the height of the plate at the median line of the ambulacrum is small and less than at the poriferous zone. The most apically placed of the plates, or the first (no. 1), is a low ‘and broad primary, lowest at the vertical suture, and with the adoral edge curved adorally, the abactinal edge being straight and trans- verse. The adoral edge of this plate crosses the tubercle not very far from the mamelon. The transverse aboral edge is in contact with the actinal plate of the compound plate situated immediately abactinally. All four plates combine to form a solid compound plate, and they - are to be recognized by the direction of their sutures. The angle A432 PROF. P. M. DUNCAN ON THE STRUCTURE OF of the compound plate at the median line is formed by the large primary (no. 3). It will be observed that this arrangement of the component plates is not like that of the species already noticed, in which an occasional fourth plate has been sometimes produced; for in the present instance there is no demi-plate to be seen, and all the plates are primaries. The compound plate at the ambitus (fig. 8) has a larger tubercle than the one immediately above, and is larger altogether. It has five plates entering into its composition, and there are therefore five pairs of pores and five peripodia; these are in an arc, and the third pair from the abactinal edge of the compound plate is the most remote from the median line of the ambulacrum. The first, second, and third plates from the abactinal edge are formed after the model of the abactinal plates 1 and 2 of the compound plate above, and they are low and broad primaries with a curved adoral edge. The fourth plate is the largest, and corresponds in shape to the third plate from the abactinal edge of the compound plate above; it is on the type of the middle plate of a Diadema, and is expanded towards the median line, and is lower on the tubercle, the actinal half of which, and sometimes more, it carries. The last and actinal plate of the combination (no. 5) is a primary, low at the median suture, slightly higher at the poriferous zone, and with an arched aboral edge which curves towards the mamelon and just reaches the tubercle. The adoral edge of the plate is trans- verse and straight, and it is the actinal boundary of the compound plate. Thus the three actinal plates of this compound plate resemble in shape and in position the three adoral plates of the compound plate above, and it appears that the additional plate of the ambital com- pound is either the fourth or fifth from the actinal edge. Great as the downward growth-pressure must have been, there are no demi- plates. I have not had access to some of the most important poly- porous species figured in Dr. Wright’s monograph, but which do not belong to his collection, and I can therefore only assert that in -all the forms of the group which have been examined by me there is an absence of the demi-plate. Considering the first two groups of forms hitherto named Pseudo- diadema, it is evident that the ambulacral structures unite them, and at the same time separate them from the polyporous group. It is interesting to note that these simple forms are the oldest ; they differ from the recent species of Diadema in shape and size at maturity, and in the comparative height of their plates. More- over the occasional demi-plate in the tubercle-bearing plate con- stitutes a distinction; for this is not seen in the modern forms. The details of the peripodia of the ancient and modern forms are not quite the same. With regard to the spines there is much difficulty in making very definite distinctions, and there are many loose spines found in the Secondary series of rocks which are comparable with those of Diadema. : THE AMBULACRA OF FOSSIL ECHTNOIDEA. 433 It appears consistent with the results of these researches to decide that the genus Pseudodiadema should be restricted to the forms with triple plates, with an occasional extra plate in the nature of a demi- plate; that is, to groups one and two. Of such a genus the spe- cies placed in the following list may be taken as common forms :— Pseudodiadema Moorei, Wright; P. depressum, Ag.; P. radiatum, Wright ; P. Bakerie, Woodw.; P. priscum, Cott. ; P. inequale, Des. ; P. Wrightir, Cott.; P. prisciniacense, Cott.; P. rotulare, Ag.; P. Benettie, Forbes ; P. ornatum, Goldf.; and the species which has been partly described in this communication. Pseudodiadema Brongmarti, Ag., and P. Bailyi, Wright, may be taken as good examples of the subgroup with an occasional demi-plate; and of course P. hemisphericum is the type. On the other hand, the species with at least four and with five pairs of pores or more, both in forms not full-grown and adult, should be ranged in another genus—Plesiodiadema. Under this genus will be arranged the species P. mamillanum, Romer; P. Micherm, Ag.; P. Blancheti, Des.; P. Vernewilii, Cott.; P. tenuis, Des.; P. annulare, Desor, &c. Fig. 9 (see p. 452). Genus Prpina, Agass. The diagnosis of Pedina (an Oolitic genus) has been partly ~ noticed (page 422), and it is now necessary to determine what dis- tinction the obliquity of the triple pairs of pores makes in the shape of the plates. Taking Pedina Smithii, Wright, as the type, an examination of the specimen in the late Dr. Wright’s collection indicates that the ambulacra are different from those of Hemipedina. The arrangement of the triplets of pores is to a certain extent like that in typical recent Triplechinide, and the first or aboral pair (fig. 9, ¢) of each series of three in one line is, as in the recent forms, the adoral or actinal pair of a triple compound plate, and is situated much nearer the median line of the ambulacrum than the pair immediately above (fig. 9,6). The pairs are in oblique series of three, 434 PROF. P. M. DUNCAN ON THE STRUCTURE OF slanting adorally and towards the interradia. But when a series of pairs is considered in relation to a compound plate it appears that there is really great arching, for the second and third pairs of pores in the linear series are the first and second pairs of the compound plate, whilst the third pair of the plate, or the adoral, belongs to the linear series immediately actinally, or they are much nearer the ambulacral median line. The pair of pores which is in the abactinal part of a compound plate is the second pair of a triplet, and of course the third pair belongs to the middle plate of the combination. The second pair of the triplet of pores is- nearer the interradium than the first pair, which belongs to the compound plate above ; but the third pair, which is in the middle plate of the compound one, is nearest the interradium. The peripodia of the pairs are rather close. The compound plates are low and much crowded, and there are no less than four of them in contact with an interradial plate slightly above the ambitus, where the diagrammatic sketch was taken. ‘Thus as each compound plate consists of three plates combined, there are twelve in relation to an interradial plate. In the specimen in Dr. Wright’s collection the sutures of one of the ambulacra can be distinguished in a vertical series of four plates (fig. 9), the most apical of which and the most actinal bear tubercles, the two others being simply granular. The shape of the plates con- stituting the compound plates and the direction of the sutures differs in some of the compound plates ; nevertheless there is no difficulty in seeing that the variation has been due to pressure from growth influencing plates which, under other circumstances, might have remained typical of Diadema. The arrangement of the component plates is not at all like that seen in Hchinus, and the genus Pedina does not enter the family of the Echini proper. Compound plate I1—The edges of the plate which are in the -lines of the sutures between the plate and those immediately apical and adoral are, as is usual, transverse, and reach the median line at the reentering angle of the median zigzag. The aboral plate (a’) of the compound is a demi-plate which does not reach far beyond the poriferous half of the combination; and the adoral pore is on the adoral suture, which is curved with the convexity directed actinally. The middle plate, a primary, carries the bulk of the tubercle and gradually increases in vertical measurement from the poriferous area to the vertical suture at the median line. It is bounded aborally by the demi-plate (a) and by part of the transverse suture, and it is bounded actinally by the edge and suture of the third plate, a primary (c). This suture is curved, with the convexity aboral ; it just touches the adoral part of the tubercle, and reaches the median line at a slight distance from the actinal and inner angle of the compound plate. The direction of the suture is that seen so commonly in the third plate of a triplet in Hemipedima and Diadema. THE AMBULACRA OF FOSSIL ECHINOIDEA. 435 Thus the plate a’ is a demi, plate 6 is a large primary, and plate c is a low and broad primary with an arched aboral edge. Compound plate II.—This is composed of three primaries, of which the middle is the largest and occupies most of the plate near the median line. The plate is trily Diadematid in its shape and in the details of the sutures. Plate a is a low broad primary with its adoral edge curved actinally. Plate ¢ is also a low and broad primary and the aboral edge is curved with the convexity placed towards the apex. Plate 6 is low at the poriferous area, nipped in and lower further towards the centre of the plate, and expanding considerably towards the median line. Compound plate III.—This resembles the last; but the direction of the suture uniting the middle plate with the adoral plate is less curved and approaches a straight line. Compound plate IV.—This is Arbacioid in shape and there is an aboral demi-plate (a’), a large middle primary plate (6), and an adoral demi-plate (c’). The middle plate, much the largest, carries the tubercle, and the whole of the vertical suture is in relation toit. The poriferous part of this hatchet-shaped plate (6) is low. Plate a’ has its actinal edge much curved adorally, and the suture nearly reaches the median line, but the plate is a demi-plate. Plate c’, also a demi-plate, has its aboral suture curved with the convexity aboral, and it terminates short of the median line and at about the same vertical position as the suture of plate a’. It is evident that Pedina is a well-defined genus, and that the situation of the sutures which are in the ambulacra is different from that seen in the family Echinide, and in the main resembles that of Diadema and Pseudodiadema. The presence of the demi-plates fashioned after the Arbacioid type ally the form with Hemicidaris. Genus Stomecuinvs, Desor. The examination of the ambulacra of the typical species of this Oolitic genus shows that the plates are not arranged after the method which characterizes the true Echinide, of which the common Lchwnus is the type. The compound plates of Stomechinus are made up of primary plates combined and modelled after the Diadema type and not after that of Hchinus or Strongylocentrotus. Desor placed this Oolitic genus with Achinus and Psammechinus, and apart from the Diadematide. The following is his diagnosis (‘ Synopsis des Echinides,’ p. 124) :— Urchins of moderate size, subconical, with pores distinctly tri- geminate as in the true Kchini. Peristome large, profoundly cut, no longer decagonal, but in the form of a pentagon, the bifid angles of which correspond to the interambulacra. Spines striated longi- tudinally and small. Stomechinus bigranularis, Lamk., sp., is the type, and its synonyms are Hchinus serialis, Wright, HL. intermedius, Agass., and E. arenatus, 436 PROF. P. M. DUNCAN ON THE STRUCTURE OF Lamk. Desor notices that the amount of the cutting of the peristome differs in the species, and that in some specimens of the typical species this characteristic peculiarity is not so intense as in others. Nevertheless Desor, with his usual sagacity, seized upon the cha- racter which of itself distinguished this genus from its fossil allies. There are numerous species, and the specimens, so far as I can make out, have some other distinctive structures equally important with that chosen by the founder of the genus. These freshly noticed characters, well known to all writers, are of great importance now that the structure of the ambulacra is decided. Taking a good specimen of Stomechinus bigranularis from the Great Oolite, it is seen that the apical disk is small and compact, the basal plates project well into the median line of the interradia, and this line is very bare and well marked by the vertical suture. The triangular basals have large generative pores and alone form the anal ring. The radials are wide at the adoral edge, which is notched, and the optic pore is in that edge. The tubercles of both areas are smooth, imperforate, non-crenu- lated, and not very unequal. The rows of tubercles diminish in numbers abactinally. The ambulacra are about one half of the width of the interradia above the ambitus, and at the peristome the ambulacra are nearly twice as wide as the interradia. The pores are in triplets, and above the ambitus the series of threes are very oblique and barely in arcs, but nearer the peristome they are more in arcs. The pairs are very numerous, and although there is a crowding towards the peristome still the pairs are in place. Near the radial plate the poriferous plates are low and broad primaries. A little way down, and where the first large tubercle is seen, three primaries have combined to form a compound plate, low and broad. The adoral plate of the compound is a low primary with a slight aboral bend, and the aboral plate is also low and broad, and it has an adoral curve where it comes in contact with the middle plate; this is low at the poriferous part and expanded towards and at the median line. There are no demi- plates. The cuts are well developed, and yet in a form which will for the future be accessible in the British Museum these branchial slits are not so very distinctive ; but there is always the great width of the ambulacra at the peristome and the remarkable diminution of the size of the interradia there. It appears therefore that, bearing in mind the deep branchial cuts of some modern Diadematidez; and the fact that these and other members of the family have bare median spaces, the peculiar shape of the component plates of the compounds, and the nature of the radial plates, Stomechinus must come amongst the Diadematide. Its position is clearly near Pedina, from which it is distinguished by the imperforate and non-crenulated tubercles, together with the deep branchial cuts. Genus Hemicrparis, Agass. The genus Hemicidaris, Agass., is very readily distinguished from THE AMBULACRA OF FOSSIL ECHINOIDEA. 437 all others, according to its founder and Desor, by the structure of the ambulacra of the species. Desor remarks (‘Synopsis des Echinides Fossiles,’ p. 51, plates x. and xi.): “The distinctive character is found in the ambulacra, which, in one part of their length, particularly towards the base and sometimes as far as the ambitus, are furnished with true tubercles, which are smaller than those of the interradia, but which like them are distinctly crenulated and perforated.” The generic diagnosis also notes that the pori- ferous zones are composed of two simple rows of pores which are fre- quently doubled at the peristome. If the narrowness of the ambulacra and the multiplicity of the pairs of pores are added to the above very definite characters, all that has hitherto been recorded about the morphology of the ambulacra will be found to have been stated. But the exceeding narrowness of the ambulacra above the ambitus, and the relatively narrow interporiferous area, coupled with the curving of long series of pairs of pores in relation to the great interradial tubercles placed near to the ambulacra, are necessary additions to the diagnosis. The species are numerous, and are Oolitic. Many of the forms from the Coral Rag are well preserved, and show structures which have hitherto escaped notice and which are of considerable classificatory importance. In Hemicidaris intermedia, Forbes, and Hemicidaris crenularis, the plates of the ambulacra near the radial end are simple primaries. Each pair of pores is in a separate plate which either is ornamented with a tubercle or only carries one or more granules (fig. 10). There is usually an alternation of small tubercle-bearing and granular plates. The sixth plate from the radial plate, on ambu- lacrum IT. zone a (fig. 10), specimen in Brit. Mus. no. 14122, may be taken as a type of the small primaries at this part of the Fig. 10 (see p. 452). ambulacrum, where the plates are numerous and narrow. The position of the peripodium is usually slightly oblique and close to the interradial edge, near the adoral suture. The plate is broader than high, and much of it is covered by the tubercle. This is low and has a mamelon which is perforated. The granule-bearing plates of this part resemble that just described, except that a granule occupies the position of the tubercle. Usually there is but one granule. The tubercle-bearing plate intrudes upon the granule-bearing plate, which is placed aborally, so that this last is often the smaller of the two. Besides the usual extension of the tubercle of the small primary plates very high up in the ambulacrum, an oblique direction of their adoral edge is often noticed; and it is evidently the result of the upward expansion of a plate which is situated adorally. Q.J.G.8. No. 163. 24 438 PROF. P. M. DUNCAN ON THE STRUCTURE OF From the effects of the obliquity of the adoral edge, the part of the plate near the interradium is greater in vertical measurement than that towards the median line. Numerous small and usually very low primary plates succeed, and in the ambulacrum under examination, wherever a granule-bearing plate is in contact adorally with a small tubercle-bearing one this last intrudes upon and deforms the other (fig. 11). Fig. 11 (see p. 452). The plates 15, 16, 17, and 18, of the same ambulacrum and zone, may be taken as typical of the greater part of the area halfway between the great tubercles at the ambitus and the radial plate. Plate 15 is a low primary with a very small mamillated boss and three minute granules. The interporiferous portion is on a slightly higher level than the poriferous area, and the aboral edge of the plate below (plate 16) fits into a space which is produced by this want of conformity of level. Plate 16 is of the usual height in the poriferous area, but it is forced up aborally by the expansion of the tubercle-bearing plate 17, situated immediately actinally to it, so as to conform at its adoral edge with the curve of the base of the tubercle. Hence this plate, which is very sparely ornamented with a granule or two, is almost linear towards the median line. Plate 17 has a small tubercle which occupies nearly the whole of a much expanded interporiferous area, the increase in growth being apical. The next plate, 18, is a low primary with granules, and it is not much deformed by the slight adoral extension of the above- mentioned tubercle. All these plates are primaries. Nearer the ambitus the fusion of primaries, forming compound plates with two pairs of pores, becomes evident. Thus at plates 35, 36, and 37 (fig. 12), this is well seen. Fig. 12 (see p. 452). Plate 35 is a primary, or, rather, was one before its adoral edge united, organically, with the aboral edge of the plate 36, and before THE AMBULACRA OF FOSSIL ECHINOIDEA. 439 this union produced a symmetrical plate towards the median line. The tubercle of plate 36 intrudes on plate 35, the adoral suture of which crosses the boss to reach the median line not far from the apical angle of the compound plate: this suture is curved, with the convexity directed adorally. A few granules are placed between the tubercle and the median line, and upon the apical part of plate 35. On comparing plates 35 and 36 with plates 16 and 17, it would appear that the resisting power of the plate 35 was greater than that of plate 16; but this is the first evidence we have of the direction of the aboral plate of a combination. It is important to observe that the poriferous area of plate 35 is higher in measurement than the part close to the median line. The tuberculiferous area of plate 36 is much larger than the corresponding poriferous area. The next plate, 37, is a small low primary, with granules, and the first step towards its organic connexion with plate 36 is the symmetrical arrangement of the granules in conformity with their place and trend in the two other plates 35 and 36, which certainly do form a double-pored combi- nation. The structure of the plates immediately aborally to the first large tubercle at the ambitus, counting from the radial plate, is simple as a rule, and differs in a remarkable manner from that of the great tubercle-bearing compound plates. Taking the Amb. III. of the species of Henwerdaris, and the zone “ a,” it will be noticed that the small compound plate placed aborally to the great tubercle, consists of three low primary plates united to form a symmetrical com- bination (fig. 13)*. The tubercle which is placed on this compound Fig. 13 (see p. 452). plate is small, and its boss is crossed, from the poriferous area to the median line, by the sutures of the aboral and adoral plates (37 & 39) where they are in contact with the edges of the central plate, which usually has themamelon upon it (38). The line of thesutures is almost transverse in most instances; but it may happen that the adoral plate of the combination is so jammed by the huge tubercle of the plate immediately on the actinal side, that it becomes a demi- plate, because it cannot reach the median line (fig. 14). The following is the construction of a large tubercle-bearing plate at the ambitus (figs. 13, 14). * Specimen 24122, British Museum. 2u 2 440 PROF. Pe Me DUNCAN ON THE STRUCTURE OF Fig. 14 (see p. 452). The tubercle covers nearly the whole of the three plates which compose the compound plate, and even the peripodia are on its slope. The tubercle, as is well known, is large and tall, has a sloping boss, a wide crenulated ridge and groove, and a large perforated mamelon. There are three pairs of pores surrounded by as many peripodia in immediate relation with the plate, and they are rather distant and in an are. (A pair situated adorally to the others is in connexion with the compound plate placed immediately actinally. Again, a pair which is on a line with the aboral edge of the tubercle belongs to the plate above.) On examining most specimens the only trace of a suture between any of the component plates is seen very generally as a depressed line on the side of the boss towards the , median line of the ambulacrum and passing towards the aboral and inner angle of the compound plate or rather of the tubercle. The direction of the line is apical and to the median line, and it reaches this last either slightly or considerably below the aboral angle of the compound plate at the vertical suture. But in many weathered specimens there is another and distinct suture visible, and it passes actinally from the crenulated edge over the adoral face of the boss, and it may reach the transverse suture with a gentle curve. On the poriferous side of the tubercle the first-mentioned suture is seen to be in relation with the highest of the three peripodia of the plate, to commence in the line of groove passing adorally to the obliquely placed first pair of pores, no. 40, and to reach up the side of the boss to the crenulated ridge, and then to cross the boss towards the median line. The direction of this suture may be in a right line or in a slight curve with the convexity looking actinally. The suture joins the aboral and central plates of the triplet,-and it leaves the mamelon adorally and pursues a more or less oblique course. It is clearly touched by the adoral pore of the pair. The shape of the suture and its direction determine to a great extent the shape of the aboral plate of the combination, and this is a primary plate with the poriferous area higher in vertical measurement than the opposite extremity, and with the inter- mediate part the highest of all. The next pair of pores, situated adorally to the last, are also obliquely placed, and on the edge of the boss (no. 41), and the adoral pore is in contact with a suture which passes inwards and up Ss THE AMBULACRA OF FOSSIL ECHINOIDEA. 441 the flank of the boss adorally to the crenulated ridge, and which then turns with a more or less wide angle to reach the suture between the tubercle-bearing plate now under consideration and that placed immediately adorally. But the suture does not reach the median line of the ambulacrum, for the plate (42) which it bounds aborally is a demi-plate *. This demi-plate, the third or adoral, of the compound tubercle- bearing plate (no. 42), varies in size in different tubercles and is always highest at the region of the boss. The central plate (no. 41), which is bounded actinally by the suture first described which crosses the tubercle obliquely, and also by that just noticed, is very large and is a primary. It is rather low at the poriferous area, but the height increases on the surface occupied by the mamelon, and all the inner part of the combination- plate is occupied by it towards the median line, except a small por- tion close to the aboral and inner angle which belongs to the highest of the triplet. Thus the great tubercle-bearing compound plate is composed of a large intermediate primary, a smaller aboral primary, and a large demi-plate (sometimes a primary) which is the adoral of the three. It is interesting to note that in shape the aboral plate re- sembles the corresponding plate in the genus Diadema, and that the adoral has frequently the outlines of the corresponding plate in Celopleurus, Duncan and Sladen, op. cit. All the great tubercle-bearing plates of Hemicidaris show the details just described, and if there is any variation it depends on the position and nature of the plate towards the peristome where the sutures come closer together. In the majority of ambulacra the next three plates, situated adorally to those just described, carry a large tubercle resembling in shape that noticed above, but smaller. The plates form a com- pound one, and the lines of their sutures and therefore their shapes are the same as in the compound plate just noticed. The peri- podia are in an arc, and are three in number, and the aboral plate of the triplet is a broad and low primary resembling that of the first tubercle-bearing plate ; the second is also a large primary, and the third or adoral plate is a demi-plate. The next compound plate is also a triplet, and so are all the others down to the peristome. The pairs of pores and their peripodia are closer, and the arcs are interfered with in consequence of growth and pressure; but the three peripodia of a tuberculiferous plate can always be distinguished, although the second peripodium of a series may be almost excluded. There is no addition of plates or pairs of pores, and the position of the pairs corresponds with that observed and described by Lovén in Strongylocentrotus, although the expla- nation he gave will hardly meet the instance of Hemicidaris. An important exception to the rule regarding the regular sequence of the ambulacral tubercles, occurs in some specimens. Thus in a * There is some variation in different specimens and the suture does reach the median line in some (see fig, 18). 449 PROF. P. M. DUNCAN ON THE STRUCTURE OF well-preserved specimen the first great tubercle-bearing compound plate of ambulacrum ITI., zone “a,” is followed apically by granule- bearing plates, two of which clearly form a compound plate ; but the third or adoral one seems to have become jammed into the aboral face of the tubercle-bearing plate below (fig. 15). Fig. 15 (see p. 452). It is evident that there are four plates in this compound one, and that the existence of the small demi-plate is due to the great pres- sure to which it was subjected whilst a primary. Henaeadaris granulosa, Wright, a species from the Inferior Oolite, of which there is a specimen in the Museum of Practical Geology, Jermyn Street, has the ambital compound plates made up of four primaries. The three placed actinally present the typical Diadema- arrangement, and the aboral plate is a low and broad primary (fig. 16). Fig. 16 (see p. 452). The same arrangement of four plates in a compound one occurs in Hemicidaris Wrightt, Desor, from the Great Oolite. In small and immature specimens of Hemicidaris intermedia the plates which bear the great tubercles at the ambitus are made exactly after the fashion of the simplest Pseudodiadema. In a specimen of H. pustulosa, Agass., in the Museum of Practical Geology, the suturing of the plates at the peristome is perfectly visible. The pairs are in triple series, and the plating is like that of the simple Psewdodiadema. It is certain that there is no trace of a demi-plate in these last three species. It is possible that the existence of a demi-plate in some of the specimens of H. intermedia may be an individual peculiarity; for in the specimen already noticed with a demi-plate jammed into the aboral part of a compound plate, there is another anomaly. The compound plates begin nearer the radial plate than is usual, and the plates of zone “a,” ambulacrum III., numbered 31, 32, and 33, form a triplet (fig. 17). THE AMBULACRA OF FOSSIL ECHINOIDEA. 443 Fig. 17 (see p. 452). It appears, then, that in the genus Hemicidaris the multitude of ' small primaries is succeeded by doublets or triplets and the great tubercle-bearing plates. These are either triplets after the Diadema- type, more or less modified, or have four pairs of pores, the additional pair being in a low primary, which has been joined to the aboral edge of a compound plate, or in a demi-plate (fig. 15). The influence of the growth of the large tubercles upon the spreading of the middle plate and the curvature of the adoral and aboral plates is very evident. Finally, it appears that the arrangement of the triplets when crowded at the peristome is not very remote from that seen in some abactinal parts of the ambulacra of species of Pedina. Genus Dirropop1a, McCoy. Small immature specimens of such types as Pseudodiadema versi- pora show a doubling of the pairs of pores near the apex unlike the condition which prevails in small specimens of the true Pseudo- diadema, which are unigeminal. This species, according to the principles which govern the classification of the recent Echinoidea, cannot remain in the genus Pseudodiadema, and must come within Diplopodia. Other forms are said to become diplopodous only at adult age, and this has been considered a sufficient reason for not placing them out of the genus Pseudodiadema ; but it was forgotten by the adopters of this reasoning that zoologists must consider the adult development of a form, and not its immature condition. A form with bigeminal pairs of pores in the upper part of the ambulacra is a Diplopodia ; and as yet I must confess not to have been able to recognize any forms about to become diplopodous. We can only deal with absolute facts, and not with presumptions. The question arises, leaving out the bigeminal nature of the pairs, Are the other generic characters sufficient to separate Diplopodia from Pseudodiadema? It appears that the diplopodous condition near the apex is accom- ‘panied. by crowding and doubling of the pores near the peristome, and, as a rule, by some departure of the pairs of pores in plates at the ambitus from a regular line or are. Moreover, the structure of the part of the ambulacra near the radial plates differs in the diplopodous series from that seen in the true Pseudodiadema. ‘There is not that blending of the small plates into compound ones which is.a character of Pseudodiadema. When there is such a combination as in Diplopodia Roissyi, Cott. 444 PROF. P, Me DUNCAN ON THE STRUCTURE OF (Echinides du Départ. de la Sarthe, par Cotteau et Triger, 1859, plate xxxiv. fig. 5), the propriety of calling the species a Diplopodia is doubtful ; for the pairs of pores resemble in their arrangement those of Pedina. The genus Cyphosoma, Agass., is characterized by the doubling of the pairs of pores near the apex; and this character is certainly developed with varying age according to the species. But the adults have the character, and the forms which are without it are placed in the genus Coptosoma, Desor. The alliance of Cyphosoma to the Pseudodiadema-group is evident from the common external characters, and there are points in the structure of the ambulacra which unite the genera and at the same time refer to the Triplechinide. DreLopopia VERSIPORA, Phill., sp., non Diplopodia subangularis, McCoy. This species, usually attributed to Pseudodiadema, is very familiar to the students of the fossils of the Coralline Oolite, and it has been figured by Dr. Wright (op. cit. plate vii. fig. 4). The nature of the construction of the ambulacra he not been given, except in a general manner. The diplopodous condition of the pairs of pores is well worthy of study, and it can be examined in a specimen in my possession. Taking one of the zones of an ambulacrum, it is seen that the first plate next to and in contact with the radial plate is a low and narrow primary, with the adoral pore close to the median line of the ambulacrum, and the aboral placed obliquely to it, the first- mentioned pore being also on the line of suture between the first and second plates (fig. 18). The second plate is at least twice the size of Fig. 18 (see p. 452). 1 the other, is slightly higher and much broader, and the adoral pore reaches the suture between this and the third plate, being - placed almost directly actinally to the aboral pore of the first plate. The aboral pore is far out of the vertical line of the corre- sponding pore of the first plate. Both of the plates are primaries, and do not form a compound plate. The third plate is high at the median line and very low at the ambulacro-interradial suture ; the THE AMBULACRA OF FOSSIL ECHINOIDEA. 445 aboral edge is transverse, and the actinal is oblique from the median upwards and outwards. The pair of pores is decidedly oblique, and the aboral pore is on a vertical line with the adoral pore of the second plate. Plate four is a primary with a large expansion in the poriferous part and a very low and almost linear interporiferous area. Its pair of pores are nearer the interradium than those of plate three. Plate five is a primary, its shape is irregularly rectangular, and it is larger than any of the plates noticed; the pair of pores can hardly be said to be one of the inner set, and there is a small tubercle close to the median line. Following the rule which has been observed in recent forms, this tubercle, being bound to grow in all directions. prevented the adoral growth of the plate immediately above. Plate six is low externally and higher somewhat towards the median line. Its pair of pores are in a peripodium, and they belong to the inner row. Plate seven, also a primary, is largest close to the interradial edge, where the pair of pores are, and it is almost linear towards the median line. It is decidedly broader than the other plates hitherto noticed ; andindeed every plate in this region becomes broader as the distance from the radial plate is increased. This plate is one of the outer set. Plate eight is very low externally, swells at the peripodium, and is higher at the median line; its pair of pores belong to the inner series. Plates ten, twelve, and fourteen belong to the same series as plate eight, and are formed after the same plan; they are all pri- maries, and have low and almost linear outer parts; the pores belong to the inner set and the plates are highest at the median line. On the other hand the plates nine, eleven, thirteen, and fifteen are upon the same type as plate seven, and belong to the outer series, with low and linear portions near the median line and enlarged poriferous Zones. sey In a young specimen the alternation of different-sized plates, all of which are primaries, extends at least to the twenty-fourth plate. Then the primaries become combined into a compound plate, some being blocked out, however, from the median line and becoming demi-plates. This condition is seen in adult as well as in young specimens, and just where the bigeminal pores begin to diminish and to be replaced by simple pairs. : The first compound plate is a tubercle-bearing one in the specimen under examination; there are four pairs of pores belonging to it and they are in double series (fig. 19). (The upper two pairs do not belong to the plate.) Fig. 19 (see p. 452). NX af 8 446 PROF. P. M. DUNCAN ON THE STRUCTURE OF The aboral pair, a, like the others, is oblique and in a peripodium. It belongs to the inner series, and is separated from the interradial suture by a rather large space, which is ornamented. The adoral pore of the pair is on the line of suture between the poriferous plate and the next in adoral succession, and the suture is curved with the convexity adoral, so as to reach the flank of the boss and thence to pass inwards and aborally, to the median line, and close to the aboral angle of the geometrical compound plate. This plate, with the aboral pair of pores, is of the Diadema-shape ; but the pores are remoter from the interradium than is the case in the genus Pseudo- diadema. The next pair of pores, 6, placed actinally, is close to the inter- radium, belongs to the outer set, and is in a peripodium. The plate is nipped in just adorally to the position of the first pair, and it then expands so as to include the mamelon and much of the boss and form the greater part of the compound plate near the median line. The adoral pore of the pair is in contact with the suture at the edge of the plate below, which is curved with the convexity aboral, and the suture reaches the median line slightly aborally to the actinal angle of the compound plate. This suture is the limit of the third plate, c, of the combination, and this has its pair of pores forming part of the inner series. The adoral pore of the plate (c) is on the transverse suture placed actinally to the compound plate. Finally the actinally placed plate, d, is a demi-plate which may seem to have nothing to do with the combination; but it forms a small portion of it, and the pair of pores belongs to the outer series. The plate does not reach further towards the median line than the position of the adoral pore of the pair of the third primary plate. There is no doubt that such a combination is not found in the genera Diadema and Pseudodiadema. Nearer the ambitus, or at that spot, the usual number of pairs of pores to a compound plate is four, the line of the pairs is simple, and the distribution of the composing plates is as in the species of Hemicidaris, that is, there are four primaries, of which the third is the largest (fig. 20). Fig. 20 (see p. 452). In some plates, however, there is a> demi-plate; and then the structure rather recalls the compound plates,of the Plesio- diademata. The doubling of the pairs of pores towards the peristome is almost a copy of that seen near the radial plate; there is no addition THE AMBULACRA OF FOSSIL ECHINOIDEA. 447 of new plates, and the triplets are all reducible to their normal position from which growth-pressure has forced them, on the principle elaborated in the instance of Strongylocentrotus &e. In very young examples of Diplopodia versipora the doubling of the apical pores is seen, and the large compound plates are of the Diadema-ty pe. In Diplopodia Malbosii, Desor, of Cretaceous age, the replace- ment of the ordinary demi-plate of the ambital plates by a low and curved primary is not uncommon, and both conditions may be seen in the same ambulacrum (fig. 21). Fig. 21 (see p. 452). Genus CrpHosoma, Agass. The genus Cyphosoma is diplopodous; but the structure of the ambulacra is different from that in Pseudodiadema and Diplopodia. Many of the species are polypores, and four, five, or six plates may enter into the construction of a compound and tubercle-bearing plate. Cyphosoma Konigi. is a very good example, and well- weathered specimens are common. They frequently show the line of partition between the component plates of the compound ones, or rather the lines may be distinctly seen passing from the adoral pores of the oblique peripodia up the boss, and more or less obliquely towards the mamelon. In the majority of specimens two sutural lines are seen on the flank of the boss which is opposite the peripodia and near the median line of the ambulacrum (fig. 22). These are perfectly visible in most cases. See figs. 22-25. Pe Ow DY oO OU One of these, that actinally situate, is seen to come from the 448 PROF, P. M. DUNCAN ON THE STRUCTURE OF adoral and inner shoulder of the crenulation on the boss, and to pass obliquely actinally and towards the median line of the ambulacrum. The line forms an arch, the chord of which is the transverse suture at the actinal edge of the compound plate. The other line starts from the abactinal and inner shoulder of the crenulation, and passes obliquely abactinally and towards the median line. Both of these well-marked lines are sutural, are between certain plates, and they both reach the median or vertical suture of the compound plates. The adorally situated line is the aboral limit of a primary plate, just as the aboral line is the limit of the aboral primary plate of the combination. A line can be traced from the first (the most abactinal) peripodium of the compound plate to the part of the crenulation at the aboral and outer shoulder of the poss; and there is little doubt of the continuity along the abactinal edge of the mamelon of the whole actinal line. The last peripodium but one of the compound plate, counting from the abactinal peri- podium, has a line passing from the adoral pore obliquely inwards and towards the nearest shoulder of the boss, and this corresponds with the aboral edge of the actinal primary plate of the combina- tion. Hence there is an adoral primary with a bent or curved edge, and there is also a similar actinal primary. ‘There is also a middle primary, the direction of the arching of the plates being opposite. In the compound plates with six peripodia there is an aboral primary, an adoral primary, and there are also lines of suture passing to the base of the mamelon from the 2nd, 3rd, & 4th peripodia (besides those from 1 & 5). -But, as in the instances of the com- pound plate with five peripodia, there are no signs of sutural lines passing down the inner flank of the boss corresponding to the 2nd, 3rd, & 4th lines on the outer or interradial side. There are, then, three demi-plates to the compound plates with six peripodia, and therefore there is a third primary plate, as there must also be in the combination ,with five peripodia. The position of the third primary is readily made out on the part of the tubercle-bearing plate near the median line, for it must relate to the expansion that exists between the inner ends of the aboral and adoral plates. But its position near the peripodia is a matter of doubt, in consequence of the homogeneous condition of the mamelon. The direction of the part of the plates close to the peripodia is, however, a somewhat correct guide where to look for the primary between the others. Certainly the first pair of pores is in relation to the aboral primary, and it is clear that the second pair is in a demi- plate. In most plates the narrow part between the demi-plate just noticed and the next line in adoral succession, passes either directly transversely or slightly actinally and towards the boss, and it is this direction which opens out two possibilities regarding the position of the middle primary. In the compound plates with five component plates, the peripodia (fig. 23, nos. 1, 2, 3, 4) have sutural lines represented by grooves passing from their adoral pores to the mamelon, but not so the fifth. Of these lines, nos. 2 & 3 pass up the boss to the crenulated groove THE AMBULACRA OF FOSSIL ECHINOIDEA, 449 and are then lost at the very base of the large imperforate mamelon. The lines converge, and as the other lines of union of the plates nos. 1 & 4 already mentioned also converge, a very marked feature results ; but there are no lines in continuation of those numbered 2 & 3 to be seen on the part of the tubercle near the median line and between the two very distinct lines already noticed. Conse- quently there must be at least two demi-plates, also the aboral and adoral primary plates, besides a middle primary. Fig. 23 (see p. 452). There is sometimes an appearance in compound plates consisting of five plates, as if the third plate from the abactinal edge were the middle primary (fig. 23). The fourth plate appears to be a demi- plate which joins on to the fifth or the adoral primary. This arrangement would be very exceptional amongst forms of Kchinoidea with many demi-plates ; nevertheless the position of the middle primary would be that seen in the Diadematide of the recent fauna, with the addition of a demi-plate placed aborally and adorally to the middle plate. It is also to be remembered that Alex. Agassiz gives a diagram of Phymosoma (Cyphosoma) crenulare, Agass., in the ‘ Revision of the Echini,’ plate vi. fig. 2,in which the middle primary has a demi-plate on either side of it, and the arrangement is the same as that now under consideration. But the species mentioned by Agassiz is not a Cyphosoma, for the abactinal pores are not diplopodous ; the form must come within a new genus. This diplopodous condition of the pores must be considered in investigating the formation of the ambulacral compound plates. In a specimen of Cyphosoma Kénigi, Mant., there is a compound plate higher than the ambitus, in which the diplopodous condition lingers on, and there are three double sets of pores (fig. 24). Fig. 24 (see p. 452). Oo rk WN & The rule is followed in the compound plate, with regard to the succession of the pairs, which prevails moré abactinally and where the double sets are not united in compound plates. The outer pairs of pores are in plates which are crushed and crowded out from the 450 PROF. P. M. DUNCAN ON THE STRUCTURE OF median line of the ambulacrum by the growth of the inner set. Plate 1 of the compound is in relation to an inner pair of pores and it is the aboral primary. Plate 2 is one of the outer set and it is a demi-plate which only reaches a very slight distance from the pair of pores. Plate 3 is in relation to an inner set of pores, and it is larger than the last, but still it does not reach the median line; it isalargedemi-plate. Plate 4is a small demi-plate and it belongs to the outer series of poriferous plates. Plate 5 is one of the inner series and is a large primary, the middle one of the three primaries. Plate 6 is one of the outer set and is a large demi-plate or possibly a primary. It is of the usual shape of the adoral primary in com- pound plates situated lower down. In a compound plate with six plates,in Dr. Wright’s collection, of which I took a diagram (fig. 25), there is little doubt that the diplo- Fig. 25 (see p. 452). podous condition must be considered as really affecting the relative dimensions of the plates. In the specimen (C. Konigz) the existence of an adoral and aboral primary is evident, and there is a large middle primary ; but it is in relation to the fifth pair of pores. The second, third, and fourth plates are demi-plates, and are arranged after the fashion of Strongylocentrotus, as described by Lovén. This is the same arrangement as is seen in the diplopodous compound plate. Under the circumstances the Cyphosomoid type of ambulacrum differs from the Diadema-type in its simplest expression, and also from the diplopodous type exemplified in Diplopodia versipora. The Cyphosomoid type may be said to unite the Diadematoid and the Echinoid types. LY. ConcLUSIONS RELATING TO THE TYPES OF AMBULACRA. It may be now assumed from the results of former observations, and from the consideration of the structures noticed in this essay, that there are certain well-defined types of ambulacra in the regular Echinoidea, 1. The Cidaroid type. All the plates of the ambulacra are primaries, and they do not combine to form compound plates. 2. The Diadematoid type. The newest plates are primaries, and at greater or less distance from the ambitus three primaries unite to form a compound plate, the middle plate of the three being the largest. (Journ. Linn. Soc. Zool. vol. xix. p. 95, 1885.) 3. The Arbacioid type. The newest plates are primaries, and at varying distances from the ambitus three primaries unite to form a THE AMBULACRA OF FOSSIL ECHINOIDEA. 451 compound plate, the middle plate being the largest, and the two others are smaller and become demi-plates in consequence of the growth-pressure exercised by the great tubercle of the compound plate. (Journ. Linn. Soc. Zool. vol. xix. p. 25, 1885.) : 4. The Echinoid type. This has primaries near the radial plate and then compound plates are seen of three or more plates combined. The middle plates are demi-plates and the primaries are aboral and adoral, or all the aboral plates may be demi-plates. (Lovén, Etudes, and Monogr. of the Fossil Echinoidea of Sind, Fase. Gaj Series, Pal. Indica, Ser. xiv. 1885, Duncan & Sladen, Hipponvoe.) 5. The Cyphosomoid type. This unites the Echinoid, the Diade- matoid, and the next or diplopodous type. 6. The Diplopodous type. The primaries near the radial plates are, in young forms as well as in the adults, arranged in a double row ; and this condition reaches to a greater or less distance towards the ambitus or even to the peristome. There is great diminution of the height or absorption of the non-poriferous parts of some plates. It is evident that while the Cidaroid type never varies, the Diadematoid and Arbacioid types tend to the Echinoid type in some instances on account of the formation of one or more demi-plates in a compound plate. It is also interesting to notice that the Arbacioids, which came later in time than the Diadematide, have the usual simple Cidaroid arrangement in the young plates near the radial plate, and at some distance down a plate or two on the Diadematoid type. Then come the true Arbacioid compound plates. The demi-plate came in with the Pseudodiademata, and became of importance in the construction of the compound plates of Cclo- pleurus and the later genera of Arbacioids. Finally the differences in the construction of the ambulacra necessitate the separation of the genera Plesiodiadema and Diplo- podia from Pseudodiadema. The only notice that I have been able to discover of the re- markable disposition of the plates of the Diadematidz is in the description of Heterodiadema ouremense by De Loriol (Recueil Zool. Suisse, t. i. no. 4, Sept. 1884, p. 626). There is a drawing given and a description of the triple plate, and they conform to the type of the true Diademata. I did not see this communication of M. de Loriol until the essay I have read before the Geological Society was completed. Cotteau gives indications of some sutures in many of his plates on the Echinoidea, but he does not describe the sutures or pay attention to them. DESCRIPTION OF THE FIGURES IN THE TEXT. Fig. 1. Two compound plates of Strongylocentrotus, after Lovén (p. 421). 2. A compound plate of Hemipedina Jardini, Wright (p. 423). 3. A compound plate of Hemipedina marchamensis, Wright (p. 424). 4, A compound plate of Hemipedina tuberculosa, Wright (p. 425). 5. Part of the ambulacrum near the ambitus of Pseudodiadema hemi- sphericum, Lamk. (p. 428). 452 PROF. P. M. DUNCAN ON THE STRUCTURE OF Fig. 6. A compound plate with a demi-plate of the same form (p. 429). 7. Two compound plates of Pseudodiadema depressum, var. (p. 480). 8. Two compound plates at the ambitus of Plesiodiadema Micheling, Agass., showing the numerous primary plates (p. 431). 9. A diagram of four compound plates of Pedina Smithi. a. Primary plates, 6 & c also primaries. a’ & ec’ are demi-plates (p. 433). 10. A single primary of Hemicidaris intermedia (p. 437). 11. More or less deformed primaries (p. 438). 12. The first compound plate from the union of two primaries, a third and ununited primary being beneath (p. 438). 13. Two compound plates of Hemicidaris crenularis. The lower plate carries a great tubercle. Amb. iii. (Brit. Mus. No. 24122) (p. 439). 14, Two compound plates of Hemicidaris crenularis (p. 440). 15. Two compound plates of Hemicidaris intermedia: the adoral plate of the upper series has been formed into a demi-plate by growth- pressure, and now forms a part of the lower plate (p. 442). 16. A plate of Hemicidaris granulosa, showing affinities with Plesiodiadema - 442). ive The Sieat triplet of a specimen of Hemicidaris (p. 443). . 18. The ambulacrum near the radial end of Diplopodia versipora (p. 444). 19. A compound plate of Diplopodia versipora, showing the persistence of the diplopodous arrangement (p. 445). 20. A compound plate of the same species with a low primary plate (p. 446). 21. Two plates of Diplopodia Malboszi, Desor. In the actinal there is the arrangement of Plesiodiadema, and in the other that of the Liassic Diadematide (p. 447). 22. A compound plate of Cyphosoma Konigi, Mant., with six plates showing the numerous sutural lines on the poriferous side and the two lines towards the vertical suture (p. 447). 23. A compound plate of the same species with five plates and the sutural lines (p. 449). 24. A compound plate from the same specimen showing the relics of the diplopodous arrangement, and indicating the alternation of large and small plates and the direction of the sutures (p. 449). 25. A diagram of the plates and sutures in a specimen of Cyphosoma K6nigi, in the collection of the late Dr. Wright, F.R.S. (p. 450). All these figures are magnified and more or less diagrammatic copies from nature, Discussion. Mr. W. Percy SxiapEn spoke of the importance of this communi- cation, both on account of its explaining points which were little known and forits bearing on classification. A.Agassizand Lovénhave cleared up some of the difficulties in the classification of the regular Echinoids, but probably this contribution to the question would prove of still moreimportance. He had himself had the opportunity of following and confirming Dr. Duncan’s observations, and expressed the strongest conviction that the structures indicated would shortly be shown to be of higher importance from a morphological point of view than had hitherto been supposed. Prof. SreLey said that it seemed to him that this was a most important contribution to zoological paleontology, and its importance would be more clearly seen as its bearings on classification and evolution were traced out. It showed the effects through genera- tions of crushing upon the characters of the ambulacral plates. The question then arises: As the plates are crushed together, forced THE AMBULACRA OF FOSSIL ECHINOIDEA. 453 downwards and partly absorbed by pressure, why do fhey group into certain definite associations of plates and half-plates? Prof. Secley Hid for many years had the opportunity of studying what had been written upon this subject, and he thought that much light had been thrown upon it by thispaper. He believed the growth “oF the inter- ambulacral plates had much influence on the form of the compound plates of the ambulacral areas. Dr. Murte considered that the paper was of great value from its recognition of physiological facts, and its indication of their bearing upon the theory of the evolution of organized forms. Mr. Eruerines called attention to the work of Dr. Wright on the characters furnished by the ambulacra in the study of the regular Echinoidea, and showed that Dr. Duncan’s contribution had brought into view the value of those investigations. The ambulacra were of vast importance in classification, and they were most difficult to examine. Lovén’s work, too, was of very great importance. The AvrHor, in reply, said that he had been much indebted to Lovén’s investigations. Doubtless the action of growth-pressure which he had referred to as “ crushing,” resulted in part in producing geo- metrical figures, the interambulacra acting as “‘ buffers” to the ambu- lacrai plates. The gradual formation of more complicated types was very interesting. The increase in the number of pores above the ambitus in the recent Diadematide certainly meant increase in power of respiration, Q). J. Gas.. No. 163, 21 454 T, M. READE ON THE ACTION OF LAND-ICE 32, Evrprnce of the Action of Lanp-Ick at Grear Crospy, Lanca- sHIRE. By T. Muriarp Reape, Esq., C.E., F.G.8. (Read May 13, 1885.) (Abridged.) In previous papers* I have described a deposit of rubble-débris and red sand lying on the Triassic rocks and underlying the Low- level Boulder-clay and sands in the neighbourhood of Liverpool, which I suggested was due to the grinding and crushing action of land-ice. I also pointed out that where this deposit did not occur, the rocks, as is well known, are usually polished, grooved, and striated. Until lately no opportunity has occurred of testing the validity of this view by reference to any other than sandstone rock that such land-ice may have moved over ‘. In October 1884 I described, in the ‘Geological Magazine,’ a section of Keuper marls at Great Crosby previously unknown, and since then I have made frequent observations of the upper part of the marls in relation to the Low-level Boulder-clay that overlies them. From time to time as the excavations have proceeded, it became clearly apparent that the upper part of the marls had been from some cause or other much disturbed. There were imbedded in it large angular and sometimes nearly square blocks of sandstone. These were not merely pressed into the surface, but actually imbedded in the marl at all angles. In the undisturbed marls are well-defined bands of a harder nature, and one of these bands was at one place broken up and contorted, the fragments displaced, and irregularly forced into and amongst the worked-up softer marls or shales (see fig. p. 405). This was very striking, as the band con- tinued in an undisturbed condition towards the south-west +. As fresh faces were disclosed by the progress of the excavations, it could be distinctly seen that in some cases the upper soft fissile marls had been forced up into contortions. The thickness of the dis- turbed bed was from 3 to 4 feet. The imbedded sandstone blocks were of two kinds: one a very fine- grained grey rock slightly micaceous ; the other composed of coarsely rounded grains, mostly quartzose. They are evidently sandstones . belonging to the Keuper series, though not found in this pit in sotu. Neither are they exactly like any of the Lower Keuper sandstone beds found in the quarry at Little Crosby, about one mile and a half to the north-west. 1am of opinion that they belong to beds under- lying those at the bottom of the pit, which at the north-east side approach in structure the coarser of the two sandstones. * « Drift deposits of the N.W. of England,” Quart. Journ. Geol. Soe. vol. xxx, p. 27; and vol. xxxix. p. 122. t+ Mr. Strahan, in his Survey memoir of the ‘ Geology of the Country around Chester,’ 1882, says “There is evidence of the passage of a heavy bady over the ground in the crushing and drawing out of soft beds as if by pressure” (p. 29). + The contortion of the beds below the eroded line in the section I consider to be due to earth movements. AT GREAT CROSBY, LANCASHIRE. 455 It was not until several examinations were made that I was able to discover any striations on the imbedded sandstone. At last I detected them on a block measuring 4 ft. x 2ft.10 in. x 1 ft. 9in. in extreme dimensions. On washing the marly clay off the face, very good parallel groovings were disclosed, running along the plane of bedding and the longer axis. With this clue I soon saw that the undersides of most of the stones were polished smooth, and others irregularly scratched. Section at Mowbrey Brick and Tile Works, Great Crosby. a,a. Grey shaly Keuper marl. 06. Hard band in Keuper marl broken off at 3’. 6", 5". Fragments of hard band, 6, scattered through and imbedded in the “ kneaded-up” marl. c¢,c. “ Kneaded-up” mar), that is the Keuper marl or shale, worked-up into a grey clay. d,d. Blocks of sandstone, some fine-grained and strong, others coarser in grain and often smoothed and striated, in one instance strongly fluted. ¢. Half-imbedded block f. Low-level Boulder-clay (marine), containing far-travelled erratics and broken marine shells (brown in colour). Specimens of the undisturbed marl and the kneaded-up marl were sent to Mr. David Robertson, F.G.S., who kindly examined them microscopically. No organisms were found in either, and they were practically of the same constitution. No far-trayvelled erratics, nor any stones or material that could not be referred to the Keuper formation could be found in the kneaded-up marl. Even the half- imbedded stones were, in all cases that I have seen, Keuper sand- stones. The true erratics are confined to the overlying Low-level Boulder-clay. This clay is so distinctive a deposit that it is only necessary to say that here as elsewhere it contains fragments of marine shells, and is undoubtedly of aqueous and marine origin. Importance of the Discovery.—The evidence of these disturbed shales is of importance taken in connexion with the prevalence in South-west Lancashire and Cheshire of glacial markings and smoothed rocks. At the present moment (March 1885) is to be seen a very fine example of polished and striated rock at Flaybrick Hill, Birkenhead, Cheshire, a veritable roche moutonnée which has only just been bared of its covering of Low-level Boulder-clay. Tt has, however, been a moot point with local geologists whether these markings are due to land-or floating ice. I have myself always considered that the weight of evidence preponderated in favour of land-ice, though there are some facts apparently irrecon- Ai2Z 456 ON THE ACTION OF LAND-ICE AT GREAT CROSBY, LANCASHIRE. cilable with that view. The phenomena described in this paper seem to me stronger evidence in favour of the land-ice hypothesis than any I had previously seen. It seems to me next to impossible that the disturbance of these shales could have been effected by floating ice in any form, and theentire absence of extraneous material in the *‘ kneaded-up marls ” lends further force to this view. It is not easy to get the exact direction of the dip of the shales ; but it is from north to south or between that and north-east to south-west. It follows from this that the lower beds must crop up towards the north, though the country is so buried in a mantle of Low-level Boulder-clay that the outcrop is not seen. If the dis- turbance of the shales were due to land-ice coming from the north or north-west (the nearest striz so far recorded are at Little Crosby quarry, 22° W. of N., and opposite the Police Station at Great Crosby, 40° W. of N.), the outcrop of the lower beds consisting of sandstones would be torn up and pushed over and into the kneaded-up shales at all angles, and this so far corresponds with the facts described. Some of these rocks may haye been glaciated in situ, and then broken off and pushed along and into the shales. The tendency of the foregoing facts and phenomena is towards proving that the period of greatest cold preceded the deposition of the Low-level Boulder-clay. This I have already pointed out, first in 1874 and in various papers since. Discussion. The PresIbEnT, while diindtiee that Mr. Reade’s evidence aahina to point to land-ice, said that it was difficult to imagine a glacier on so slight a slope as that between the Lake-country hills and Liverpool. Mr. Wuitsker insisted that the lower bed, having no erratics from a distant source in it, must have been of different origin from that with so many far-travelled blocks. Dr. Hixve said that the absence of far-travelled erratics in the till of the area described by Mr. Reade was a local and not a general characteristic of this kind of rock, since in the lake-region of Canada and the United States the till, which is believed to have been similarly formed by land-ice, contains an abundance of erratics from distant localities, though it is mainly composed of the debris of local rocks. The Avrnor admitted the difficulty suggested by the President as to the motion of ice from so distant a source as the Lake-district over so slight a slope. He believed, however, that the mechanics of land-ice remained to be explained ; but the facts he had recorded in the paper seemed to him quite irreconcilable with the theory that the deposit was formed by floating ice either as icebergs or shore- ice. In reply to Dr. Hinde, he stated that he did not think that the view that the Canadian Boulder-clay was due to land-ice was by any means proved to be the true one. ON AN ALMOST PERFECT SKELETON OF RHYTINA GIGAS. 457 33. On an almost perfect SxeLeton of Ruyrina cieas* (RHYTINA STELLERI T, ‘‘ SrELLER’s Sea-cow”), obtained by Mr. Rosert Damon, F.G.S., from the Pietstocenr PEat-DEposits on BEHRING’S~ Istanp. By Henry Woopwarp, LL.D., F.R.S., F.G.8., &e. (Read March 25, 1885.) Tue extinction of any group of animals by the influence of man or other agencies cannot fail to be a subject of interest to the paleontologist. Unfortunately the list of exterminated species has now become extremely large, and it seems impossible to doubt that in a few more years all the larger Mammalia not reduced to domestication, or under protective legislation, will have succumbed to man the destroyer. The musk-sheep, bison, giraffe, African elephant, wild deer, antelopes, and the iarge-horned wild sheep of the Alpine ranges, are all eagerly stalked down by the modern sportsman; whilst the hunter, in search of ivory, horn, bone, furs, or hides, wages a ruthless war of extermination against them all. The “fur-seal ” and the ‘“ whale-fisheries ”’ are still pursued ; and though the pursuit of the latter is now much diminished, the steady destruction of all the Pinnipedia in both the northern and the southern hemisphere continues with unabated ardour. I wish, very briefiy, to draw your attention this evening to a remarkable animal, now extinct, the Rhytina gagas (=Rhytina Steller’), commonly known as ‘“ Steller’s Sea-cow.”’ This interesting species of marine phytophagous mammal, onee no doubt abundant along the shores of Kamtschatka, the Kurile Islands, and Aliaska peninsula, but now entirely extinct, was first discovered by the eminent German naturalist Steller=, who, in company with Vitus Behring, a captain in the Russian Navy and a celebrated navigator of the northern seas, was with his vessel and crew cast away upon Behring’s Island (where Behring died), in 1741. We have fortunately preserved to us Steller’s original description of the animal, as seen alive by him, during his long enforced residence on the island; and no other competent observer has since had the same opportunity ; for between 1742 and 1782, a period of forty years, this large and harmless mammal appears to have been entirely extirpated, for the sake of its flesh and hide, around both Behring’s Island and Copper Island, to the shores of which in Steller’s time it was limited. The bones of the Rhytina are not to be seen anywhere lying upon the surface of the ground in either of the two islands, nor do they oceur along the shore at the level of the sea, but they are met with at a distance from the shore in old raised beaches and the Post- tertiary peat-mosses, deeply buried and thickly overgrown with » Zimmermann, 1780. Tt Desmarest, 1819. t “De Bestiis marinis, auctore Georg. Wilhelm. Stellero” &c. Mém. Acad. Sci. St. Pétersbourg (read 1745 published 1751), tom. ii . pp. 294-330. 458 DR. H. WOODWARD ON AN ALMOST luxuriant grass. It would be next to impossible to find them by digging, but they are found by boring into the peat with an iron rod or some such tool. The same method is adopted in the peat- deposits in Ireland, when one desires to find a timber-tree for gate- posts or other purposes; the resistance offered to and the sound emitted by the boring-rod, when in contact with a solid, is at once noticed by the operator. The specimen now in the British Museum was obtained from compact peat, and all the vertebrae: and other bones having cavities in them were full of peat-growth when they arrived, as was also the skull. I am informed that in Aliaska territory bones of the Rhytina have been obtained in a similar manner from deposits of peat. A detailed description of the Rhytina is rendered almost superero- gatory by the magnificent work of the late Dr. J. F. Brandt, of St. Petersburg, who in his monograph, ‘ Symbol Sirenologice,’ 1846-68, has left us a masterly and detailed account of the anatomy of this interesting genus, accompanied by admirably executed plates. Never- theless the recent acquisition by Mr. Robert Damon, F.G.8., of a specimen nearly as complete as that in the St. Petersburg Museum, and more so than Nordenskiold’s, seems deserving of a brief notice*. One of the contemporary writers on Rhytina with Brandt, after Steller, was Alexander v. Nordmann, Professor of Zoology in the Imperial University of Helsingfors, in Finland (see Beitrage zur Kenntniss des Knochen-Baues der Ithytina Steller, von Dr. Alexander v. Nordmann, 4to, Helsingfors, 1861, Acta Soc. Beient Fennice, tom. vil. with 9) plates). Rhytina: General Characters.—The Rhytina belongs to the order Sirenia, all the species of which are purely aquatic in their habits and of fish-like form of body, which led to their being formerly confounded with the Cetacea, from which, however, they are widely separated. The head in the Sirenia is rounded, and of miederate size, never disproportionately large, as in the Whales; the neck is short and scarcely offers any marked constriction between the head and body. The muzzle is truncated and obtuse, and the nostrils, which are placed above the fore part of the snout, are valvular and distinct. The external ear is absent, or very small; the eyes very small with an imperfect eyelid, but a well-developed nictitating membrane. The form of the body is depressed, fusiform, tapering behind, and without any dorsal fin ; the tail is flattened and expanded horizontally, as in the Cetacea. The fore limbs appear to be remarkably free, and capable of being moved from the shoulder-joint. Thus the living Manatee has been observed to use its fore limbs, “‘ manus,” to assist in bringing the food towards the mouth in feeding; and, as the mammary glands are axillary, the females all hold the young, in early life, under their arms 7. * The specimen has now been acquired for the British Museum (Natural History), Cromwell Road, London. t That the appearance of these grotesque animals, no doubt frequently seen PERFECT SKELETON OF RHYTINA GIGAS. 459 The pelvis in the Sirenia is ex- ceedingly rudimentary, consisting of a pair of small bones suspended at some distance below the vertebral column. (These have not been ob- ! served in Rhytina.) There is no lz trace of any hind limb; but a rudi- ie mentary femur has been noticed in ime another extinct form of Sirenian (Halitherium). ; 3 by Rhytina: The Head.—The head ie ¢. in Rhytima is small in proportion to eS, = oe the long and very thick body. The bones of the skull are massive, but very loosely connected together. Sir Richard Owen observes that this character of the skull, taken in connexion with the density of the bony skeleton, and the absence of cavities * in the bones themselves, reminds one of the skeleton of the Reptilia (Owen, “‘ On the Dugong,” Proc. Zool. Soc. 1838, pp. 28-45). The nasal bones are quite rudi- mentary; the maxillary border is narrow and straight; the premaxil- lary bones, forming the rostral por- tion of the skull, are long and con- siderably developed in front, forming the strongly curved border of the nasal opening, and projecting with Mi a a downward curve (as in Halicore, ee D> but less acute), its upper and outer tS) contour being very convex, and the SS ig lower and inner palatal surface being concave. The zygomatic arch is strongly developed and much curved. The occipital portion of the skull is the I 7. A GF “J ; af 7 Ye vs ee Ny { 94} UL poarosord [eurstIgQ “purest ‘MnuIsag “MOoT[oyg “Y= "uuyy “svsis euydAyy puyar ayp fo wozopyy—y] “Sq *(Aroqstyy [Binge yy) UnosNyY st} by the earlier voyagers, both in the East and West Indies and on the coasts of Africa, should have originated the legends of Mermaids and Sirens, seems at first = sight incredible; but art was then in its infancy in this country, and doubtless the engraver, who pourtrayed at second hand the features of the ‘ sea-siren,” had but little assistance in his delineation from the narrator. * Ornithopsis Sceleyi, Hulke, was not then discovered. (‘seyour 9 400f GT yyduorT) 460 DR. H. WOODWARD ON AN ALMOST broadest; the supraoccipital portion is very rugose, the condyles are semicircular and prominent, and the foramen magnum is very wide. The Lower Jaw.—The lower jaw is deep in proportion to its length. The coronoid process rises very little above the condyle itself. The symphysis of the mandible extends for about one third (or rather more) of its length, having a convex contour on its upper surface to correspond with the concave contour of the pre- maxilla. The symphysial surface is very rugose. ) Teeth absent or only Rudimentary Incisors—Two kinds of teeth (molars and incisors) are usually present in most of the Sirenia*. Dr. James Murie, in his elaborate and exhaustive memoir on the Manatee (Trans. Zool. Soc. vol. vill. 1872, pp. 127-202, pl. xvii.— XXv1.), observes: —‘ Although Rhytina was edentulous in the adult condition, I strongly suspect that, hke other Sirenian genera, rud?- mentary teeth may have existed in its earlier stages of growth. Nord- mann seems also favourably inclined to this opinion.” Trace of Rudimentary Incisors.—It is interesting to observe, in confirmation of Dr. Murie’s observation, that the skulls of Rhytina in the British Museum demonstrate the former presence of small rudimentary incisor teeth in the premaxillaries, two small alveoli being clearly shown; and the sides of these bones are swollen slightly, just where the pulp-cavities of these small incisors would have been present. Horny Palate.—As compensation for the absence of teeth in Rhytina, the palate and sides of the gums of both the upper and the lower jaw were covered by tough corrugated horny plates, of peculiar structure, which assisted in the process of mastication. With regard to the structure of the palatal and mandibular Jaminee, although their function was undoubtedly that of the tritu- ration of food, Prof. Brandt has shown tT that they are destitute of true bony or dental substance, and that they are in fact indurated epithelium. Dr. Murie has also expressed his conviction that the strongly ridged palatal plate in Rhytina is homologous with that found in Manatus and Halicore. “ It certainly,” he adds, ‘* does not appear to me to be the representative of teeth, nor of the baleen plates met with in the true Cetacea.” ‘The maxillary alveolar ridges are narrow and quite behind the bruising-plate, the latter occupying the intermaxillary and not the maxillary bones” (Murie, ‘Trans. Zool. Soc. vol. vii. 1872, p. 167). Cast of Brain-cavity secured —Advantage was taken of the loose and readily separable state of the sutures of the skull, to make a careful gelatine mould of the brain-cavity. The result is shown in the cast exhibited, which differs somewhat from the figure (similarly obtained) of the brain-cavity of Rhytina taken by Brandt. Brandt cited on Brain of Rhytina.—That author observes that, according to Steller, Rhytina has a small cerebrum, which is not * In Prorastomus canines are also developed; but Rhytina possessed neither. Tt Brandt, Mém. Imp. Acad: Sci. St. Pétersbourg, 1846, vi. série, pt. 11. Sci. Nat. vol. v. livr. iv. pp. 1-160, tab. i.—v. PERFECT SKELETON OF RHYTINA GIGAS. 461 separated from the cerebellum by a bony septum: he was unable to find any other peculiarity. He proceeds:—‘ As no brain was pre- served, the only means of knowing its form was by taking casts of the cranial cavity with plaster of Paris. In general character the brain of Rhytina is intermediate in form between those of Halicore and Manatus. In some points perhaps it is nearer to the former, but in others it approaches Manatus. The cerebral hemispheres higher and more elongated than in the Manatees; the posterior lobes of the hemispheres longer and higher than the anterior ones, convex above and impressed laterally, and the medulla oblongata projecting above, in the form of a median longitudinal crest; all show a resemblance to the brain of Halicore. The hemispheres of Rhytina are, on the contrary, shorter than in Halicore; the anterior lobes of the hemispheres of Rhytina are impressed on their anterior faces and not convex as in Halecore ; again the medulla oblongata of Rhytina is very broad, and the corpora clayata are more depressed from the sides than in Halicore, and remind one rather of Manatus. But besides the above-mentioned affinities to Hulicore and Manatus, fhytina also shows peculiar characters of its own. “Thus the anterior lobes of the hemispheres of Halicore are exceedingly convex ; in Rhytina they are even more so, and even higher than in the Manatee; they are depressed from the same cause, on the anterior surface, especially on the sides, but less than in Halicore and Manatus, but they overhang in the middle to a greater degree. The posterior lobes of the hemisphere of Rhytina, on their posterior border with the cerebellum, are broader than in the other genera of Sirenians before mentioned (and in this respect they are not unlike the same lobes in the elephant) ; they also show on the upper surface an oval convexity or furrow ; these then constitute peculiarities. The hemispheres of the brain of Rhytina further differ in this, that they appear to approximate very closely to one another. The cerebellum in Rhytina is depressed to a greater extent, and is broader and stronger than in the other genera. ‘The brain in Khytina affords therefore a form intermediate between Halicore and Manatus. Otherwise the brain of the Rhytina, considering the huge size of the body of the animal, seems to be six times smaller * in proportion than that of Manatus or Halicore. The plaster-cast of the brain of Rhytina shows traces of the small optic nerves, and of a very large fifth hypophysis showing a rounded prominence ’’?. Bones of the Ear of Rhytina Stelleri preserved.—The os petrosum of the periotic, with the tympanic annulus, is preserved on both the right and left sides of the skull. On removing the peat from the cavity of the mid-ear Mr. C. * This agrees with Prof. Marsh’s observations on the smallness of the brain in Tertiary mammals, and is in favour of the very high antiquity of Rhytina. See Marsh in Silliman’s Journ., ‘On the small size of Brain in the Tertiary Mammalia,” Srd series, vol. vii. 1874, p. 66, ibid. op. cit. vol. xii. 1876, p. 61 and vol. xxix. 1885, pp. 190-193. t+ Brandt, “ Symbolz Sirenologice,” fase. iii. 1878, p. 256. Tab. ix. Mém. de l’Acad. Imp. d. Sc. St. Pétersbourg, sér. vii. tom. x1. 462 DR. H. WOODWARD ON AN ALMOST Barlow (the formatore of the Geological department) discovered the three auditory ossicles still within the cavity. They agree very closely with the figures given by Brandt *, and are also near to the ossiculz auditus of the Manatee. The Stapes.—The stapes is a short columella-like bone, dationed at each end, having a small perforation (which may perhaps indicate the remnant of a much larger opening, the stirrup, observable in this bone in some other mammalia). It fits at one end into the fenestra ovalis, and unites at the other with the end of the incus. The Incus.—The incus is longer and stouter, and the superior and inferior faces are depressed, and the posterior process, the long crus, which articulates with the stapes, is shorter than in the Manatee and Dugong. The Malleus.—The body of the malleus is much swollen, more so than in the Dugong ; the superior face is convex, not depressed, as in Manatus latirostris. The external process of the malleus has a straight internal border (not arched as in Manatus) ; the external border is strongly arched (not truncated below) ; the external face is greater in breadth and is flatter than in Manatus. The condyles, articulating with the incus, are bilobed and depressed. Bones of the Scapular Arch and Fore Iamb.—The sternum has been figured by Brandt t. It is a much stouter and stronger bone than in the Manatee, but is similar in form. Scapula.—The scapula is somewhat convex externally, the inner concave face fitting closely against the anterior ribs to which it was applied ; the spinous process of the scapula is strongly developed. The glenoid cavity is deep and circular and well fitted to the rounded head of the humerus; the humerus is short and stout; the radius and ulna, which are also short, are anchylosed together at both extremities and incapable of any rotatory motion; the olecranon is strongly produced and curved, showing that the fore arm as well as the humerus had considerable free lateral movement for the act of swimming. The Manus.——The carpal bones and digits are unknown in Rthytina; the digits were probably five, as in Manatus and Halicore (but the thumb in the latter is rudimentary). Externally viewed the fore limbs in Rhytina were fin-like, with no external digits or nails visible; but Steller describes their extremities as thickly covered with short bristly hairs. Density of Skeleton—The skeleton is rem arkable for the massiveness of the bones, especially the great density of the ribs, which have the hardness of ivory. There is a general absence of medullary cavities in the bones. The great specific gravity of the bones no doubt assisted these * See also Claudius ‘‘On the organs of hearing in Rhytina,’ Mém. Acad. Imp. Sci. St. Pétersbourg, 1867, vol. xi. no. 5, 2 plates; Brandt, “‘Symb. Siren.” Fase. ii. pp. 8-10, Tab. 11. figs. 11-20. Mém. Acad. Imp. Sci. St. Pétersbourg, sér. vil. 1861. t I believed we also had in the Museum an imperfect sternum of Rhytina, and Prof. Flower, after comparison, agrees in this determination. PERFECT SKELETON OF RHYTINA GIGAS, 463 animals in keeping their large bodies sunk beneath the surface of the shallow waters in which they dwelt whilst feeding upon the marine vegetation upon which they wholly subsisted. Variations to the rule of seven Cervical Vertebre usually obtaining im the Mammalia.— Although the normal number of cervical vertebre maintained in the Mammalia is usually seven, yet some of the Sirenia (such as the ‘‘ American Manatee”) have only sia. Con- versely in Bradypus the number of the cervical vertebre is increased to eight or nine. This is explained by the fact that the thoracic vertebre in Bradypus pass into the cervical region, while the diminution to six in Cholwpus and in the American Manatee is similarly explained by the complete development of the rib of the seventh cervical vertebra. Rhytina has been described by Steller as only possessing six cervical vertebre, like the Manatee; but Brandt correctly gives the number as seven, and the specimen now in the Museum confirms this determination. The atlas- and axis-vertebre in Rhytina are fairly robust, and the atlas is as broad as the second dorsal vertebra; but the five remaining cervical vertebre, although quite free, are thin and plate-like, asin the Cetacea proper. But the Sirenia are distinguished from the true Whales by their capability of moving the head from side te side, and up and down, by means of the “‘ odontoid ”’ process of the axis vertebra on which the head rotates. In the Cetacea, in which the cervical vertebre are anchylosed together to a greater or less. extent, and the neck is consequently immovable, the odontoid process is also wanting. As the Sirenia spend their whole lives browsing upon the Lami- narie and other Algee and aquatic plants, this power to move the short neck pretty freely must be essential to them both in feeding and also in putting up their heads to breathe. The number of vertebree attributed to the Sirenia, both of living and extinct genera, is very variable according to different authors. Prof. Brandt attributed to Rhytina 7 cervicals, 19 thoracic or dorsal vertebre, and from 34 to 37 lumbar, sacral, and caudal. The cervicals and dorsals are readily determined ; but, as none of the vertebre are anchylosed together to form a sacrum, it is a matter of some difficulty to decide which are lumbar and which are sacral vertebree. Not only does anchylosis never occur in the vertebree of the Sirenia, but the flat ends of the centra of the vertebrae do not ossify separately so as to form disk-like epiphyses in the young state, as is commonly the case in all the other Mammalia. Brandt indicates the 7th vertebra beyond the last of the dorsal or thoracic series as bearing the rudimentary pelvis ; but as the ver- tebree are never anchylosed to form a sacrum, we can only conjecture (by noticing a slight prominence upon the posterior border of the extremely wide transverse processes) which of these lumbar-sacral vertebre seem marked as sacral, probably about the 5th, 6th, and 7th. The 13 vertebre. next behind the dorsal series may, from their 464 DR. H. WOODWARD ON AN ALMOST size and their wider and longer transverse processes, be considered lumbar and sacral, and the 21 following vertebre as caudal; about 6 or 8 of the most anterior of the latter had small chevron-bones or heemal arches attached to them in the St. Petersburg specimen. The transverse processes in the caudal series are much smaller, thicker, and shorter, and are directed obliquely backwards. Variation in form of the Centra in the Vertebral Column.—There is a marked change in the form and size of the neural arch and the centrum of the several vertebre in the spinal column, from before backwards. ‘The anterior dorsal vertebrae have each a small com- pressed centrum, much broader than deep; the neural arch is triangular, the neural spine erect. From the 5th to the 8th dorsal the centra are longer and cordi- form, and the neural canal is smaller and more rounded ; the neural spine bends backwards, and the zygapophyses are more prominent. The lumbar vertebree are much dilated laterally, the centra being nearly three times as broad as deep. The neural canal is reduced in size, and the neural spine is moderately large; but the transverse processes are very flat, long, broad and straight, being in relation to the centrum as 5 to 1. The centra of the caudal vertebre are rounder, the transverse processes are short and stout and bent backwards ; the neural canal is reduced to a very small size, and the neural spine gradually disappears. The earlier caudals Ls short V-shaped chevron-bones or r hemal arches. The 11th to 16th thoracic or dorsal vertebree case irregularly - developed hypapophyses on the ventral surface of their centra. There are 19 pairs of ribs in RAytina, probably not more than two pairs of which were articulated to the sternum. The Ist and 2nd pairs are short and much compressed laterally, the third and following are round and very massive, and increase in curvature and length up to the 12th, when they gradually become shorter and less curved, the 19th being quite rudimentary. This large number of rib-bearing vertebre in the Sirenia is only equalled in Elephas and Rhinoceros, and only exceeded in Dendrohyrax (which has 22 costal vertebre), thus affording another point of analogy in Rhytina to the Ungulata*. The ovoid visceral cavity thus enclosed within the bony walls of the ribs is of vast dimensions ; and one realizes readily the statement that a full-grown male, covered with its integument and flesh, weighed as much as 34 tons. Habits of Rhytina, &e.—The Sirenia pass their whole life in the water, being denizens of the shallow bays, estuaries, lagoons, and _ * The teeth in Manatus and Halitherium approach in form to the molars in Hippopotamus, Mastodon, and the Suide. Dr. Murie strongly insists upon the dermal characters as offering a very close resemblance between Manatus and Elephas. The short (rudimentary) nasal bones and the prolonged premaxillaries, with their tusk-like incisors, afford further points of resemblance with the Proboscidea. PERFECT SKELETON OF RHYTINA GIGAS, 465 large rivers; but they never venture far away from the shore. Their food consists entirely of aquatic plants, upon which they browse beneath the surface, as the terrestrial herbivorous mammals feed upon the green pastures on land *. When Steller came to Behring’s Island in 1741, the Sea-cows pastured in the shallows along the shore, and collected in herds like cattle. As they fed, they raised their heads every four or five minutes from below water in order to breathe before again descending to browse on the thick beds of sea-weed which surround the coast. They were observed by him to be gregarious in their habits, slow and inactive in their movements, and very mild and inoffensive in their disposition. Their colour was dark-brown, sometimes varied with spots. The skin was naked, but covered with a very thick, hard, rugged, bark-like epidermis, infested by numerous parasites. When full-grown they are said to have sometimes attained a length of 35 feet and a weight of 3 or 4 tons. Like most of the Herbivora, they spent the chief part of their time in browsing. They were not easily disturbed whilst so occupied, even by the presence of man. They entertained great attachment for each other ; and when one was harpooned, the others made incredible attempts to rescue it. They were so heavy and large that, Steller records, they required 40 men with ropes to drag the body of one to land. Fossil and Recent Allies of Rhytina.—In Miocene and Pliocene times Sirenians were abundant over a large portion of Europe. Many of these are referable to the genus Halitherium, first described by Kaup from the Miocene of Hesse Darmstadt. Halitherium resembled the Dugong in its dentition (fig. 3), having tusk-like incisors in the upper jaw, though these were not so largely developed asin Halcore. ‘The molar teeth were 2 or $, the anterior teeth were simple and single-rooted, the posterior teeth of the upper jaw with three roots, and those below with two roots, and with enamelled and tuberculated or ridged crowns, in all which points they resemble the Manatee more than the Dugong. The anterior molars were deciduous. The pelvic bones are better developed than in existing Sirenians (fig. 2); there is also a rudimentary styliform femur. They were therefore less specialized than their modern representatives (Flower). In Prorastomus (Owen) from the Tertiary of Jamaica, the denti- tion is very remarkable ; for we have present at one and the same ; c c ohne DES 5 Nest time, clearly differentiated—incisors 75, canines j—, premolars 5—5 3—3 =z, and molars =—.=48 teeth. * Mr. William Carruthers, F.R.S., F.G.S., informs me that the large sea- weeds called Laminarie grow in water at or just below low-water; they are nutritious and are eaten by animals. They abound in the North Pacific Ocean. Ruprecht, in his account of the Algz of the North Pacific, records eight species of these large weeds growing in the Sea of Ochotsk, on the shores of Kamts- chatka, and the north of North America. He adds :—‘‘ When I went to see the Coniferous trees at Monterey, California, last autumn, I was surprised at the magnitude and quantity of the Fuct and Laminarig thrown up on the coast.” sop ‘YdV) 18ST “puysumrecy . DR. H. WOODWARD ON AN ALMOST ‘soyntd ogaunb 104 pur ‘(of ‘dd *y ‘jory ‘puvg *y ‘sutor0A “sopoos ‘urotyapoyyt yA rsnisdoy ‘AT “4 ‘A(T UOA ‘sUOoog LoZUILT, Sop OUOAIG OTISSOJ OIP “Lewryogy wongvayzy MET UO MOWOETAL O9G Le cil Suse Se ‘SoYOUL Q Jooy J YRSUOT "pvoy pfoMuToIH ‘(Aroqyst]T [VAngvNT) WMosN AL YSHItg oy} UL MON ‘snisdo'y "YT 9) “1 ‘Jorg Aq poavdord ‘umnosnpy ypeysuareqE oy} woafy MouMTods oY} Jo 4svo OY} Wo.ty poydvasojoyg (gprysutre(y 48 WHOSN, OY} UL UOJOPOYS potoysoa oy} AOYPY) ‘spOsuumg ‘ounvorpyy ‘,dnny “Wuryoy WHiLLoYyyT[S FT f0 wojpapayJ~—G SLi] 466 PERFECT SKELETON OF RHYTINA GIGAS. 467 Halicore (fig. 4), at first sight, seems widely separated, and appears to approach towards the condition of Rhytina, having in the adult Fig. 3.—Dentition of Halitherium Schinzi, Kaup. A. Left half of the palate. B. Part of left ramus of mandible. Fig. 4.—Dentition of Halicore australis. Queensland. A. Left half of the palate. B. Part of left ramus of mandible. state only one pair of incisors left in the upper jaw, and two (rarely three) molars on each side above and below, making 14 teeth in all, But, adding the milk-dentition, we have Q ahi 1—1 oe Milk-dentition 33 2a e Incisors. Molars. 3-5 Permanent teeth = = rarely -— The teeth in Halicore are more or less cylindrical ; the incisors in their form and wear resemble those of the Hippopotamus. The last molar is compressed laterally, giving the crown a figure-of- eight shape; but there is no distinction into root and crown. The ns of the crown are tuberculated before wearing ; afterwards they a are flattened or slightly concave. 468 DR. H. WOODWARD ON AN ALMOST In which disappear. The molars amount to + ae = the upper Alara have two ridges and three roots ; the lower mandibular series have an additional posterior ridge or talon, and only two fangs. Fig. 5.—Dentition of Manatus senegalensis. West Coast of Africa. : A. Left half of the palate. B. Part of left ramus of mandible. The teeth drop out in front, and are renewed from behind as in the Proboscidea. This extreme variation in the number of the teeth from 2 to 48 is exactly paralleled in the Cetacea, in which we have many eden- tulous species (Baleenidz); others with only two teeth present (Zi- phioid Whales); others again with very numerous teeth (Delphinide). All the earlier voyagers confounded the Sirenia with the Seals, and the Rhytina with the Morse or Walrus. In 1811, Illiger separated the three genera—Manatus, Halicore, and Rhytina, under the name Sirenia, and placed them between the Seals and the Cetacea. They are now placed by Prof. Flower and other naturalists between the Ungulata and the Cetacea. The following is a List, with their distribution, of the eaisting species of the order Sirenia :— Manatus senegalensis, Desmarest (the African Manatee), inhabi- ting the west coast of Africa from about 16° N. to 10° S. lat. and as far into the interior as Lake Tchad ; and according to native accounts, to the River Keebaly, 27° E. long. Manatus latirostris, Harlan (the West Indian Manatee), inhabi- ting the creeks, lagoons, and estuaries of the West Indian Islands and coast of Florida. Manatus americanus (the Brazilian Manatee), inhabiting the coast as far south as about 20° S. lat., and the great rivers of Brazil almost as high as their sources. Hahcone tabernanle (the Dugong) inhabiting the Red Sea and the east coast of Africa. Halicore dugong, inhabiting the Indian Sea, Ceylon, Bay of Bengal, Indo-Malayan Archipelago, and Philippine Islands. Halicore australis, the coasts of Kastern and North Australia. PERFECT SKELETON OF RHYTINA GIGAS. . 469 Passing to the West Indies, we find a fossil species from thence haying important differences in dentition, by which to separate it from the now living Manat. Three other species occur in the Tertiary beds of South Carolina; and a doubtful form in the deposits of Darling Downs, Queensland, Australia. Lastly, there is the extinct Rhytina of Behring’s Island now under notice. We have, then, at the present day living in America, Africa, India, and N.E. Australia, two genera and six species of Sirenia ; and in Europe, Africa, and America, 12 genera and 27 species of extinct Sirenians. Conclusion.— Distribution of the Strenia.—There are, it appears to me, two very important points in connexion with the Sirenia which are worthy of our special attention as geologists and paleon- tologists. I allude to the present and the past distribution of this order over the world. If we take the belt of tbe tropics, that is 233° N. and 232° S. of the equator (or, better still, say 30° N. and S. of the equator), we shall cover the geographical distribution of all the living Stirenians. If we take another belt of 30° North beyond the tropic of Cancer, we shall embrace the whole geographical area in which fossil remains of Sirenians have been met with. Assuming, as I think we may, that the Sirenia at the present day belong exclusively to the tropical regions of the earth, and that Rhytina, in its boreal home, was simply a surviving relic from the past (a sort of geological “outher,” as of a stratum elsewhere entirely denuded away), we must conclude that the presence of about 12 genera and 27 species of fossil Sirenia, as widely distributed then as the recent forms are at the present day, but with a range from the tropic of Cancer up to 60° of north latitude, affords a most valuable piece of evidence (if such were needed), attesting the former northern extension of subtropical conditions of climate which must have prevailed over Europe, Asia, and N. America, in Eocene and Miocene times and in the older Pliocene also. The early appearance of so highly modified a form of mammal, its abundance, distribution, and variations, serve to attest the great lapse of time occupied in the accumulation of even our later Tertiary deposits, which we are sometimes apt to pass over as representing but a very brief chapter in the geological history of our earth; and further, it must necessitate our carrying back the Mammalian class four into Secondary times. Note.—Drifted remains of Manatee (either from Florida or from the West Indies) are recorded as haying reached our shores, probably on the waters of the “‘ gulf-stream,” in 1785. The carcass of one of these animals was washed ashore at Leith ; it was much disfigured, but Mr. Stewart informed Dr. Fleming that it was the putrid body of a Manatee, or Manatus borealis. (Bell, Brit. Quadrupeds, 8vo, 1837, p. 525.) Q.3.G.8. No. 163. 2 470 DR. H. WOODWARD ON AN ALMOST The following is a list of fossil Sirenia, with formations and localities :— Chirotherium subapenninum, Bruno. Pliocene: Piedmont. Mem. Acad. Sci. Tor. ser. ii. vol. i. (1839) p. 148. | Chronozoon australe, C. W. de Vis, Proc. Linn. Soc. N. 8. Wales, 1883, viii. p- 382, pl. xvii. Pliocene: Darling Downs, N.S. Wales. Crassitherium robustum, Van Beneden. Pliocene: Belgium. Diplotherium Manigaulti, Cope. Miocene?: 8. Carolina; Proc. Acad. Philad. 1883, p. 52. Enotherium egyptiacwm, Owen. Eocene?: Mokattam, Cairo; Quart. Journ. Geol. Soc. vol. xxxi. p. 100. Felsinotherium Forestii, Capellini, 1872. Pliocene: Riosto, Bologna; Mem. dell’ Acad. delle Sci. dell’ Istit. di Bologna, ser. iii. tom. i. fase. 4, pp. 605- 634, tay. i.—vil. —— Gervaisii, Capellini, 1872. Pliocene: Siena, op. cit. pp. 634-642, tay. viii. (Felsinotherium closely resembles Halicore :—i. Lm: 2 2.) Halitherium Serresti, Gervais. Pliocene: Montpellier ; d’Estrés (Bouches-du- Rhone) ; Gervais, Zoologie et Paléontologie Frangaises, 2nd edit. Paris, 1859, p. 277. fossile, Cuv. sp. Miocene: St. Maure, Loire; Angers, Rennes, Morbihan ; Gervais, op. cit. p. 281. Beaumontii, Christol, sp. Miocene: Beaucaire, Gard, Gervais, op. ct. p. 281. —— Guettardii, de Blainy. Miocene?: Etréchy (Seine), &. &c. Gervais, op. Cit. pp. 281, 282. , sp. —— dubium, Cuv. Eocene: Blaye, Gironde, Gervais, op. cit. pp. 281, 282. bellunense, Zigno, 1875, Mem. del Reg. Ist. Veneto, vol. xviii. part iii. 1875, pp. 438-44, tav. xiv. figs. 1-5, tav. xv. figs. 1-7. Miocene: Belluno, Venetia. angustifrons, Zigno, 1875. Miocene: Belluno, op. e¢ loc. cit. pp. 441-443, tay. xvi. figs. 1-4. curvidens, Zigno, 1875. Miocene: Belluno, op. e¢ loc. cit. pp. 443-445. tay. xvii. figs. 1-4. veronense, Zigno, 1875. Miocene: Belluno, op. et loc. cit. pp. 445-449, tay. xviii. figs. 1-10. : Schinzi, Kaup, Beitrage zur naheren Kenntniss der urweltl. Saugeth. 1855. Miocene: Darmstadt; Miocene: Malta. Canhami, Flower. Crag (derivative); Quart. Journ. Geol. Soc. vol. xxx. . 1-7. eee eee Owen. Miocene: Montpellier. sp., Van Beneden. Miocene (“ Bolderian”): Elsloo, near Maestricht. —— (Chirotherium) Brocchii, Bruno (Owen, cit.). Miocene: Herault. , sp., Zigno, Mem. Ist. Venet. vol. xviii. 1875, pp. 427-453. Miocene: Chalaif, Isthmus of Suez. Hemicaulodon effodiens, Cope. - Hocene: Shark River. Manatus Coulombi, Filhol (1878) (named after M. Coulomb, the discoverer). From the Eocene ? Quarries, Mokattam, near Cairo (founded on three teeth of lower jaw like the Manatee); Bull. Soc. Philom. de Paris, 7° sér. tom. ii. pp. 124, 125. inornatus, Leidy. Miocene?: Phosphate beds, South Carolina; Rep. U.S. Geol. Survey, i. p. 336. Pachyacanthus trachyspondylus, Brandt (in part), Van Beneden, emend., 1875. Miocene: Nussdorf, near Vienna ; Bull. Acad. Roy. Soc. 2nd ser. t. xl. 1875, pp. 823-340. (Based on vertebre and ribs of a Sirenian,) Zool. Record vol. xii. 1875, p. 14. Prorastomus sirenoides, Owen. Tertiary: Jamaica; Quart. Journ. Geol. Soc. 1855, vol. xi. pl. xv. figs. 1-6, vol. xxxi. pp. 559-567. Rhytina gigas, Zimmermann, Geograph. Gesellsch. 1780. Pleistocene: Behring’s Island, = Rhytina Stelleri, Desmarest, 1819. Rhytiodus Capgrandi, Lartet. Pliocene: Basin of the Garonne. pie is Raulini, Gervais. Miocene: La Réole, Gironde, op. cit. pp. 282, a PERFECT SKELETON OF RHYTINA GIGAS, 471 We thus see that remains of Sirenians are met with over the greater part of Europe (in England, Holland, Belgium, France, Germany, Austria, Italy), and in the deposits of analogous age in the Isthmus of Suez at Chalaif, and the quarries of Mokattam near Cairo, in Africa. Bibliographical Inst of Works on the Strenia. Srecter, G. W. ‘De Bestiis marinis, auctore Georg. Wilhelm. Stellerc, Descriptio Manati seu Vaceze marinz Hollandorum, Sea-cow Anglorum. Russorum Morskaia Korowa, occise d. 12 Jul. 1742, in insula Behringii, Americam inter et Asiam in Canali sita,” pp. 294-330, 1745. Mém. Acad. Sci. St. Pétersbourg, t. ii. 1751. Branpt, J. F. “Symbol Sirenologice.” Mém. Acad. Imp. Sci. St. Péters- bourg, 1846, 6™° Série, ii. Part, Sci. Nat. v. vol. 4"° liv. pp. 1-160, Tab. i—v. Ibid. 7me Série, vol. xi. pp. 1- 383, Tab. i.-ix. NorpMann (A. yon). “ Beitrage zur ‘Kenntniss des Knochen-Baues der Rhytina Stellert.” to, Helsingfors, 1861. Acta Sci. Fenn. tom. vii. Buarnvitte (H. M. de). ‘ Ostéographie ou Description Iconographique comparée du Squelette et du ee Dentaire des cing Classes d’Animaux Vertébrés récents et fossiles.... ouvrage accompagné de planches lithographiées sous sa direction par M. I. C. Werner.’ Texte, 4 tom., & Atlas, 4 tom. 4to, Paris, 1839-64. Kaup (J. J.). ‘Beitrage zur naheren Kenntniss der urweltlichen Saugethiere.’ Heft. 1-5. Ato, Darmstadt, &e. 1854-61. Bruno. “Illustrazione di un nuovo Cetaceo fossile.” Mem. Acad. Sci, Tor. ser. li. vol. i. pp. 143-160 (with 2 plates). Lepsius, Prof. G. R. “Der foss. Sirene, Halitherium Schinzi, d. Mainzer Beckens.” Abhandlungen mittelrheinischen geol. Vereines. Srerecer, L. Proc. United-States Nat. Mus. vi. 78; records discovery of Rhytina in Commander Islands. Wautacez, A. R. ‘Geographical Distribution of Animals,’ 1876, vol. i. p. 119. Leivy, Prof. J. Description of Vertebrate Remains from the Phosphate Beds of South Carolina.’ Philadelphia, 1877, p. 214; and Holmes, ‘Post-Pliocene Fossils of South Carolina.’ Owen, Ricuarp. “ Description of the Anatomy of the Dugong from Penang.” Proe. Zool. Soc. Lond., Mar. 27, 1838, pp. 28-45. Rogsr, CO. “Liste der bis jetzt bekannten Saugthiere.” Corresp.-Blatt. d. Ver. Regensburg, 1880, p. 165; 1881, pp. 27, 52, 117, & 162. DysowskI, B. Proc. Zool. Soe. 1883, p. 72; Zool. Record, 1882 (835), p. 35. Frantzivs. In Wiegmann’s Archiv, 1869, pp- 300-304 : ‘““Manatus americanus, Notes on the Distribution of, in Central America.” Branpt, J. F. ‘‘ Notes on the Extinction and former Distribution of Rhytina,” Bull. Imp. Acad. St. Pétersbourg, xi. 1867, pp. 445-451. —. “Cyamus Rhytine.” Mém. Acad. St. Pétersb. 1871, vol. xvii. No.7; and Ann. & Mag. Nat. Hist. 1872, pp. 306-313. Cuavupivs, Prof. ‘On the Organs of Hearing in Rhytina.” Mém. Acad. Sci. St. Pétersb. 1867, vol. xi. No. 5, 2 plates. Kraus. “ Manatee (the pelvic arch-bones of).” Arch. Anat. Physiol. 1872, pp. 257-292. . ‘“Halicore.” Op. cit. 1870, pp. 525-614. Moris, Dr. J. “On the Form and Structure of the Tinea: ” Trans. Zool. Soc. vol. viii. 1872, pp. 127-202, plates 17-26. Owen, Ricuarp. ‘‘Anatomy of the Dugong.” Proc. Zool. Soc. Lond. 1838, p- 28-45. Gaerne Paun. “ Hxtinct Sirenia.” Journal de Zoologie, tome i. 1872, p. 332. Norpensxioup, A. H. ‘The Voyage of the Vega round Asia and Europe,’ in 2 vols., vol. ii. pp. 272-281. Gurvals, Pavu. ‘Zoologie et Paléontologie Francaise,’ 2nd edition, 1859. Frowsr, W.H. Order Sirenia, Article “ Mammalia,” in Encyclopedia Britan- nica, 9th edition, vol. xv. 1883, pp. 389-391. ——. Article “ Manatee,” op. cit. pp: 456, 457. Auten, J. A. “ Cetacea soe Sirenia,” Bull. U.S. Geol. Surv. vol. vi. p. 99. 2K 2 472 ON AN ALMOST PERFECT SKELETON OF RHYTINA GIGAS. Discussion. Prof. Bory Dawxins thought the evidence brought forward sup- ported the view that we are still living in the Tertiary period. He thought Halicore was as highly specialized as Prorastomus. He believed the multiplication of teeth was connected with the aquatic habit. Dr. Moniz pointed out that the characteristics of the whole group of the Sirenia allied them to the Cetaceans, Pachyderms, and pos- sibly the Ungulates. He insisted on the similarity of the skin of the Sirenia to that of the Elephants. The heart, blood-vessels, bones, muscles, and viscera of the Sirenia are all peculiar. He referred to the differences of the tail in different genera of Sirenia. He did not agree with the enumeration of recent and fossil species, as shown in the diagram. He thought that there might be two, but possibly only one, living species of Wanatus, and one of Halicore, while many of the so-called species of Halithertwm would not stand. The AvtHor, in reply to Prof. Boyd Dawkins, pointed out that the presence of canines and differentiated molars and premolars indi- cated Prorastomus to be a more highly specialized form. That the multiplication of teeth in aquatic forms is not a universal rule is shown by the edentulous Rhytina. j i i j ‘ Quart.Jdourn Geol. Soo -Vol. Xl. Pl XIV. S$ Poord del et lth . GN Mintern Bros. imp STERNAL APPARATUS OF IGUANODON. us es J. W. HULKE ON THE STERNAL APPARATUS IN IGUANODON. 473 34. Note on the STERNAL APPARATUS 7n IGUANODON. By J. W. Horxs, Esq., F.R.S., F.G.8. (Read June 10, 1885.) [PuatTe XIV.] One of the few parts in the osteology of Jguanodon upon which the rich series of Bernissart fossils preserved in the Musée d’Histoire Naturelle at Brussels, so ably worked out by M. Dollo, and con- cerning which the numerous remains discovered in our own country have hitherto not afforded any certain information, is the sternal apparatus*. A specimen which I lately had the pleasure of seeing in the rich collection of Jguanodon-remains made from the Wealden Beds at Hastings by 8. H. Beckles, Hsq., F.R.S., a Fellow of this Society, appeared to me to supply the desired knowledge. Mr. Beckles readily acceded to my wish to bring it under the Society’s notice ; and I tender him my warm thanks for his permission, and also for most courteously placing this and other fossils at my disposal for examination and study. The piece which I identify as part of the sternal apparatus is an azygos bar, from near one end of which two lesser rods diverge laterally, one from each side (Pl. XIV. fig. 1). Each of these rods (cl) has an expanded mesial end, a contracted cylindroid shaft, and a swollen outer extremity. The expanded, mesial, ends are applied to that surface of the azygos bar which I regard as ventral, approaching each other here so closely as to leave between them only a very narrow interval in which the bar is visible. Their dimensions are as follows, viz. :— SUSE AL Sta es eae ei Be ONO hee OD a) 22-5 cm. react ot mesialiend ) 2 oo eae oes see... Gb Se Ae shaft at.its middle 0 2).3 000... 0) We Longer diameter of outerend .............. Toe Extreme distance between outer ends ........ - 46°5 ,, The identification of these divergent rods with the bone cemented by rock to an Jguanodon scapula in the British Museum (recognized first as clavicle by Mr. W. Davies), and also with the two bones figured by M. Dollo as the right and left moieties of the sternum (Pl. XIV. fig. 2), will not, I think, be questioned. Some minor * Other parts of the pectoral arch—the scapula and coracoid—have long been known, the clavicle more recently. The latter was first, I think, recognized as such by Mr. W. Davies. His identification was accepted by Prof. O. C. Marsh, and subsequently by myself, with some reservation (Quart. Journ. Geol. Soc. Vol. xxxIx, p. Gn): 474 J. W. HULKE ON THE STERNAL APPARATUS IN IGUANODON. differences are, I think, fairly attributable to mutilation and com- pression. The symmetry of their junction with the azygos bar strongly favours the belief that we see here preserved the undis- turbed normal relation of the several parts. On this supposition the two divergent rods occupy precisely the position, and they have the same relation to the azygos bar or interclavicle (Pl. XIV. fig. 3, icl) as the clavicles in extant Lacertilia ; for the apposition of their outer ends to the process termed “ acromial ” on the anterior border of the scapula will hardly be doubted. The azygos piece (Pl. XIV. fig. 1, icl) has the form of a long flattened bar, the width of which appears to increase slightly from that which I regard as its anterior end to a point about 9°5 c.m. behind the clavicles, and thence to decrease slightly to the posterior extremity. The anterior extremity, which advances slightly in front of the mesial ends of the clavicles, is indented at its middle. The posterior margin is nearly straight, but I do not feel certain that this is a natural edge, and that the bar may not originally have been somewhat longer. The lateral borders for the space of 7 c.m. behind the clavicles to the point where the bar attains its greatest width are smooth and arcuate, suggestive of having formed a small segment of a long curved articular groove for the reception of an epicoracoid ; whilst the remainder of the border behind this is rough, uneven, and apparently non-articular. A mesial ridge or low keel divides the bar longitudinally. Its greatest elevation is about 1°5 ¢.m. Measurements of Azygos Bar. PEN SGh i wierate oe atric ee Seen nee 39°4 ¢.m. Width at anterior extremity ........ HeisOn ss Maximum width, behind clavicles.... 15:3 ,, Length of exposed arcuate part of lateral margin about ..:.-.....:2. aahed Ome Pte Width at posterior end of bar ...... bO-O G35 What is this azygos bar? ‘That it comprises the interclavicle (Parker) (=episternum of some authors, the clavicular sternum, Hoffmann), is, I submit, demonstrated by its connexion with the clavicles, which, as I have already said, agrees with that obtaining in existing Lacertilia. But does it comprise the sternum (costal sternum, Hoffmann) also? Marks of connexion of coste with its lateral borders would be decisive of this, but none are recog- nizable. The extent. of the arcuate part of the lateral border is quite incommensurate with the size of the arc which we know the mesial border of the epicoracoid must have had. Lastly, the figure of the azygos bar is quite unlike the shield-like sternum of extant Lacertilia and Crocodilia. These considerations weigh with me in regarding the azygos bar as an interclavicle only—the homologue of that of now living Lizards, and of the bony sternum, so called, of extant Crocodiles. If this view is correct, the bar was splinted to a shield-like sternum J. W. HULKE ON THE STERNAL APPARATUS IN IGUANODON. A475 bearing ribs. The non-recovery of such a sternum by Mr. Beckles, when we bear in mind that under his personal superintendence a very considerable part of the skeleton, including both fore limbs, was exhumed, favours the suggestion that I threw out in my Pre- sidential Address in 1882, that the sternum in Jguanodon may have been cartilaginous, as in living Crocodiles. EXPLANATION OF PLATE XIV. Fig. 1. The clavicles with the interclavicle. Halfnatural size. In Mr. Beckles’s collection. 2. The bones suggested by Dollo as the moieties of the sternum. 3. Schema of the restored pectoral arch. The following lettering applies to all the figures:-—c/, clavicle; zc/, inter- clavicle; cor, coracoid; ep. cor, epicoracoid ; sc, scapula; ¢s, cost; st, (carti- laginous?) sternum. Discussion. The Prestpent congratulated the Author on the interesting’ dis- covery he had made in connexion with the anatomy of the Dino- saurs. 476 J. E. MARR AND T. ROBERTS ON THE 35. The Lower Patzozorc Rocks of the NetcHBourHoop of Haver- FoRDWEST. By J. E. Marr, Esq., M.A., F.G.S., Fellow of St. John’s College, Cambridge, and T. Ropsrts, Esq., B.A., F.G.S., St. John’s College, Cambridge. (Read June 10, 1885.) [Pate XV.] § 1. Introductory. Tuer country around Haverfordwest is of great interest to geologists, . first, on account of the evidence furnished therein of the relations of the graptolite-bearing beds to the strata which are characterized by the presence of higher organisms, and secondly, from the nature of the foldings which the rocks of the district have undergone. We propose, in this communication, to devote our attention to the former of these subjects. Our work is based upon that which has been done by the Geo- logical Survey, and published in Sheet 40, Horizontal Sections, Nos. 1 & 2, and Mem. Geol. Survey, vol. ii. part i. Whilst fully acknowledging the great value of these publications, we think it desirable, now that our knowledge of the forms of life occurring in these rocks has been so much increased by the labours of many geologists in recent years, to attempt a more minute classifi- cation of the rocks of this district than that adopted by the Govern- ment Surveyors. In our opinion, this further description of the beds will throw considerable light upon the character of the movements which the district has undergone. Our thanks are due to Dr. Hicks for the very kind way in which he placed a series of specimens collected by himself at our disposal. We have also to thank Prof. Lapworth for his kindness in examining our collection of graptolites. The area which we have chiefly examined is a well-defined tract (see Map, Pl. XV. fig. 1), about eighteen miles in length from east to west, and having an average breadth of five miles, lying to the north of the towns of Haverfordwest and Narberth. It is bounded on the north by a great fault, running from Roch Castle in an easterly direction, along the margin of a mass of rock which Dr. Hicks has claimed as Pre-Cambrian. On the west and south, the Lower Paleozoic rocks of this tract are succeeded by Old Red Sandstone and Carboniferous deposits, and on the east, a considerable extent of Llandeilo limestone is represented on the Geological Survey map. Within this area is a portion of a wide synclinal, complicated by minor foldings, running from near Clynderwen Station on the east, to the Coal-measures on the west. South of this is a complicated anticlinal in the neighbourhood of Narberth. § 2. Establishment of the Succession. 1. Lingula Flags.—To the north of the great fault alluded to as wid ; Wels Ate eo ‘poe, laligalet ve? ee Rha bn 0 Behe 4 PAA eee “) inlay) : A Si gir Pee) bi at + © So awe waar Skea IS Foy pice oS ’ am , t hws ged ’ me * EEO IA Bray [o> Quart. Journ. beat. Soc. Vol. XLT. PL. XV. Fig.1. Geological SketchMap, OF THE NEIGHBOURHOOD or HAVERFORDWEST. Scale 3 Inch=1 Mile. >>. Slebech [roe | eck Hill et Slade Stages. Fig. 3. SECTION THROUGH ROBESTON WATHEN. Length of Section, ? mile. |. Dicranograpius Shales, 4. Red Huh Stage. 2, Reebeston Wathen Limestone. 5. Slade Stage. 2 Summit of Sholeshook Limestone Stage. 6. Conglomerate. 7. Sholeshook limestone. 4. Grit. 3. Sholeshook Limestone Stage. 2. Red Hill Stage. 5. Lower Elandovery./2) much folded. 8 Slade Stage. tobeston Wathen& Yo le.s/took Lamestomes Did : ingula |Sxa ee gat “Sales. THES Be Archean Koudts. Fis. 4. SECTION IN Lane N. oF PRENDERGAST CHURCH. mS Length of Section, 3 mile 2 us : ; = ¥ 1. Dicraegraptus Shales. 2. Caleareous summit of ditto. F. feed Mill Stage. 5, Slade Stage. ee Fig. 2, Quarry S.E. oF TREFGARN BRIDGE. , Length of Section, about 20 yards. a => SSS 7. Archean, about 18 fi.seen, 4. Shales with Olenus &€© 2. Gnglomerate. 5. Drift. & Grit. 6. Debres. Fig. 5. Diacram-SECTION ALONG RAILWAY FROM HAVERFORDWEST STATION To NORTH OF CRUNDALE. Length of Section, 1$ miles. Sholeshook s. "Lane E.of \ Radway. Brock. MAP AND SECTIONS OF PALZOzOIC ROCKS NEAR HAVERFORDWEST. DanceRric.o, Lith, 22, Beororp ST Covent Ganven 7025/7865) M a rr m 7 vp te ) bes LOWER PALZZOZOIC ROCKS OF HAVERFORDWEST. A477 running eastward from Roch Castle, north also of the Pre-Cambrian ridges, parallel with this, are black iron-stained slates, weathering olive-grey or yellowish, generally dipping north. They are well seen near Leweston, Trefgarn Bridge, and Spittal Cross. At Lewes- ton Old Mill they have yielded :— ceoes pisiformis, Linn. | Olenus spinulosus, Wahi. , var. socialis, Tallb. At Trefgarn Bridge the following very important section occurs in a quarry by the roadside, close to the fourth milestone from Haver- fordwest (fig. 2) The shales are considerably disturbed, and contain a fair number of fossils of the same species as those found at Leweston Old Mill. The conglomerate adheres to an ashy-looking rock of Pre-Cambrian (?) age, with nearly vertical divisional planes, the origin of which we were unable to determine. The fossils found in these two localities prove that these beds are Lingula Flags. Dr. Hicks has recorded the presence of Lingula ‘Flags about this spot (Q. J. G.S. vol. xxxy. p. 287), but gives no fossil list; and it is interesting to find that his determination of the age of the beds, based presumably upon lithological characters, is fully borne out by the fossil evidence. To the south of the great fault, much newer beds occur, so that we are unable to record the occurrence of Tremadoc and Arenig fossils in the area under consideration. © 2. Didymograptus Shales.—These beds occur in the complicated anticlinal to the east of Narberth, and, next to the Lingula Flags, are the oldest beds we have met with in the tract of country we have examined. They consist of black graptolite-shales of the ordinary type, crowded with “tuning-fork” Didymograpti, and con- taining also small horny brachiopods and fragments of trilobites. Didymograptus Murchisoni occurs in abundance. That these beds are underneath the Llandeilo limestone is shown by their occurrence in an anticlinal arch between the limestone of Llan Mill and that of Lampeter Velfry. The southern arch of this anticlinal is vertical, and even reversed in places, but it is indicated as an anticlinal in the horizontal section No. 2 of the Geological Survey. The lime- stone of Lampeter Velfry is a faulted synclinal, and to the north occurs another anticlinal, between Lampeter Velfry and Llandewi Velfry, and here again the Didymograptus-shales are found, and have yielded Didymograpti by the roadside west of “‘ Ll” in “ Llandewi Velfry.” The same fossils are found in similar shales near Whitland, below the limestone, but at some distance from its outcrop. Prof. Lapworth (Ann. & Mag. Nat. Hist. Ser. 5. vol. iii. p. 59) also places the Didymograptus-shales of this area below the Llandeilo limestone. 3. Llandeilo Limestone.—The well-known black limestone of Llan Mill, Lampeter Velfry, Llandewi Velfry, &c., interstratified with black shales. Itis frequently crowded with fossils, and the following A78 J. E. MARR AND T. ROBERTS ON THE are preserved in the Geological Survey Museum from the limestone of this region :— Monticulipora favulosa, Phill. Trinucleus favus, Salt. Beyrichia complicata, Salt. Leptzena sericea, Sow. Calymene cambrensis, Saiz. Orthis striatula, Conr. Asaphus tyrannus, Murch. &e. &e. The limestone is also seen north of Stoneyford, on the road between Narberth and Clynderwen Station ; and similar limestone, which has, however, not furnished us with any fossils, occurs at Bullhook and Camrose, as marked on the Geological Survey map. 4. Dicranograptus Shales—These beds immediately succeed the _ Llandeilo limestone of Llandewi Velfry, and are seen above the lime- stone quarry at “ P” in “ Parsonage.” They are black shales, with some grit bands, and are usually crowded with graptolites, including Dicranograptus ramosus, Climacograptus bicornis, &e. We have nowhere seen a section giving the complete series. At Llandewi Velfry there is room for about 50 feet of shales between the Llandeilo limestone and the beds above the shales, but it is very doubtful whether the whole of the shales are now represented here. The uppermost beds of the series certainly occur at this locality. They are well-defined, flaggy and sandy black shales, characterized especially by the abundance of Orthis argentea, His., and may there- fore be spoken of as the zone of Orthis argentea. Dr. Hicks (Q. J. G. S. vol. xxxi. p. 178) also places the Llandeilo limestone between the Didymograptus- and Dicranograptus-shales. Confirmatory sections.—The Dicranograptus-shales are exposed to a considerable extent to the north of the complex synclinal. On the west side of the Western Cleddau, they occur much folded in the neighbourhood of Camrose, and at Camrose Mill the Dicrano- graptus beds are again seen succeeding the Llandeilo limestone. At Wolfsdale they have yielded Ogygia Buchii. On the east side of the Western Cleddau the beds set in at Rudbaxton, and we have found graptolites at Green Plain, south of Trefgarn Bridge. At Clarbeston-Road Station also graptolites occur. The beds can then be traced in several sections along the railway as at Pendwr, Long- ridge Bridge, and Blaen Waen, between Clarbeston-Road and Clyn- derwen Stations, and they appear to overlie the Llandeilo limestone south of Bullhook, although the two are not in close proximity. These beds are also brought up by folds to the south of this. North of Stoneyford they lie immediately over the Llandeilo limestone. The Orthis-argentea zone is seen near Grondre, at Robeston Wathen, and at Prendergast, but no Llandeilo limestone is exposed at these places. We have then several independent sections showing the Dicrano- graptus-shales immediately succeeding the Llandeilo limestone, and the latter may, indeed, be looked upon as merely a calcareous development of the black shales which occur below, within, and above it. The fossils, other than graptolites, of the Dicranograptus-shales, occur chiefly in the Orthis-argentea zone, with the exception of LOWER PALAOZOIC ROCKS OF HAVERFORDWEST. 479 Ogygia Buchit. In that zone we find Turrilepas sp., Pleurotomaria and Orthoceras. Siphonotreta micula also occurs in abundance, as well as in lower zones, and other horny brachiopods are common. 5. Robeston Wathen Inmestone.—This deposit is best known as occurring at the village of Robeston Wathen, where a quarry to the north of the church contains a black limestone with interbedded black shales, dipping 8.S.W. The calcareous bands are crowded with Halysites catenularius, and other fossils occur, including Orthis elegantula, Dalm. Trilobites are rare and fragmentary. (It is to be noticed that many of the fossils from this locality in the Jermyn-Street Museum are not from this limestone, but from higher beds, to be described presently.) As the section here is an important one, a figure of it is added (Pl. XV. fig. 3). The graptelite-shales are seen by a stream immediately below the quarry, dipping under the limestone. These shales belong, as stated. above, to the Orthis-argentea zone, and the limestone itself appears to be a calcareous development of the upper part of these shales. Confirmatory Sections.—Near Grondre, two miles north-west of Robeston Wathen, the same limestone is seen, as represented on the Geological Survey map. It is crowded with Halysites, as at Robeston Wathen, and is here nearly vertical. In a quarry, at this place, the ‘black limestone is associated with an ashy-looking limestone which yielded a cystidean, and which is apparently the representative of the lowest stage of the next series ; but the relations of the two were not determined. Fossils of the black limestone at Grondre :— Syringophyllum organum, Linn. Ilznus Bowmanni, Sa/z. Halysites catenularius, Linn. Orthis Actonix, Sow. Petraia zquisuleata, M‘Coy. To the north-east of the limestone quarry, in a small quarry in a field close to Grondre farm, the Orthis-argentea shales are dipping north. The limestone strikes as though it would pass above the shales. The tract between Grondre and Robeston Wathen is much disturbed, newer beds being faulted and folded in. At Llandewi Velfry, the Orthis-argentea shales, which occur some way above the Llandeilo limestone, pass up into flaggy black limestone like that of Robeston Wathen. At Fron, 12 mile north-east of Llandewi Velfry, where the Llan- deilo limestone is not seen, the Orthis-argentea shales are found in a small roadside exposure, dipping a little north of west; and on the hill-side to the west of this and above it, black limestone is exposed in a quarry, presenting an appearance quite similar to that of Robeston Wathen, also with abundance of Halysites, and amongst other fossils the following :— Heliolites interstinctus, Wahl. Glauconome disticha, Goldf. dubius, Schmidt. Orthis Actoniz, Sow. Petraia xquisulcata, M‘ Coy. calligramma, Dali. elongata, Phill. Leptzna transversalis, Wahl. Illznus Bowmanni, Saiz. | Strophomena rhomboidalis, Wilck. At Prendergast, north of Haverfordwest, the Orthis-argentea a a elie 480 J. E. MARR AND T. ROBERTS ON THE shales are seen ina lane north of the church, dipping north, and they are very flaggy and calcareous towards the summit, but lime- stone bands do not occur as in the above localities. The section seen in this lane, and in a quarry immediately to the east of it, is shown in Pl. XV. fig. 4. 6. Trinucleus-seticornis Beds.—These are subdivided into three stages, Viz. :— (a) Sholeshook limestone. (6) Redhill shales. (c) Slade calcareous shales. The beds succeeding the Robeston Wathen limestone consist mainly of blue-grey shales, weathering olive-green, with a con- siderable development of calcareous matter at the base and summit. The form Tyrinucleus seticornis, or its variety Bucklandi, occurs throughout, and is very characteristic of these beds, which may therefore be spoken of as the Trinucleus-seticornis beds. (a) Sholeshook Limestone.—At Robeston Wathen, the central part of the quarry, as shown in the section (fig. 3), contains the upper portion of these beds immediately succeeding the Robeston Wathen limestone. It differs considerably from that limestone both lithologically and palzontologically. Whereas the black limestone is evidently a calcareous development of the black shales, the caleareous band we are now considering is no less clearly a member of the blue-grey shales; and this is also true of the lower zones which occur in other localities. The following fossils occurred in this calcareous band :—Heliolites interstinctus, Wahl., Glyptocrinus: basalis, M‘Coy, Trinucleus seticornis, His., Phacops Brongniarti, Portl., P. alifrons ?, Holopella, Orthoceras. The actual limestone appears to have been crushed out at this point, the fossils occurring in calcareous shales which are elsewhere seen immediately above the limestone itself. Confirmatory Sections—At Prendergast, as seen in fig. 4, the uppermost member of the Orthis argentea beds, which is there calcareous, is succeeded by greenish, impure limestone, crowded with fossils, especially trilobites, although the limestone itself is much crushed. The fossils are similar to those of Robeston Wathen, but are much more abundant. The following occur :— Halysites catenularius, Linn. Homalonotus ? Petraia. Trinucleus seticornis, var. Bucklandi, Crinoid and cystoid fragments. Barr. Tentaculites anglicus, Sal¢. Agnostus trinodus, Sai¢. Phacops mucronatus, Brongn., var. Orthis elegantula, Dalm. alifrons, Salt. ? Leptena quinquecostata, M*‘ Coy. Cheirurus bimucronatus, Murch. juvenis, Saiz. sericea, Sow. tenuicincta, M‘Coy. octolobatus, M‘Coy. Strophomena rhomboidalis, Wilck. Lichas laxatus, M/‘Coy. Ctenodonta ? Stygina. Bellerophon bilobatus, Sow. Cybele verrucosa, Dalm. Orthoceras. Ilenus Bowmanni, Sal. Cyrtoceras sonax, Salt. At Sholeshook a splendid section is exposed in the railway- LOWER PALZ0ZO1C ROCKS OF HAVERFORDWEST, 48] cutting. The beds here are of the same nature as at Prendergast, but the calcareous matter is mainly collected into nodules. The general dip is northerly, and the beds which appear to dip under the Sholeshook limestone are probably newer beds brought down by a faulted overfold. To this part we shall refer presently. Although the Sholeshook section does not assist us in determining the rela- tionship of this calcareous band to the older beds, it is important as containing so many fossils, and being a well-known fossil locality. The following list of fossils from this place is compiled from the specimens in the Jermyn-Street Museum, those collected by ourselves, and those noticed by Tornquist (Ofy. af K. V.-A. Foérhandl. Stock- holm, 1879, No. 2, p. 70). Favosites fibrosus, Goldf. Cybele verrucosa, Dalin. Chetetes petropolitana, Pand. Loveni, Linnrs. Cystideans (cf. Mem.Geol.Sury.vol.iil.). | Enerinurus sexcostatus, Salt. Beyrichia strangulata, Salt. Cheirurus bimucronatus, Murch. Agnostus trinodus, Salz. octolobatus, M*‘ Coy. Ampyx tumidus, Forbes. —— juvenis, Sa/f. Trinucleus seticornis, His. Sphzrexochus boops, Saiz. , var. Bucklandi, Barr. angustifrons, Anq. Remopleurides longicostatus, Pordl. Phacops aratus, Salt., MS. radians, Barr. Brongniarti, Port. dorso-spinifer, Porti. Glauconome, n. sp. _ Stygina latifrons, Por?l. Lepteena sericea, Sow. TIilenus Bowmanni, Salt. tenuicincta, M*Coy. Lichas laxatus, M‘Coy. . Orthis testudinaria, Dalm. Calymene fatua, Sal¢., MS. calligramma, Dalm. Cyphaspis megalops, JZ‘ Coy. Cyrtoceras sonax, Salt. Phillipsia parabola, Barr. Trochoceras cornu-arietis, Sow. At the schoolhouse north of Pelcomb Cross (3 miles north-west of Haverfordwest), the Orthis-argentea shales are seen by a small stream to the west of the road, dipping in a southerly direction. South of this, a quarry by the roadside contains beds apparently overlying the Orthis-argentea shales. These consist of crushed calca- reous shales of a greenish colour, quite like those of Sholeshook and Prendergast. There is room between the Orthis-argentea shales and the quarry for the Robeston Wathen limestone, but no exposure is seen. This quarry is probably the place from which Prof. Phillips obtained the fossils mentioned in ‘ Memoirs of the Geological Survey,’ vol. li. pp. 235 et seg. The following occur here :— Agnostus trinodus, Salt. Staurocephalus globiceps, Port. Ampyx tumidus, Forbes. Phacops Brongniarti, Porti. Cybele Loveni, Linnrs, Phillipsia parabola, Barr. Encrinurus sexcostatus, Salt. Trinucleus seticornis, var. Bucklandi, Tllenus (young). Barr. Cheirurus bimucronatus, Murch. These beds can be traced to the north of West Pelecomb, where similar fossils are found, and Trimucleus Bucklandi is specially abundant, and well preserved. Chetrurus juvenis also occurred here. On the north side of the complex synclinal, calcareous beds are seen by the platform on the south side of Clarbeston-Road Station, where Trinucleus Bucklandi is found in plenty with :— Phacops Brongniarti, Por?d. Lepteena tenuicincta, M‘Coy. Homalonotus ? A482 J. E. MARR AND T. ROBERTS ON THE On the north platform, the Dicranograptus-shales are seen, dipping as though to pass under the calcareous beds, and a small thickness of these occurs on the south side, just at the east end of the platform. Although the two series are there seen in apposition, a small fault must occur along the line of strike, cutting out the greater part of the calcareous beds; for the summit of the graptolite-shales (the Orthis-argentea zone), the Robeston Wathen limestone, and the lower part of the Sholeshook limestone stage are absent. (6) Redhill Beds—We have named these beds after the farm of Redhill, two miles north of Haverfordwest, where a quarry by the roadside shows a good section of the beds, which are also fairly fossiliferous here. (As a general rule, fossils are somewhat scarce in them.) They consist of blue-grey shales, weathering olive-green. In all cases where the Sholeshook limestone is seen, it is found to pass gradually up into these beds by disappearance of the calcareous material. We have obtained fossils from the Redhill beds, at Redhill, Pelcomb Bridge. and Wolfsdale Well, on the west side of the Western Cleddau; and at Prendergast Mill, Crundale, and Robeston Wathen, on the east side of that river. The list here given shows the principal fossils obtained from these localities :— | : lo lo a / oO cs | — - iS Ss js ct | Bee Seds|sal s [es Balsaeelee| 2 Se Pomme eS ae —————— Eee SCLERLOLESFIADE taciece eee: a eter espeu oes acca nce orleans [eevee bee A ese oe SEC MOP OLEL ISD yp Or acne wdias nee ens Saxe tp econ: thal en dene Bese [izence lees | * Crim Gis crIMscOiS esr: Bel see eRe a ieee ee 1s cal gael * Phacops mucronatus, Brongn., VaT..........0: * | | ) CLUTEPONIS! SSQUL MEY C2 at ieee cara teens ae one x | | / Broneuiarth, POT, . 15.0c.-an.cstaose=osenest ee | # |eeeeee * | x | x Calyaneme Wap t J3) 232) dares wae se ee Fe eae Soceccee he aoorlas a| eee oe ease teens * transverna VE ori. Ue 262 oases. eee a auesla: | ee * Holopeasonemmua; MW" Cay (i... ecs520-<2-b 22-0 * Plenrolomiatia, Space. ssceeaecesteee coca eles % ‘Bellerophon spp 47 oss os haces ee ae | eee eee ee Ececuliomphalus Bucklandi, Portl................|...0+ | sae * | (Orthoceras eraciles Poril. s.— oc..2..25.8-f-aes ee * OYECOECTAS; BPs co 2s4-3 2 resiemec aus eaaaee sccempeten ee x | The large tract of country west of the Western Cleddau occupied by these Redhill beds, is due to frequent repetition by folds, and the LOWER PALHOZOIC ROCKS OF HAVERFORDWEST. 483 same has taken place, but to a less extent, on the east side of the river. (c) Slade beds.—These succeed the Redhill stage at Lower Slade, immediately north of Haverfordwest, on the west side of the Western Cleddau. They are seen by the roadside, and also in a cutting near the mill. From the latter place, we have examined a number of fossils presented to the Woodwardian Museum by Dr. Hicks. To the south they are faulted against Lower Llandovery beds, the fault being seen in section in the road-cutting. The beds consist of gritty green shales, with weathered calcareous bands, very: similar in lithological character to the well-known Lower Llandovery beds of this district, but the fossils are to a considerable extent different. Trinucleus seticornis is fairly common, and has never been found in the Lower Llandovery beds of this area. Many calcareous bands of this stage are crowded with Phyllopora Hisingert, M‘Coy. Among the fossils at Slade are :— Stenopora, sp. Glauconome disticha, Goldf. Glyptocrinus basalis, M‘Coy. Tentaculites anglicus, Salt. Calymene Blumenbachii, Brongn. Phacops Brongniarti, Pordl. Iilznus Murchisoni, Salt. ? Bowmanni, Salt. Homalonotus bisuleatus, Salt. Trinucleus seticornis, His. Lingula. Strophomena rhomboidalis, Wilek. ? corrugatella, Dav. Leptzna sericea, Sow. Orthis biforata, Schloth. elegantula, Dalm. testudinaria, Dalm. On the east side of the Western Cleddau, these Slade beds occur in a lane north of Crundale, dipping away from the Redhill beds of that locality, which appear to pass under them. They are there very fossiliferous, and have yielded Trinucleus setivornis along with :— Petraia, sp. Tentaculites anglicus, Salt. Phyllopora Hisingeri, M‘Coy. | Calymene trinucleina, Linnrs.? _ Orthis testudinaria, Dalm. Bellerophon bilobatus, Sow. These beds are very extensively exposed in this region, being found also in the railway-cuttings at Little Hareshead and Clover Hill, and in a small quarry at Dallaston. At Robeston Wathen they occur above the blue-grey shales of the Redhill stage ; and on the other side of the Robeston Wathen synclinal, are seen at Benlomond Cottage, where Prof. Phillips found Zrinucleus ornatus, var. Caractact (Mem. Geol. Survey, vol. ii. p. 240). Fossils from the north side of the Robeston Wathen synclinal are:— Climacograptus. Petraia. Tentaculites anglicus, Saiz. Ptilodictya costellata, M/‘Coy. Calymene trinucleina, Tinwrs.? Trinucleus seticornis, His. Cheirurus, sp. From Benlomond Cottage :— Tentaculites anglicus, Saiz. Lichas. Orthis calligramma, Dalim. Phacops Brongniarti, Pordi. Tllzenus. Orthis porcata, M‘ Coy ? Leptzena sericea, Sow. Strophomena. Bellerophon bilobatus, Sow. Orthis testudinaria, Dali. Lepteena sericea, Sow. 484 J. E. MARR AND T. ROBERTS ON THE North of Stoneyford, the beds of this stage are also seen in the southern limb of a small synclinal, the lower beds of which are apparently absent, owing to a slight dislocation. , To the east of this, the same beds are found occupying the more central part of the synclinal north of Llandewi Velfry. — 7. Conglomerate Series.—Near the centre of the complex syn- clinal, and in the centres of the minor synclinals of Robeston Wathen, Penblewin, and to the north of Llandewi Velfry, a coarse conglomerate is found with pebbles of vein quartz, and other materials of distant origin, succeeded by a coarse quartzose grit. To the west, this grit appears to be first met with in the railway- cutting south of Sholeshook, where it is faulted in against older beds on the north. To the east of this, it is seen near Mary- borough, dipping north at a low angle. From here it runs eastward along a ridge to Wiston Wood. In a quarry south-west of Valley Farm, green-banded mudstones, with beds of quartz-grit, possibly belonging to this series, are found. On the north side of the quarry they dip at a very low angle to the north, whilst on the south side they are vertical. This appears to be due to a sudden bend rather than to a fault. To the west of Wiston Wood, the conglomerate is exposed in a quarry in a field. It is here nearly vertical, but dips slightly north, and, according to the strike, would pass beneath the beds of the last-mentioned quarry. Another ridge of grit runs to the north of this one, also in a general east and west direction. It is seen faulted against Trinu- cleus-seticornis shales, in the railway-cutting, west of Wiston Mill. Proceeding in an easterly direction, we again find it exposed on the ridge 4 mile 8. of “o” in “ Dallaston ;” it is here much disturbed. It appears to be continued along this ridge to Wiston. In a quarry south of Church Hill, near this village, a very coarse grit is found, dipping south. Wherever exposed, the grit of this ridge appears to overlie or be faulted against beds of the Slade stage. A third grit-ridge runs parallel to these, and to the south of them. Grit is found, apparently overlying green shales, in a road- cutting west of Slebech New Church. In a quarry south of Clerken Hill, east of the last place, conglomerate is exposed, dipping north. At Robeston Wathen the conglomerate is many feet thick, and occupies the centre of the synclinal shown in fig. 3. In each limb of the synclinal it rests upon the representatives of the Slade beds, containing 7’rinucleus. A patch of grit is seen in a quarry south of “ Camp,” 13 mile north-east of Robeston Wathen. The relations of this to the sur- rounding beds are somewhat obscure, as the tract of country between the limestones of Robeston Wathen and Grondre is, as already stated, much broken. Another ridge runs from near Penblewin eastward. Here the conglomerate is found in a quarry west of Carmine, dipping north at an angle of 20° and succeeded by coarse grit. It rests upon the representatives of the Slade beds which occur at the cross roads at Penbelwin. LOWER PALZOZOIC ROCKS OF HAVERFORDWEST. 485 ' The last appearance of the conglomerate eastward, in the area we have examined, is in a quarry west of Wheelabout, where it is succeeded by sandstone, the beds dipping N.W. It occurs at this place also above beds of the Slade stage, which are well seen at the “k” of ‘ Bank Saison” dipping west. From the numerous exposures of the beds of this series, where they immediately succeed the Slade beds, there seems little doubt that this is the true position of the conglomerate; and as we have found no evidence of its resting upon any beds lower in the series, it would seem that there is no very great physical discordance at the base of the conglomerate-band, which nevertheless may mark an important physical change in the area. We have unfortunately been unable to find any exposures showing the conglomerate succeeded, without suspicion of faulting, by still higher beds, :as it occurs in most cases on the summits of ridges, and the higher strata have been removed by denudation. In one instance, however, the grit is found between the Bala and the fossiliferous Lower Llandovery beds. This is in a section, pre- viously alluded to, on the railway between Haverfordwest station and Sholeshook, ‘The diagram section (fig. 5) shows the actual exposures, and the fault and folds which we consider necessary to explain the apparent sequence. Between the Sholeshook limestone and the grit only one isolated exposure is seen, in a lane east of the railway, having beds lithologically like those of the Slade stage, and containing fossils which are too imperfect for determination. The beds between the grit and the station are also somewhat un- fossiliferous, and though the fossils found, including Phacops mu- cronatus, Ang. (the form which occurs in the Upper Brachiopod beds of Sweden, and not the variety of the Sholeshook and Redhill beds), seem to indicate the Lower Llandovery age of the beds, the deter- mination is doubtiul. We can, however, draw no line between these beds and the very fossiliferous beds of the Gas-works, of true Lower Llandovery age. Another point to be noticed is the absence of the conglomerate, which, however, occurs in connexion with the grit, further east, as_ . above described. Its absence appears to point to the existence of a ~ fault, as well as the inversion represented in the diagram. The relationship of the conglomerate series to the Lower Llandovery further east is obscure, owing to the paucity of sections. From the nature of the ground, we should expect this series to pass con- tinuously round from Wiston to Slebech, thus lying between the Lower Llandovery and the Bala beds which occur further east. What scanty evidence we have, therefore, certainly points to the conglomerate series being immediately succeeded by the fossiliferous Lower Llandovery beds, and this conclusion is supported by the paleontological evidence; for the fauna of the Slade beds, though differing from that of the Lower Llandovery beds, has several forms in common. Moreover, the accumulation of the conglomerate series shows only a slight pause in a period during which beds of similar litho- Q.J.G.8. No. 163. Ot 486 J. E. MARE AND T. ROBERTS ON THE logical character were being laid down, as the Lower Llandovery beds closely resemble the Slade beds lithologically. 8. Lower Llandovery Beds.—These beds are, as explained above, apparently faulted against the lower beds in the immediate neigh- bourhood of Haverfordwest. They are usually very highly inclined, and stretch to the south of the town for nearly two miles. The well-known section at the Gas-works shows the general character of the rocks, which consist of gritty green shales, with bands of grit, and weathered calcareous bands crowded with fossils. As the organisms of this deposit are preserved in many museums, it is un- necessary to give a full list. Nidulites favus, Petraia subduplicata var. crenulata, Tentaculites anglicus, and brachiopods, lamellibranchs, and gasteropods are all abundant. Amongst the fossils hitherto unrecorded from these beds are Phacops elegans, Boeck and Sars (=elliptefrons, Esm.), and Deiphon Forbesi, Barr. A fine specimen of the latter was presented to the Woodwardian Museum by Mr. H. T. Wills. § 3. Comparison with the Deposits of other Areas. The resemblance of many of our stages to those of other areas, whether we take into account their lithological or paleontological characters, is so striking, that it cannot be a mere coincidence, especially as this resemblance does not occur in isolated stages, but in the consecutive stages of some of the series. We propose, there- fore, to point out briefly some of these similarities, as they afford assistance in attempting the correlation of deposits of different areas. . i. Lingula-Flags——These beds appear, from the occurrence of Olenus spinulosus, to represent the Lower Dolgelly beds of the Lingula-Flags of North Wales, which are correlated by Prof. Brégger (Sil. Et. 2 and 3, p. 144) with his “Parabolina-spinulosa niveau ” (25) in the Christiania district, where that fossil is likewise associated with Agnostus socials. It is desirable, however, that additional species should be obtained ; for whilst the fossils already procured leave no doubt as to the Lingula-Flag age of the rocks containing them, it is perhaps dangerous to attempt to assert positively to what portion of the Lingula-Flag series they belong, without further evidence. . ii. Didymograptus-Shales.—The “tuning-fork” graptolites of these beds are characteristic of Dr. Hicks’s Llanvirn beds in the St.- David’s district, as elsewhere. As the horizon is so well known in many places, and contains this-particular type of graptolite, it is needless to give a list of deposits of the same age in other areas. ili. Llandeilo Limestone.—The remark just made applies in this case also. The position of the Asaphus-tyrannus beds is well estab- lished in South Wales. At the same time it is possible that the beds included in the Llandeilo limestone of other regions are partly represented by the lower beds of the succeeding division of the Haverfordwest district ; for whereas Ogygia Buchit has not been discovered by us in the limestone, and is apparently not recorded LOWER PALAOZOIC ROCKS OF HAVERFORDWEST. 487 from the limestone of this region, it does occur in the graptolite- shales of the succeeding group. iv. Dicranograptus-Shales.—It has already been stated that several zones must be represented among these beds, and that we have been unable to work these out in the field, owing to the absence of exposures continuous throughout the series. That the beds do represent generally the Glenkiln and lower portions of the Hartfell groups of Scotland appears probable: but as we have sub- mitted a large collection of specimens from this horizon to Professor Lapworth, we leave the fuller determination of the age of the group to him. The uppermost bands, which are crowded with Orthis argentea, may be compared with the Orthis-argentea zone of Dr. Linnarsson in Sweden (cf. Lapworth, Geol. Mag. dec. ii. vol. vii. p. 48). v. Robeston- Wathen Limestone.—The fossils of this limestone are , certainly of Middle Bala facies; but trilobites are rare, and the organisms are chiefly corals. The identification of this bed with parts, at any rate, of the Bala and Coniston limestones receives strong support from the evidence furnished by the succeeding deposits. vi. Trinucleus-seticornis Beds. (a) Sholeshook Limestone Stage.——This is comparable both litho-— logically and paleeontologically with the Rhiwlas limestone of Bala, which must certainly be of different age from the true Bala limestone. The bed is so peculiar in character, and maintains its appearance and paleontological characters so uniformly over a wide area, that it is very easy to identify, and forms therefore a very important horizon for purposes of comparison. The Rhiwlas cystideans are similar to those of Sholeshook, and the trilobites are mostly of the same species. Staurocephalus is present at Rhiwlas as in Pembroke- shire, and associated with it are the following fossils of the Sholes- hook stage :— Ampyx tumidus, Forbes. Trinucleus seticornis, His. Cheirurus juvenis, Sal. Lepteena tenuicincta, M‘Coy. bimucronatus, Murch, Cyrtoceras sonax, Salt. It may be observed that, as Professor Sedgwick made his Upper Bala series to include the beds above the Bala limestone, this stage must be taken as the base of that series, and it forms, as observed, a readily recognized base. In the Lake-district a bed of quite similar lithological cha- racter occurs immediately above the Coniston Limestone. Its fauna has not yet been fully described, but one of us has elsewhere noticed it (‘Sedgwick Essay,’ 1882, p. 58). Stauwrocephalus is there associated with the same cystideans as at Sholeshook, and a large number of trilobites are common to the two deposits, and do not occur in the underlying Coniston limestone. The starfish-bed of Prof. Lapworth (Q. J. G. S. vol. xxxviii. p. 619) may possibly be the representative of this in the Girvan area; it also contains Stawrocephalus globiceps. In Ireland the same group of fossils appears to occur at Desert- 242 488 J. E. MARR AND T. ROBERTS ON THE creat, Tyrone, judging from an examination of the specimens pre- served in the Museum of Practical Geology. Amongst the fossils common to Sholeshook and Desertcreat are :— Phacops Brongniarti, Portl. TUenus Bowmanni, Sait. Staurocephalus globiceps, Por7l. Stygina latifrons, Portl. Remopleurides dorso-spinifer, Pordd. Trinucleus seticornis, Hs. The absence of cystideans at Desertcreat is noticeable. A large number of fossils are recorded from this Irish locality, which seem to show that the representatives of the Redhill stage occur there also. In Sweden the same fauna appears at the same horizon in beds of precisely similar lithological character. Immediately above the beds correlated with the Middle Bala series, in Westrogothia, Dr. Linnarsson’s Stawrocephalus-beds (at the base of the Brachiopod- schists) contain Staurocephalus clavifrons, Ang., Proetus brevifrons, Phacops mucronatus, Calymene tuberculata, Acidaspis centrina, Trinucleus Wahlenbergi, Agnostus trinodus, Phillipsia parabola, and Panderia megalophthalma (Linnarsson, ‘Om Vestergétlands Cambriska och Siluriska Aflagringar,’ p. 51). In Scania also the same bed occurs. Dr. Tullberg (‘ Skanes Grap- toliter,’ i. p. 17) records in his zone with Staurocephalus clavifrons :— Staurocephalus clavifrons, Ang. Ampyx tetragonus, Ang. Phacops mucronata, Ang. Phillipsia parabola, Barr. Trinucleus Wahlenbergi, Rouwauit. Acidaspis, sp. Tllznus, ef. Salteri, Barr. Calymene Blumenbachii, Brongn., var. Proetus brevifrons, Ang. Agnostus trinodus, Saiz. Cheirurus, sp. Dentalium, sp. Turbo, sp. From the general occurrence in this zone of Staurocephalus globi- ceps, or a closely allied species, it may be conveniently spoken of as the Staurocephalus-zone. (6) Redhill Stage.—This stage is lithologically like the Ashgill shales of the Lake-district, which also immediately overlie the Staurocephalus-zone. In Scotland the “soft blue mudstones, homogeneous, thick-bedded, and more or less coneretionary in structure,” described by Prof. Lapworth as occurring above the Starfish-bed of Lady Burn, in the Girvan area, seem to be likewise similar (Q. J. G. S. xxxviil. p. 619). In Scandinavia the beds with Phacops eucentra, Ang. (a variety of P. mucronatus ?), which immediately succeed the Stauwrocephalus- zone in Scania and Westrogothia, have elsewhere (Q. J. G. S. xxxviii. p- 321) been compared by one of us with the Ashgill Shales of Britain. (c) Slade Beds.—These are not precisely like any beds known to us as occurring about the same horizon in other areas. In the Lake-district a mottled grey limestone with many brachiopods occurs immediately above the Ashgill Shales and below the Birkhill beds in Skelgill Beck. Like the Slade beds, it is marked by the occurrence of Climacograptus and the absence of Monograptus. LOWER PALZOZOIC ROCKS OF HAVERFORDWEST. 489 In Scania, Dr. Tullberg (‘Skanes Graptoliter,’ i. p. 17) finds above his zone with Phacops mucronatus (P. eucentra) a zone with _Diplograptus and Climacograptus scalaris, and marked by an absence of Monograptus. This zone he places at the top of the Upper Cambrian (Sedgwick), and not at the base of the Silurian, where Prof. Lapworth describes a zone marked by the absence of Mono- graptus, viz. at the base of the Birkhill beds (cf. Lapworth, Q. J. G. 8. vol. xxxiv. p. 318). In Westrogothia the gritty beds with 7rinucleus at Mosseberg may represent our Slade beds. vu. Lhe Conglomerate.—As stated, when describing the apparent position of these beds, they appear to succeed everywhere the Slade beds. If this be their true position, they form a satisfactory base to the Silurian rocks of this area. We may compare them with the Mullock-Hill conglomerate of Prof. Lapworth (Q. J. G. 8. vol. xxxviii. p. 621), which lies in the Girvan district directly above the Trinucleus-shales, just as the con- glomerate in the district now described lies above our Trinucleus- shales. vili. Lower Llandovery Beds.—We have applied this term to the shelly sandstones immediately south of Haverfordwest town, as they have been constantly spoken of as Lower Llandovery. If they do actually succeed the Conglomerate stage, the latter should also be included in the Lower Llandovery series. These shelly sandstones are lithologically and paleontologically similar to two well-known deposits, viz. the Mullock-Hill Sand- stones of the Girvan district, and stage 53 in the neighbourhood of Christiania. All these contain Miduhtes along with Stricklandinia and a host of other brachiopods. A comparison of the published lists will show the practical identity of the faunas (cf. Catalogues of Paleozoic Fossils in the Woodwardian Museum, and that of Practical Geology, also Kjerulf’s ‘ Veiviser ’). The upper part of the Brachiopod-beds of Westrogothia has. similar fauna, and is placed on this horizon by the Scandinavian geologists. One of us has in a previous communication (Q. J. G. 8. vol. XXXvill. p. 316) discussed the age of the Leptena-limestone of Mr. Tornquist, which occurs in Dalecarlia, and has referred it to a posi- tion above the Lobiferus- and Retiolites-shales of that region. This was certainly a mistake, due to ignorance of the phenomena pre- sented by a greatly disturbed region at the time of examination. Dr. Fr. Schmidt has shown (Q. J. G.S. vol. xxxviii. p. 523) that the fauna of the stage F of the Kast Baltic provinces is that of the Leptcena-limestone of Osmundsberg. The Leptena-limestone contains a mixture of faunas of several of the Haverfordwest beds, viz. :—the Lower Llandovery, 77rinucleus- seticornis beds, and perhaps even of the Robeston-Wathen limestone, the corals of which also occur in the Leptena-limestone. 490 J. E. MARR AND T. ROBERTS ON THE § 4. Conclusion. We have endeavoured, in this paper, to establish the succession. in the district under consideration. That certain difficulties are not yet cleared up is admitted. Our inability to discover any section showing normal Sholeshook limestone resting upon normal Robeston- Wathen limestone is unfortunate. In separating these stages from each other, we are influenced by the lithological and paleontological differences between the two deposits, and by comparison with similar beds in other areas. But for this, we should be disposed to look upon the Robeston-Wathen limestone as a local development of the Sholeshook limestone. We may note, however, that there are many places in the district where one or more of the limestones can be satisfactorily proved to have been crushed out. As already explained, also, the relation of the conglomerate to the succeeding beds requires further study. These minor difficulties have been encountered when studying portions of the sequence which are typically developed elsewhere. As they do not greatly affect our establishment of the sequence in this area, and as other difficulties would probably arise upon further exploration, the announcement of our results might be indefinitely postponed, and we therefore venture to bring our work before the Society, in the belief that what we have done will prove sufficient to furnish a clue to the solution of a very interesting question, viz. the nature of the foldings which have affected the district. EXPLANATION OF PLATE XV. Fig. 1. Geological Sketch-Map of the neighbourhood of Haverfordwest. The map, based on that of the Geological Survey, is simply intended as a sketch-map, showing the general distribution of the beds; and the boundaries in many places are only approximately correct. The Redhill beds and Slade beds have been represented by the same sign, as we have not traced the boundary between them over the whole district. The Dicranograptus-shales of Grondre and Longford. may extend further east than represented. 2. Section in Quarry south-east of Trefgarn Bridge. 3. Section through Robeston Wathen. 4, Section in the Lane north of Prendergast Church. 5. Diagram-section along the Railway from Haverfordwest Station to north of Crundale. Discussion. The Prestpent expressed his pleasure at seemg that such ad- mirable work had been done by Cambridge geologists. Dr. Hicxs stated that the Authors had entirely confirmed his. views that the rocks of Roch Castle and Trefgarn which he had referred to the Archean were not, as believed by the Geological Survey, intrusive rocks penetrating Lower-Silurian strata. The recognition of the important fact that these are of Pre-Cambrian age was absolutely necessary before the geology of the area could LOWER PALZOZOIC ROCKS OF HAVERFORDWEST. 491 possibly be interpreted. The succession of the rocks in this district had never been unravelled till the Authors undertook the task. Prof. Hugues remarked on the absence of the evidence of the occurrence of the Harlech Grits except the basement-bed, of the Menevian, the Tremadoes, part of the Arenigs, and other forma- tions. He thought the Hirnant limestone really consists of two members which are separated by a great break, and the lower of these only is represented by a limestone in the area described. He thought it probable that the equivalents of the Upper Conglo- merates might be found in the Malvern district, and that they form the base of the Silurian. Mr. Marr thought that the beds in Trefgarn-Bridge Quarry exhibit signs of faulting, which may account for the apparent absence of some of the strata. He thought that a great confusion had arisen as to the position of the conglomerates at the base of the Silurian. 492 REV. A. IRVING ON A GENERAL SECTION OF THE 36. GENERAL Section of the Baesnor Srrata from ALDERSHOT to Woxrnenam. By the Rev. A. Irvine, B.Sc., B.A., F.GS. (Read April 15, 1885.) A RESIDENCE of some years in the Bagshot district of the London Basin has afforded me opportunities for many observations on the Bagshot strata which have escaped the notice of previous writers on the subject. Some of these have been already recorded *. Two or three years ago I was led to investigate the origin of the green colouring-matter so prevalent in the Middle and Lower Bagshot strata, and an account of the results arrived at was given in the ‘ Geological Magazine’ tT, the bearing of the facts upon the question of water-supply being shown to be of some economic importance. More recently I have given some results obtained by a further prosecution of the same line of inquiry, and have stated that they have led me to regard the Middle and Lower Bagshot strata as, upon the whole, a series of delta-, marsh-, and lagoon- deposits, such as are now forming in the alluvial flats ‘at the mouth of many a large river, but those of the Upper Bagshot as the deposits of a marine estuary, which covered up and overlapped the Middle and Lower series, so as to have extended over parts of the London Clay. This inference from chemical and physical evidence is at variance with the generally received view as to the physical history of these strata, the first eminent worker on these beds having declared that they were conformable to the London Clay §, and the Geological Survey having mapped the district in accordance with such a supposition. The main object of this paper is to bring before the Society stratigraphical evidence on this question. It must be understood that I make no attempt here to correlate the strata of our Bagshot district in detail with the corresponding strata of the Hampshire Basin: I use the terms ‘ Upper,’ ‘ Middle,’ and ‘ Lower, therefore, as applied to the Bagshot strata, in them natural sense, to mean the well-marked upper, middle, and lower divisions of the latest Eocene formation of the district to which it owes its name, regarding this as a distinct area of deposition in Bagshot times. In the classification of the Bagshot beds I have included the bed of loamy sand (No. 4, figs. 1 & 2), which occurs so generally imme- diately above the green ‘sands and clays, in the Middle Division (as was done by the Survey); the pebble-bed, however, which commonly See Proceedings of the Geologists’ Association, vol. viii. pp. 143-173. See Geol. Mag. dec. ii. vol. x. pp. 404413. Iéid. dec. iii. yol. ii. See Prestwich, Quart. Journ. Geol. Soe. vol. iii. Dati BAGSHOT STRATA FROM ALDERSHOT TO WOKINGHAM, 493 occurs next above it, appears to have been overlooked by the Surveyors, though it crops out in many places. There is some indi- cation of considerable contemporaneous erosion in some sections where the pebble-bed rests upon this loamy bed; and in the bed itself thin seams of pipe-clay generally occur. On this last point, it would seem, my observations differ from those of the Surveyors *. Grains of quartz coated with black and green amorphous matter of vegetable origin are scattered freely in this bed: they are especially numerous in juxtaposition with the pipe-clay layers. Dertainep SECTIONS. As these are rather numerous, and are spread over a rather large area, extending about 13 miles from north to south, it will tend to simplify matters if we consider these sections in two series :—a. Deep- well sections, giving the whole range of the Bagshot Sands, and in some cases the London Clay as well; 6. Sections in which only por- tions of the Bagshot Sands are exposed. We shall find the general character of the three divisions of the Bagshot strata sufficiently determined by the evidence afforded by the former series to aid us considerably in determining the stratigraphical horizons of the sections of the latter series. a. Drrp-WELL SECTIONS. (1) Well-section at Wellington College—The specimens and measurements of the strata pierced in digging this well were pre- served with great care. The sectional diagram (fig. 1) has been reprinted (with additional notes), with the courteous permission of the President and Council of the Geologists’ Association, from vol. vi. of the ‘ Proceedings ’ of that Society. The grouping of the strata agrees substantially with that adopted by Prof. Prestwich many years ago’. A few supplementary notes, for which there is not sufficient space on the margin of the diagram, may be useful. No. 2. This isa quartzose sand, stained with carbonaceous matter on the grains, with scarcely a trace of iron. The occurrence of this bed of dirty sand here is exceptiunal; this horizon is generally occupied by a bed of stiff yellow loam, almost a clay, which passes up into the yellow sands. No. 5. This bed was worked for about twenty years in the neigh- bouring brick-field, and Wellington College was built with bricks for which it afforded the sole material. * See Memoirs of the Geological Survey, vol. iv. pp. 329, 330, where the bed is described as ‘‘a bed of ferruginous sand without pipe-clay.” The general outlines of Bagshot stratigraphy are given so fully in that work as to require no further description here. It has been generally assumed, but, I think, never proved, that this area of deposition was continuous with that of Hampshire through Bagshot times. Tt Quart. Journ. Geol. Soe. vol. iii. Joc. cit. As before intimated, however, I draw the upper boundary of the Middle Bagshots at a rather higher horizon. 494 REV. A. IRVING ON A GENERAL SECTION OF THE Fig. 1.— Vertical Section of Bagshot Strata disclose din the Trial- boring for the Deep Well at Wellington College. (Scale 40 feet =1 inch.) UppErR BAaGsHOT | (23 feet). -csccese-n- { MIDDLE BAGSHOT (76 feet)..........+. ( | | | | 230 feet. ~~ oo Vertical height of section LOWER:BAGSHOT (about 120 feet) 4 LonDON CLAY...-». aD (i CHE 285 feet above Ordnance datum-line. Surface-drift enclosing angular fiints (1 foot). Buff-coloured sand (Upper Bagshot) (12 feet). Grey sand with dark olive-green and black grains (10 feet) (rather exceptional at this horizon). Well-worn pebbles of black flint in sand (1 foot). Buff-coloured sand and loam (6 feet) (scattered green and black grains and pipe-clay). Drab-coloured: sandy clay (9 feet), in some sections laminated. Well-rolled pebbles of black flint in sand (3 feet). piers sand, yielding some water at the. bottom ‘31 eet). Sand*of a dark green tint (7 feet). Much water. ~ Fine clay, in part a pure pipe-clay (6 feet). Continuation of the next above but of darker shade (14 feet). Sand (grey),'with olive-green grains (46 feet). Thisis = simply a dirty quartzose sand. Continuation of the above, with rather more oxidized _ iron on the grains (46 feet). Indurated arenaceous%clay stained with carbon (3 feet). Blackened marl and clay laminated in its upper portion (35 feet). NotE.—To the 23 feet of Upper Bagshot Sands, shown in this section, we must add another 100 feet and more for the total thickness of these sands as they exist at present elsewhere in the district. The neigh- bouring hills, on which the Criminal Lunatic Asylum is situated, reach a height of 400 feet, and the continu- ation of the beds of the upper portion of this section beneath those hills is proved in numerous well-sections in the village of Crowthorne. We must have, there- fore, a thickness of about 140 feet of Upper Bagshot Sands preserved in this neighbourhood. BAGSHOT STRATA FROM ALDERSHOT TO WOKINGHAM. 495 No. 6. The rapid thinning-out of this pebble-bed was proved two years ago in an excavation made for a rain-water tank for the College Laundry. It was only 13 feet thick there. In the neigh- bouring railway-cutting it has dwindled to a mere layer of pebbles. No. 8. Small fragments of shells occur in this bed, which occupies the same horizon as that in which very complete specimens of Cardita &e. were found last year, in the well at Yateley Green, described below. No. 9. The uppermost 6 inches of this bed show the green sand of the bed above, coarsely mingled with the clay ; the next three feet consist of pure pipe-clay. Then, for about three feet, the clay is distinctly laminated and coloured with carbonaceous matter. No. 10. This is a very homogeneous clay-bed, much stained with carbonaceous matter. No. 12. This bed is slightly more loamy than No. 11. The speci- mens preserved have assumed a somewhat browner tint, as the result of oxidation during the last 25 years, from the presence of more iron in the material which coats the grains. The specimens of these two beds (11 & 12) have precisely the character assumed by the grey and greenish sands after long exposure to atmospheric oxygen. No. 13. The clay of this bed is exactly like that of No. 10. No. 14. The uppermost 25 feet of this bed are strongly lami- nated ; the remaining 10 feet pierced have more the character of London Clay than of anything else. Here, then, we seem to find a passage of the London Clay into the Bagshot Sands. (2) Farnborough Deep Well.—At the southern end of the parish, a new well was sunk last year by Messrs. Tilly and Sons for the District Waterworks. From the information furnished to me, and from inspection of the works, I have constructed the following section. The elevation of the mouth of the well above O.D. level is 250 feet. ft. in. 1. Gravel (mixture of pebbles and suban- eWiar Hints) of later drift... .scnc.-+sce-+ 2 0 ZoellowslOatay SANG .sc...csccecuaen~- ed saneee 33 0 3. Yellow sand, yielding water ............... 33 0 i ARIAL OW; MOAT juiced cclmsle s comtesimmcce castes Si Onn Ube segs, La { BetGirey loam) conlscs... ae a Found also in the Weka-pass stone, at Aotea, Raglan, and on the coast south of Port Waikato. This may be the P. gemmulatus, Reeve, mentioned by Mr. M‘Kay. Dae CAPT, F. W. HUTTON ON THE CORRELATIONS OF THE *PECTEN CHATHAMENSIS, Hutton, Cat. Tertiary Moll. of N. Z. p. 29. Reported by Mr. M‘Kay. Found also on the east coast of Wel- lington, in Pareora rocks; and according to Mr. McKay, in the Upper Eocene and Cretaceo-Tertiary rocks of the Trelissic Basin. *Proren Hocusrerrerr, Zittel, Reise der ‘ Novara, Geol. ii. p. 50, pl. xi oa: Found also in the Weka-pass stone; in the Ototara stone; at Caversham; Point Elizabeth; Aotea; Raglan, and coast to the north. Also in the Pareora system at Waikari and Motanau. *Proren Hurcuinsoni, Hutton, Cat. Tertiary Moll. of N. Z. p. 31. Found also in the Weka-pass stone; at Kakanui, and in several places in rocks belonging to the Oamaru system. Also, according to Mr. M°Kay, in the Upper Eocene and Cretaceo-Tertiary rocks in the Trelissic Basin. *Lima Lavieata, Hutton, op. ct. p. 33. Reported by Mr. M°Kay. Found also in the Cobden limestone ; | at Waihola gorge in Otago; at the Heathstock-Road Quarry in the Weka-pass stone ; and in the Mount-Somers building-stone. Lima paucisutcata, Hutton, op. ct. p. 33. Reported by Mr. M°Kay. Found also at Cape Farewell. Lima PALEATA, op. cit. p. 33. Found also in the Ototara stone, and the Mount-Somers building- stone. LIMA MULTIRADIATA, op. cit. p. 33. Probably a variety of the last. Not known elsewhere. Lima crassa (?), Hutton, op. cit. p. 33. Reported doubtfully by Mr. M°Kay. This species is perhaps the same as the recent L. neozelandica, Sow. (P.Z.8. 1876, p. 754). It is found in several localities in the Pareora system. BRACHIOPODA. THREBRATULA ALDINGZ, Tate, Trans. Phil. Soc. of Adelaide, 1880, P20; plecx- ta. Not known from any other locality in New Zealand. * *WALDHEIMIA LENTICULARIS, Deshayes, Mag. Zool. 1841, t. 41. A living species extending through the Wanganui, Pareora, and Oamuru systems. Found also in the Weka-pass stone, and in the Waihao limestone. *W sLDHEIMIA TRIANGULARIS, Hutton, Cat. Tertiary Moll. of N. Z. p. 36. Reported by Mr. M°Kay. Found also in the Weka-pass stone, and in various places in the Oamaru and Pareora systems. ‘“¢ CURIOSITY-SHOP BED ” IN CANTERBURY, NEW ZEALAND. 95953 *WALDHEIMIA pATagonica, Sow. in Darwin’s Geol. Obs. in S. America, p. 252. Found also in the Cobden limestone, and in various places in the Oamaru and Pareora systems. *?TEREBRATELLA SINUATA, Hutton, Cat. Tertiary Moll. of N. Z. p. 36. Found also in the lower beds in the Trelissic Basin, and the Upper Eocene beds at Oamaru. *TEREBRATELLA GAvULTERI, Morris, Quart. Journ. Geol. Soc. 1850, vi. p. 329. Found also in the Ototara stone, and at Raglan. *TEREBRATELLA Surssi, Hutton, Cat. Tertiary Moll. of N. Z. p. 37. Terebratella, sp., Siiss, Reise der ‘ Novara,’ Geol. ii. p. 57, taf. ix. £6: Found also in the Cretaceo-Tertiary rocks of the Trelissic Basin (McKay). TEREBRATELLA FURCULIFERA (?), Tate, Trans. Phil. Soc. of Adelaide, 1880, p. 22, pl. xi. f. 7. Not known elsewhere in New Zealand. RayYNcHONELLA NieRICANS, Sow. Thes. Conch. i. p. 342. A still living species extending through the Wanganui, Pareora, and Oamaru systems. *RHYNCHONELLA squamosaA, Hutton, Cat. Tertiary Moll. of N. Z. PeOt; Late, ts ex plavix. f. Os R. nigricans, var. pyxidata, Davidson, Voyage of the ‘ Challenger,’ Zool. i. p. 59. A living species found also in the Cretaceo-Tertiary rocks of the Trelissic Basin (M‘Kay). HicHINODERMATA. PENTACRINUS STELLATUS, Hutton, Cat. Tertiary Moll. & Hchin. of N..4..1873, p.'38. Found also at the Chatham Islands. *CIDARIS sTRIATA, Hutton, l. ¢. p. 38. Found also at Brighton on the west coast. *Kcuinvs Enysr1, Hutton, l. ¢. p. 39. Also found, according to Mr. McKay, in the Upper Eocene and Cretaceo-Tertiary rocks of Trelissic Basin. Loventa Formosa, Zittel, Reise der ‘ Novara,’ Geol. ii. p. 63, pl. xii. bade: hy Also found in several localities in Upper Eocene rocks. Probably not specifically distinct from L. tuberculata and L. Forbesiv. 554 CAPT. F. W. HUTTON ON THE CORRELATIONS OF THE Hemtaster (?) posrrus, Hutton, l.¢. p. 42. Not known from any other locality. *Mroma (?) CkawrorpD1, Hutton, J. ¢. p. 42. Also found in the Weka-pass stone; the Ototara stone; Caver- sham; Maerewhenua limestone, and many other places. Much like Megalaster compressus, Duncan (Qaart. Journ. Geol. Soc. 1877, xxxiii. p-. 61), which is the same as Pericosmus compressus of M°Coy. Meroma (?) tuBercuLata, Hutton, l. ¢. p. 43. Reported by Mr. M°Kay. Also found in the Upper Eocene beds at Trelissic Basin. Bryozoa. SELENARIA HEMIsPH@RICA, Busk, MS. (?). Woods, Geol. Obs. in 8. Australia, p. 73, pl. ‘ Fossil Bryozoa,’ f. 3. Referred with doubt, as no specimens have been compared. Our species is also found in the Upper Hocene rocks of Mount Brown. C@LENTERATA. *GRAPHULARIA (?) SENESCENS, Tate, Quart. Journ. Geol. Soc. vol. XXx1. p. 257. Found also in the limestones of Otakaika, Maerewhenua, and Waihao. Identified by Dr. Hector after comparison with 8. Aus- tralian specimens (Geol. Reports, 1881, p. xxix); he considers them, however, to be spines of Cidaris. This list contains 48 species, of which 29 or 30, including both the vertebrates, are also found in rocks regarded as Cretaceo-Ter- tiary by the Geological Survey. Also 22 species are found in the Pareora system or later, of which 14 are also found in the Creta- ceo-Tertiary series. There are 10 or 11 species not found either in the Cretaceo-Tertiary or in the Pareora. The Curiosity-Shop beds are therefore more closely related palzontologically to the Cretaceo- Tertiary than to the Pareora, while the number of peculiar species is not sufficient to make them stand separately as an Upper Hocene system. I will now, therefore, take some other localities of Cretaceo- Tertiary rocks for comparison. List or Fosstrs FRoM THE WeExkA-pPAss Stone, NortH CANTERBURY. * Species marked with an asterisk are also found in the Curiosity- Shop beds, or in acknowledged Upper Eocene rocks, or younger. VERTEBRATA. CETACEAN BONES. *PALmEUDYPTES ANTARCTICUS, Huxley. At Amuri Bluff. *CARCHARODON ANGUSTIDENS, Ag. ‘“‘ CURIOSITY-SHOP BED ” IN CANTERBURY, NEW ZEALAND. 9955 Mottvsca. ATURIA ZICZAC, var. AusTRALIS, M°Coy, Prodr. Palzont. Victoria, Decade ii. p. 21, pl. xxiv. Found also in the Kakanui limestone, and at Waihemo in the Shag Valley, Otago. *VoLUTA PACIFICA, Lamarck. Var. elongata, Swainson. *VoLUTA ATTENUATA, Hutton. V. elongata, Hutton, Cat. Tertiary Moll. of N. Z. 1873, p. 7 (not of Swainson). Found also in the Pareora system at Pareora, and, according to Mr. M°Kay, in the Cretaceo-Tertiary series at Trelissic Basin. *Cassis SENEX, Hutton. Scatarra RotunDa, Hutton, Cat. Tertiary Moll. of N. Z. 1873, p. 10. Found also at Brighton, on the West Coast, associated with bones of Paleeudyptes.antarcticus and Turtle. *Q§cALARIA LYRATA, Zittel. *PLEUROTOMARIA TERTIARIA, M°Coy, Prodr. Paleont. Vict., Decade ii p. 2, ply xxv, £1. Found also in the Ototara stone, and in the Upper Eocene lime- stone of Mt. Somers. *Prcren WILLIAMSON, Zittel. *Proren Fiscuert, Zittel, Reise der ‘ Novara,’ Geol. ii. p. 53, pl. ix. fa. Found also in the Ototara stone, and, according to Mr. M°Kay, in the Upper Eocene rocks of Trelissic Basin. *Prcren Hurcuinsoni, Hutton. Prcren Brrruami, var. 2, Hutton, Cat. Tertiary Moll. of N. Z. p. 32. Found also near Caversham, near Dunedin. *Prcren Hocustettert, Zittel. *Lima Lzvyieata, Hutton. BRACHIOPODA. — *TEREBRATULA (?) BuLBosA, Tate, Trans. Phil. Soc. of Adelaide, LS8O; p..G;, pls vant. 5. Waldheimia concentrica, Hutton, J. c. p. 35. Reported by Mr. M*Kay from the Upper Eocene and Cretaceo- Tertiary rocks of Trelissic Basin. = 556 CAPT. F, W. HUTTON ON THE CORRELATIONS OF THE *WALDHEIMIA LENTICULARIS, Deshayes. * W ALDHEIMIA TRIANGULARIS, Hutton. Watpuermia Tayrort, Etheridge, Ann. & Mag. Nat. Hist. 1876, vol. xvii. p. 18, pl if. 3; Pabeal-c. plexiats 2: EcHInoDERMATA. *Mroma (?) Crawrorp1, Hutton. Mroma (?) BrevipETazata, Hutton, Cat. Tertiary Moll. and Echin. of N. Z. p. 48. Found also in the Cobden limestone. “ScHIZASTER RoTUNDATUS, Zittel, Reise der ‘ Novara,’ Geol. ii. p. 64, tad: ai Mik, Found also in Upper Eocene rocks at Cape Farewell and Oamaru. Also at Aotea and Port Waikato. C@LENTERATA. : SpHENoTRocHUS Hurronranus, Tenison-Woods, Paleont. of N. Z. pt. iv. Corals and Bryozoa, 1880, p. 10, f. 9. *FLABELLUM RADIANS, Ten.-Woods, J.c. p. 14, f. 13. Found also in the Upper Eocene rocks at Oamaru. *FLABELLUM CIRCULARE, T'en.-Woods, J. c. p. 12, f. 7. Found also at Wanganui. Of these 26 species, 12 (including 2 vertebrates) occur in the Curiosity-Shop beds, and 8 others are found in other places in New Zealand in rocks of Upper Eocene age or younger. Of the remaining six, two are Miocene fossils in Australia. I cannot therefore hesitate in putting the Weka-pass stone into the same system as the Curiosity-Shop beds. It must also be noticed that Pecten Zittel, Hutton (Cat. Tert. Moll. N. Z. p. 32), occurs in the “Grey Marl ” above the Weka- wes stone T, which must also be re- ferred to the same series. List oF THE O7ToTARA Fossits FRoM OAMARU. * Species marked with an asterisk are also found in the Curiosity- Shop beds, or the Weka-pass stone, or in younger rocks, VERTEBRATA, *PALHEUDYPTES ANTARCTICUS, Var. AUSTRALIS, Huxley. In the Ototara limestone. Mo.utvsca. *ATURIA ZICZAC, Var. AUSTRALIS, M°Coy. In the Kakanui limestone. + Quart. Journ. Geol. Soc. vol. xli. p. 274, and Cat, Colonial Museum, Wellington, 1870, p. 190 (Pecten pleuronectes). ‘¢ CURIOSITY-SHOP BED ” IN CANTERBURY, NEW ZEALAND. 557 *VOLUTA PACIFICA, Var. ELONGATA, Swainson. In the Ototara limestone. *SCALARIA LYRATA, Zittel. In the Ototara limestone. *PLEUROTOMARIA TERTIARIA, M°Coy. In the Ototara limestone of Cave Valley. *Dentatium Mantes, Zittel, Reise der ‘Novara,’ Geol. u. p. 45. D. wrregulare, Hutton, J. ¢. p. 1. At Mahemo. Found elsewhere only in the Pareora system. *CUCULLHA ALTA, Sowerby. In Volcanic tuff at Kakanui. *PrcoreN Hocustetrert, Zittel. In the Ototara limestone. *Prcren Fiscuert, Zittel. In the Ototara limestone at Cave Valley. *Prcoten Hucrori, Hutton, Cat. Tertiary Moll. of N. Z. p. 30. In the Kakanui limestone; also’ at Brighton; and according to Mr. M°Kay, in the Upper Eocene rocks at Trelissic Basin. *Prcten Hurcurnsoni, Hutton. In the Kakanui limestone, and the volcanic tuff at Kakanui. *Prcren CrawForpi, Hutton, Cat. Tertiary Moll. of N. Z. p. 32. In the volcanic tuff at Kakanui. Found also in the Pareora ~ system. . - PECTEN, sp. ind. Maheno. *PECTEN POLYMORPHOIDES, Zittel, Reise der ‘ Novara,’ Geol. 1. p. 51, plxi., f. 3. In volcanic tuff at Kakanui; also, according to Mr. M*Kay, in the Upper Hocene rocks at Trelissic Basin. *Lima PALEATA, Hutton. In the Ototara limestone. BRACHIOPODA, WALDHEIMIA GRAVIDA, Siiss, Reise der ‘ Novara,’ Geol. i. p. 56, plese tT, S: In the Kakanui limestone. 558 CAPT. F. W. HUTTON ON THE CORRELATIONS OF THE *WALDHEIMIA sUFFLATA, Tate, Trans. Phil. Soc. of Adelaide, 1880, p. 18, pl. vin. f. 4. In the Kakanui limestone. Found also in the Pareora and Wan- ganui systems. *TEREBRATELLA GAULTERI, Morris. In the Ototara limestone at Cave Valley. Maeasetta Woops, Tate, Trans. Phil. Soc. Adelaide, 1880, p. 24, plats. Waldheimia taprrina, Hutton, l. ¢. p. 36. In the Ototara limestone at Cave Valley. Also in the Cobden limestone. EcHINODERMATA. MacropneEvstss (?) sPATANGIFORMIS, Hutton, Cat. Tertiary Moll. and Kchin. of N. Z. p. 40. In the Ototara limestone; also in the Cobden limestone. *Mzoma (?) Crawrorpr, Hutton. In the Ototara limestone. Here again we have 21 species, of which 11, including Paleeu- dyptes, are found in the Curiosity-Shop or the Weka-pass stone; and of the others, six are found in the Upper Eocene or younger deposits, leaving only four as possible Cretaceo-Tertiary forms, and these, it must be remembered, are not identical with any Waipara fossils. VALLEY OF THE WAITAKI. Although I am unable to give anything like a complete list of the fossils found in the Valley of the Waitaki, the district is too important to be passed over. The following are mentioned by Dr. Hector and by Mr. M*Kay as occurring in rocks belonging to the Cretaceo-Tertiary series (Rep. Geol. Expl. 1881). I have also added four others from the Waihao limestone in the Canterbury Museum. Maerewhenua Inmestone. Kekenodon onamata, Hector, Trans. N. Z. Inst. vol. xiii. p. 485, pl. xviii. 1881). eee bones, in the lower part. Pecten Hochstetteri, Zittel. Meoma (?) Crawfordi, Hutton. Graphularia (?) senescens, Taée. Flabellum circulare, Ten.- Woods. In 1880 Mr. M*Kay stated that the beds overlying the Maere- whenua limestone must be referred to the Cretaceo-Tertiary series from “the character of a majority of the fossils found in them” (Geol. Rep. 1881, p. 69); but the next year he referred this lime- stone with the overlying beds to the Upper Eocene, also on account of the fossils found in them (l. ¢. p. 103). Certainly there is no paleontological reason for separating this limestone from the Weka- pass stone and the Curiosity-Shop beds. ° ‘‘ CURIOSITY-SHOP BED ’’ IN CANTERBURY, NEW ZEALAND. 509 Wathao Limestone. Carcharodon angustidens, Ag. Waldheimia lenticularis, Deshayes. Eupatagus Grayi, Hutton, 1. c. p.41; also found in the Cobden limestone. Macropneustes (?) spatangiformis, Hutton. Graphularia (?) senescens, Tate. In “‘ Chalk-marls” below the limestone are the following :— Pecten Zittelli, Hutton. Sphenotrochus Huttonianus, Tenison- Woods. Here the Echinoderms are different from those of the Curiosity Shop and Weka pass, but one of them is found in the Ototara lime- stone; and, as the beds are underlain by rocks containing the Pecten Zitteli and Sphenotrochus Huttonianus of the Weka-pass stone, they cannot be looked upon as indicating a greater age. In Marly Greensands below the Limestones. At Maerewhenua :— Cetacean bones. At Wharekauri :— Nautilus danicus, D’ Orb. (?)* Harpactocarcinus tumidus, H. Woodward, Quart. Journ. Geol. Soe. vol. xxxii. p.71; found alsoat Brighton, and at Double Corner, N. Can- terbury. At Waihao :— Aturia ziczac, var. australis, M°Coy. Pleurotoma, sp., like Pareora forms. ; Limopsis, sp., like P. aurita, an Upper Eocene and Miocene form. — Here we have certainly a Cretaceous species in WVautilus danicus,. but it is doubtfully identified by Mr. M°Kay, and is probably the ventricose form of A. ziczac. In the Island Sandstone at Black Point. Aneyloceras (?), sp., Hector, Geol. Rep. 1876-7, p. x. Baculites (?), sp., Hector, 0. c. Belemnites (?), sp., Hector, 1. ¢. Here also we get Cretaceous Cephalopoda, but all are doubtfully determined. Mr. M*Kay kindly showed me these fossils in the Wellington Museum. There is, 1 believe, but one form. It is a small, delicate, straight shell, slightly tapering, with rather close, well-marked, transverse ribs (like Tentaculites). It looks like a Cephalopod, but no section has been made. The siphon is said to be marginal ; but it is obscure, and I could not satisfy myself of its ‘presence. Thereis no external appearance of lobed or foliated septa. * Mr. McKay informs me that this is the same as his so-called Ammonite from near Greymouth, Geol. Rep. 1873-4, p. 81. QJ. G°S.No. 164. QR 560 CAPT. F. W. HUTTON ON THE CORRELATIONS OF THE It cannot be Ancyloceras, because the ribs are of equal strength all round; and it cannot be Baculites, because the ribs are quite trans- verse. If it be a Cephalopod at all, it must, I think, bea new genus. and consequently it has but little chronological value. Evidently, if we can trust to paleontological evidence, the Ototara series, both at Oamaru and in the Waitaki Valley, together with the Weka-pass stone, must be included in one system with the Curiosity-Shop beds. Mr. M*Kay certainly says of the fossils of the Cretaceo-Tertiary series that “in all cases these are speci- fically different from the shells found in the higher parts of the series, which are mainly the fossils of Professor Hutton’s Oamaru formation ” (Geol. Rep. 1883-4, p. 59); but, as he gives no name, it is impossible to attempt to reconcile his statement with my list, and it is opposed to his own list of the fossils of the Trelissic Basin - (Geol. Rep. 1879-80, p. 70), where about one fifth are common to both series. But Dr. Hector does not rely altogether on paleontological evi- dence for separating his Upper Eocene rocks from the upper part of his Cretaceo-Tertiary series; he considers that an unconformity exists between them. I have already shown that no unconformity exists in the Weka-pass district *. I will now take the north of Otago, a district which I examined in December 1873. Dr. Hector says, ‘‘ These higher [Upper Eocene] beds it has been impossible to separate, either stratigraphically or otherwise, from the Awamoa series [Pareora beds|, which overlie them ; whilst be- tween this and the underlying Cretaceo-Tertiary series unconformity is to be observed at several points, as in the Cape Hills [Oamaru], and at Cape Campbell (vide Report on that district), although it, may be doubted whether the Awatere beds, which there rest unconform- ably on the Cretaceo-Tertiary series, are the true equivalents of the Awamoa beds, or of Upper Miocene age. Apart from this, however, the character of the volcanic rocks at Oamaru, as evidencing the existence of a land-surface, together with their superior position to those of the calcareous beds of Hutchinson’s quarry, with the Awamoa beds resting conformably on them in Lime-kiln Gully, sufficiently attest the unconformity, which is further supported by the occurrence of an outlier of Awamoa beds resting upon the green- sands and coal-grits in the Waireka Valley”+. This argument may be summed up as follows :—The volcanic rocks at Oamaru Cape prove a land-surface ; consequently the Hutchinson’s-quarry beds which lie above the volcanic rocks must be unconformable to the Cretaceo- Tertiary which lie below them. Further, no unconformity can be made out between the Hutchinson’s-quarry beds and the overlying Awamoa series (Pareora system); but at Cape Campbell (300 miles away) beds belonging to the Pareora system (Awatere series) are unconformable to the Cretaceo-Tertiary ; it may, however, be doubted * “*On the Geological position of the Weka-pass Stone,” Quart. Journ. Geol. e. vol. xli. p. 266. + Report of Geological Explorations, 1876-7, p. ix. ‘6 CURIOSITY-SHOP BED’ IN CANTERBURY, NEW ZEALAND. 561 whether the Awatere series is the equivalent of the Awamoa series. Now neither Dr. Hector nor Mr. M°Kay gives any proof of this land-surface ; but Mr. M‘Kay told me that his reason for assuming its existence was the scoriaceous nature of some of the rocks, which is quite insufficient. Also I fail to see in Mr. M*Kay’s Report any evidence at all of an unconformity. He certainly gives a section (No. 3) showing an unconformity ; but there must be some mistake, as the unconformity is placed between the Hutchinson’s-quarry bed and volcanic tuffs which wnderlie the Ototara limestone, while the argument is founded on the assumption that the tuffs overlie the Ototara limestone. When I examined Ototara Cape in 1873 I did not notice any unconformity ; but I have had no opportunity of examining the locality since Mr. M*Kay’s Report was published. Cape Oamaru is formed by an old volcano, which has broken through the Ototara limestone and was active when the marine beds of Hutchinson’s quarry were being deposited. Also the outlier of the Awamoa series on the “‘Cretaceo-Tertiary greensands and coal-grits,” in the Waireka Valley, proves an unconformity between the Awamoa series and the Hutchinson’s-quarry beds (which are missing), and Fig. 2.—Map of the Valley of the Waitaki and neighbouring region. go Fo We & pala wer I ES eS LY Ga ff _<@a We ; Ss \ = Oamaru Cape S| Awamoa AA wa LANG ENG : _ SY Fiakanui.R. 0 5 10 Miles Alluvia. Pareora System. Limestones. Sal Tertiary, uncertain. GF Schists and Slates. 1. Waihao Limestone. 3. Maerewhenua Limestone. 2. Otakaika Limestone. ~ 4, Ototara Limestone. 222 562 CAPT, F. W. HUTTON ON THE CORRELATIONS OF THE not between these latter and the Cretaceo-Tertiary, as supposed by Dr. Hector*. I fail therefore to see any unconformity between the Upper Eocene and the Cretaceo-Tertiary near Oamaru. In his Progress Report for 1881 (Geol. Reports, 1881, p. xxii), Dr. Hector says, “Tn the Waitaki Valley, and in the same district as far south as the mouth of the Kakanui River, Tertiary rocks, comprising lime- stones and calcareous greensands belonging to the Upper Eocene period, are present, resting indifferently on various members of the Cretaceo-Tertiary series ;” and in the ‘Sixteenth Annual Report of the Colonial Museum,’ published in 1882, Dr. Hector says that “in the Waitaki Valley he [Mr. M*Kay] completely cleared up the evidence on which the subdivision of the Lower Tertiary and Upper Cretaceous strata had been proposed, and obtained a large addition to the collection of fossils” (p. 7)f. I have carefully ex- amined Mr. M*Kay’s ‘ Report on the Geology of the Waitaki Valley’ (l. c. p. 56), for proofs of this statement, but without much success, almost all the cases given referring to unconformity of the Pareora system, and not to the Hutchinson’s-quarry beds. The rocks are said to be as under (see Map, fig. 2) :— Upper Eocene. : 1. Hutchinson’s-Quarry Beds: Greensands full of Waldhetmia triangularis (Hutton). 2. Otakaika Limestone: a calcareous greensand=Nummulitic Limestone. 3. Kekenodon Beds: marly greensands restricted to Wharekauri. Cretaceo-Tertiary. 4. Grey marls: grey sands. 5 Maerewhenua Limestone: a calcareous greensand \ =Ototara Lime- { Waihes Limestone: a white limestone. j{ stone. 6. Marly Greensands. 7. Island Sandstone: loose sandy beds with bands of calcareous rock. 8. Coal-beds. There is no stratigraphical continuity between these rocks and those at Oamaru; and in no locality is the Otakaika limestone seen to overlie the Maerewhenua limestone. Mr. M°Kay certainly says that ‘‘on stratigraphical grounds the Maerewhenua limestone must be regarded as distinct from the Otakaika limestone” (Geol. Reports, 1881, p. 66), and that he will give the evidence further on in his Report ; but I have not been able to find it. It would seem therefore that the correlations must depend upon paleontological evidence ; but no lists of fossils are given. Mr. M°Kay’s line of proof seems to be different. He says, “ In either locality [Oamaru and Maerewhenua] * In his last Report Mr. M¢Kay has omitted this outlier. He now says that “all the strata developed west of the Waireka Valley and lower part of the Kakanui River pass under the higher part of the Cretaceo-Tertiary series repre- sented by the Ototara calcareous sandstone, all Eocene and Miocene strata lying to the eastward of the great limestone scarp” (Geol. Rep. 1883-4, p. 62). But he gives no reasons for this change, and it is against the palzontological evidence. t See also Trans, N. Z. Institute, vol. xiv. p. 524. “‘ CURIOSITY-SHOP BED”? IN CANTERBURY, NEW ZEALAND. 563 the limestones are conformable to the beds which underlie, and these, proving to be the equivalents of each other, prove also the syn- chronism of the Ototara and Maerewhenua limestones” (l. ¢. p. 69). But he has just before said (on the same page) that, as the identity of the Ototara stone with the Maerewhenua limestone cannot be proved by fossils, because these are too few in the Ototara stone, “it thus became necessary to prove the relationship of the beds underlying the limestones in the two localities. Here again the tufas of the Waireka Valley differed considerably from the grey sands and marly greensands underlying the Maerewhenua lime- stone; and while in the latter locality the beds proved highly _ fossiliferous, fossils were wholly absent in the beds underlying the Ototara stone, so that in this case also identity could not be proved by means of the fossil contents of the beds.” I do not wish to dispute this point, as I believe all to belong to the same series. I merely wish to show that he has not proved his case. Indeed, in a further Report, printed in the same volume, Mr. M°Kay says that “the middle part of the Maerewhenua limestone belongs, I consider, to this horizon [ Otakaika limestone], leaving only the lower portion ° of that rock as the equivalent of the Ototara limestone” (J. ¢. p. 103), thus abandoning his supposed proof altogether. This alteration was made because remains of Kekenodon (a Zeuglodont) were discovered in the limestone; and this change alone must throw considerable doubt on the asserted unconformity between the Upper Kocene and Cretaceo-Tertiary rocks in this district. But, as a matter of fact, I can only find in the Report one place in which an unconformity is said by Mr. M°Kay to occur between the Upper Eocene and Cretaceo-Tertiary series. In his “ Section showing position of coal-seam, Wharekauri” (l.c. p. 64), the Otakaika limestone (No. 2) is shown unconformable to the marly greensands (No. 6). ‘The section is described as a sketch of the rocks seen in following up the Wharekauri Creek from the Waitaki; but at p. 73 he says that this section is, he believes, “‘ exactly as the section would appear, provided the obscuring gravels could be cleared away,” so that evidently its accuracy may be doubted. Also no evidence is given that these ‘‘marly greensands” are not the Kekenodon beds, which are found in the close neighbourhood, it being merely stated that the unconformity 1s demonstrated “ by the absence of the higher part of the marly greensands and the Maerewhenua limestone”’ (l.c. p. 68). Mr. M°Kay remarks that here “the section of the younger beds is somewhat complicated; and from the fact that the Kekenodon beds are themselves a marly greensand, and their un- conformity to the Cretaceo-Tertiary marly greensands not being well marked, the two sets of beds may in places be taken to represent the higher and lower parts of the same series” (l.¢. p. 73). Evi- dently there is here no “‘clear proof” of unconformity, especially as in his Second Report Mr. M*Kay describes the underlying marly greensands in this locality as “nearly horizontal” (J. c. p. 101), and therefore conformable in position to the overlying limestone. He certainly says that “the fossils belonging to the two horizons [of 564 ON THE CORRELATIONS OF THE ‘** CURIOSITY-SHOP BED.” marly greensands] are very dissimilar” (J. ¢. p. 73); but this state- ment cannot be received as full evidence until lists of the fossils are published. In fact there appears to be no actual proof of uncon- formity anywhere; it is merely argued that such an unconformity must exist because the Maerewhenua limestone ought in certain places to come in between the two beds of marly greensand. But this argument rests entirely on the assumption that the Maere- whenua limestone is older than the Kekenodon beds, and differs from the Otakaika limestone, of which no proof at all is given; and, as bones of Kekenodon have been since found in the Maerewhenua limestone, it is evident that the whole argument collapses. Indeed, in his Second Report, Mr. M*Kay calls the Otakaika limestone the equivalent of the middle part of the Maerewhenua limestone (I. ¢. p. 104); and if this be so, the Kekenodon beds would appear to be the same as the so-called Cretaceo-Tertiary marly greensands; and the whole of the rocks, from the Hutchinson’s-quarry beds down to the marly greensands, would form a single series, No. 1 in the Table (p. 1) being the same as No. 4, No. 2 the same as No. 5, and No. 3 the same as No. 6. It seems to me that this is the only way in which “the evidence on which the subdivision of the Lower Tertiary and Upper Cretaceous strata has been proposed” can be “‘ completely cleared up.” The stratigraphical evidence fails, therefore, equally with the paleontological evidence, to indicate any important break between these rocks, and the whole of them must be included in one system, the Oamaru System of Dr. von Haast and myself *. Discussion. Dr. BuanForp pointed out that of the 48 species from the Curiosity-Shop beds, 10, or more than 20 per cent., are still living. Such a percentage could scarcely be expected in beds older than Oligocene, and was remarkable even in strata of that age. Dr. Duncan said that he had not found so large a proportion of living species of Echinodermata and Corals even in the Miocene beds of Western India. The more carefully the morphology of late Tertiary forms was studied the fewer were the species which de- scended from the Tertiaries to the recent faunas. Even in the deep-sea faunas the species which were assigned to old genera belonged to special divisions of them. Mr. Torey inquired how far Cretaceous forms prevailed. Mr. Bianrorp read over the list of genera, which showed that very few, if any, characteristically Cretaceous types occurred in the deposit. * Some of the ‘“‘Cretaceo-Tertiary ” greensands and coal may, I think, prove to belong to the Pareora system. ON THE FOSSIL FLORA OF SAGOR, IN CARNIOLA, 565 42. On the Fosstz Fiona of Sagor, in Carntonra. By Constantin Baron von Errinesnavsen, Professor at the University of Graz, Austria, (Read June 24, 1885.) Havine recently brought the third and last part of my work on the Fossil Flora of Sagor before the Imperial Academy of Sciences in Vienna, I take the liberty of reporting to the Geological Society on the facts which may be considered interesting to the science of Palzontology, and on the principal results which have been obtained from my investigations upon the subject. The fossil plant- remains which were brought to light, mostly by my method of im- pregnating the stones with water and splitting them by freezing, came from fourteen localities :— 1. Beds called “ Friedhofschichten,” beneath the Brown Coal of Sagor. They occur near the churchyard of Sagor, and consist of yellowish-grey indurated clay. They contain many well-preserved plant-remains belonging to 40 species, many of which have also been found at Hiring and Sotzka, and in the Lower Tertiary beds of Switzerland. Among the specimens I have examined there are cones of Actinostrobus, seeds of Embothrium leptospermum and Hakea macroptera, flowers of Celastrus protogeus, fruits of Termi- naha Fenzliana, and leaves of Corylus MacQuarrit, Quercus cuspidata, Ficus primeva, Cinnamomum lanceolatum, Grevillea heringiana, Dodonea salicites, Zizyphus undulatus, Eucalyptus heringiana, Dalbergia primeva, Cesalpina Haidingeri, &c. 2. Beds called ‘‘ Bachschichten,” near Sagor. These and all the following beds here enumerated lie above the Brown Coal. Their plant-remains indicate a flora which in no respect differs from the fossil flora of the Wetterau, of the Brown-coal formation of the Lower Rhine, and of the Aquitanian Tertiary beds of Switzerland. The “Bachschichten,” consisting of dark grey indurated clay, are rich in fossil plants, and a careful investigation of them brought to light a flora of 79 species. Of these are particularly to be named Chondrites laurencioides, Davallia Haidingeri, Callitris Brongniarti, Sequoia Coutisic, Ostrya atlantidis, Quercus Lonchitis, Ficus lanceolata, Desch- manm, and Langeri, Laurus tristanicefolia, Sapotacites minor, Crssus Heer, Zizyphus paradisiacus, Rhus hydrophila, Terminalha mio- cenica, Hugenia Apollinis, Psoralea paleogea, Paleolobium hetero- phyllum, and Mimosites heringianus. 3. Beds called “‘Tagbau Schichte I.” They occur near the smelting= house of the tin-works in Sagor, and consist of yellowish-grey or yellowish-white indurated clay, which is not so rich in fossils as the preceding beds. Of the species to be found there, I may mention Taxodium distichum miocenicum, Sequoia Tournalit, Pinus hepios, Myrica deperdita, Fagus Feronie, Pterospermum sagorianum, Bur- saria radobojana, Dalbergia valdensis. 4, Beds called after the ‘‘ Francisci Erbstollen,” near the Sagor 566 CONSTANTIN BARON VON ETTINGSHAUSEN ON THE works. They show a bluish-grey shale, which seldom contains fossils. As yet only the following species have been discovered :— Glyptostrobus europeus, Sequoia Coutisice, Ficus sagoriana, F. bume- hefolia, Banksia longifolia, Andromeda protogea, and Eucalyptus oceanica, all very common in the beds Nos. 2, 8, 9, 11, and 14. 5. Beds near Sagor, containing fossil fishes, but very few fossil plants. They occur in agrey indurated clay, and the latter includes Glyptostrobus europeus, Sequoia Coutisiw, Ficus bumeliefolia, Cin- namomum polymorphum, Bumelia oreadum, and Andromeda pro- toged. 6. Beds called ‘‘Tagbau Schichte I1.,” near Sagor. The fossil plants are here to be found in a light or yellowish-grey indurated clay, and belong to Chara Ungeri, Ch. Langeri, Glyptostrobus europeus, Sequoia Couttsie, Zostera Unger, Castanea atavia, Quercus Lonchitis, Ficus bumeliefolia, Pisonia eocenica, Banksia longifolia, Apocyno- phyllum breve-petiolatum, Andromeda protogea, Robima crenata, Dalbergia heringiana, Cassia paleogea, and Podogonium Lyelli- anum. ; 7. Close by the village of Godredesch, near Sagor, there are some _ beds consisting of dark-grey indurated clay, like that of the beds No. 2. They conta plant-remains which have been referred to 11 species. With the exception of Myrsine Endymionis, Cussonia ambigua, and Pistacia palco-lentiscus, these also occur in the beds No. 2. 8 and 9. Near the village of Savine, in the neighbourhood of Sagor, there are two very rich localities of fossil plants. ‘The beds consist of a light- or yellow-grey marl, which contains well- preserved fossils. From this I have obtained a flora consisting of 313 species, which form the principal part of the fossil flora of Sagor. The locality No. 8 is the quarry from which the most valuable fossils came. Of these I mention the following as possess- ing special interest :—Muscites savinensis, Blechnum Brauni, two forms of Hquisetum, Cunninghamia miocenca, Snulax paucimervis, Pandanus carniolicus, Laurelia rediviwa, Laurus stenophylla, Intsea dermatophyllum, Conospermum macrophyllum, Cenarrhenes Hauert, Persoonia cuspidata, two forms of Hakea, Hmbothrium stenospermum, Lomatia oceanica, Olea carniolica, Fraainus primigena, Sapotacites chamedrys, Diospyros bilinica, Symplocos savinensis, Callicoma mi- crophylla, Clematis sagortana, Tetrapteris minuta, six species of Celastrus, Pomaderris acuminata, Ptelea intermedia, Ailanthus Ori- onis, Vochysia europea, and nine species of Papilionacez. The locality No. 9 is the top of a coal-pit from which the fossil plants came. I have selected for mention a few of the many new forms which I found there :—Actinostrobus miocenicus, Leptomeria distans, Embothrium macropterum, Notelea rectinervis, Fraximus savinensis, Alstonia carniolica, Chrysophyllum sagorianum, Vacer- nium paleo-myrtillus, Loranthus paleo-ewocarpi, Bombax sagoria- num, Pittosporum paleo-tetraspermum, and Ptelea mecrocarpa. 10. Islaak, near Sagor. The fossil plants occur here in greyish white marl, looking somewhat like that of Savine. All the fossils FOSSIL FLORA OF SAGOR, IN CARNIOLA. 567 which I discovered in it are to be found also at Savine, excepting Heliotropites parvifolius. 11. Trifail. The beds resting upon the coal strata are rich in different plant-remains, which mostly occur in a dark grey indurated clay, like that of the locality No. 2. The most interesting of the species collected here are the following :—Cystoseira communis, Taxodium distichum miocenicum, Pinus paleo-teda, Fagus Feronie, Castanea atavia, Banksia Haidingeri, Bumelha scabra, Diospyros heringiana, Sapindophyllum paradoxum, Carya trifailensis, Prunus mohikana, and P. palco-cerasus. 12. Hrastnigg. I obtained from a coal-pit the following species of fossil plants, which occur in a lght-grey marl :—Hypnum sagorianum, Gilyptostrobus europeus, Sequoia Couttsie, Typha latis- sima, Cinnamomum polymorphum, Banksia longifolia, Bumelia Oreadum, Andromeda protogea, Anectomeria Brongniarti, Nymphea gypsorum, Eucalyptus oceanica, and Phaseolites microphyllus. Of these, nine occur also at Savine. 13. Bresno. In a yellowish-grey marl here I found well-pre- served fossil plants belonging to the following species :—Glypto- strobus europeus, Sequoia Tournalu and Coutisie, Carpinus Heern, Ficus tyne and bumeliefolia, Cinnamomum polymorphum, Banksia longifolia, Sapotacites sideroxyloides and emarginatus, Mimusops tertiaria, Bumelia Oreadum, Andromeda protogea, Celastrus proto- geus, and Eucalyptus oceanica. 14. Tuffer. The fossil plants occur in a light or somewhat reddish-grey marl-slate resembling that of Savine. I found there many well-preserved fossils belonging to Hypnum sagorianum, Glyptostrobus europeus, Sequoia Couttsie, Pinus paleo-teda, Typha latissema, Myrica salicina, Castanopsis .sagoriana, Quercus Lonchitis, Freus sagoriana and bumeliefolia, Pisonia eccenica, Hedycarya europed, Laurus Hauert, Cinnamomum polymorphum, Banksia longifolia, Sapotacites sideroxyloides, Bumelia Oreadum, Andromeda protogea, Celastrus protogeus, Eucalyptus oceanica, Eugenia Apol- binis. I proceed now to explain the general results of my investigations of the Sagor fossil flora :— Istly, the fossil flora of Sagor contains at least 170 genera and 387 species, which are distributed under 75 families. Of the species, 21 belong to the Cryptogamez, 18 to the Gymnosperme, 14 to the Monocotyledons, 117 to the Apetale, 61 to the Gamopetale, and 156 to the Dialypetale. 18 species were aquatic, but all the others terrestrial plants. 2ndly, the fossil flora of Sagor consists of two floras of different ages, but immediately following one another. The beds No. 1, which underlie the coal, and may be the. basement beds of the Ter- tiary of Sagor, inelude a flora which existed in the last section of the Eocene period. The other beds, resting upon the coal, contain the remains of a flora belonging to the first section of the Miocene period. 3rdly. In consequence of the great diversity of fossil plants, and °° [alr - oe . —_— ly ee oe aagmamee e ae es 568 ON THE FOSSIL FLORA OF SAGOR, IN CARNIOLA. their abundance in some of the localities, the elements of the floras are so distinctly marked as to place it beyond doubt that the Tertiary flora is to be considered the origin of all the living floras of the globe, a conclusion to which the investigations of the floras of other Tertiary localities have already led. In the fossil flora of Sagor the following floras are represented :— Austria by Actinostrobus, Casuarina, Leptomeria, Santalum, sp., Conospermum, Persoonia, Grevillea, Hakea, Lambertia, Lomatia, sp., Banksia, Dryandra, Noteleca, Myoporum, Lonnie. Sp., Callicoma, Ceratopetalum, Sterculia, sp., Dodonca, sp., Bursaria, Elaodendron, sp., Pomaderris, Eucalyptus, Kennedya. Norra America and Mexico by Tawodium, Pinus, sp., Myrica, sp., Betula, sp., Fagus, sp., Ostrya, sp., Quercus, sp., Ulmus, sp., Platanus, sp., Symplocos, sp., Vaccinium, sp., Cornus, sp., Magnolia, sp., Acer, sp., Hvonymus, sp., Prinos, Berchemia, Ilex, Carya, Ptelea, sp., Prunus, sp., Robinia, and Erythrina. Catrrornia by Libocedrus, sp., Sequoia, Pinus, sp. Brazit and Tropicat Sourn AMERICA IN GENERAL by Blech- num, sp., Ficus, sp., Pisonia, sp., Persea, sp., Ocotea, Andromeda, sp., Weimmannia, sp., Bombax, sp., Ternstremia, Tetrapteris, Bani- steria, Sapindus, sp., Xanthoxylum, sp., Vochysia, Dioclea, Mache- rium, Cassia, sp., Acacia, sp. Curt by Podocarpus, sp., Laurelia, Cassia, sp. Iyora and East-Iypran Istanps by Castanopsis, Ficus, sp., Phabe, sp., Cnnamomum, Mimusops, Sterculia, Pterospermum, Prttosporum, sp., Dalbergia, Sophora, sp., Ceesalpinia. Cuina and Japan by Glyptostr obus, Cinnamumum, sp., H: 'ydranged, sp., Acer, sp., Styphnolobium. Evrorz by Pinus, sp., Phragmites, Zostera, T' ppl Alnus, Car- pis, Corylus, bese Ulinus, sp., Ligustrum, Olea, sp., Eee sp., Vaccinium, sp., Acer, Sp., Pistacia, sp., Prunus, sp., Psoralea, Sp. The Can artis by Davallia, Sp., Laurus, Sp., Per Sed, Sp. Arrica by Callitris, Kennedya, Sp., Olea, sp., Coussoma, Celas- trus, Sp., Prerocelastrus, and Fthus, sp. Norrorx Istanp by ‘Araucaria, sp., and Hlwodendron, sp. New Zearanp by Hedycarya, sp., Cenarrhenes, Weinmannia, sp. ON THE GOLDFIELDS OF LYDENBURG AND DE KAAP, S. AFRICA. 9569 43, A Sxercu of the Gotprtetps of Lypensure and Dr Kaap, in the TRaNsvaaL, Sourm ArricA. By W. Henry Pennine, Ksq., F.G.S., &c. (Read May 27, 1885.) ConrTeENTs, . Estimated Extent of the Gold Country. . Lydenburg and De Kaap Goldfields. 1. Geology of the Kaap Valley &e. 2. Granitic? Rocks. 3. Silurian? Rocks. 4. Sections and Reefs, a—f. 5. Devonian ? Rocks. 6. Sections and Auriferous Deposits, a’-q’. 3. Alluvial Auriferous Deposits. 4. Gold and Nuggets. 5. Other Metals and Minerals. 6. The Diorite Dykes. CRU bD . CRURURU? § 1. Estrmarep Extent oF THE Gotp CountTRY. Tue goldfields of the Tati are about 100 miles beyond the Limpopo River, the northern beundary of the Transvaal, and those of Hartley Hill are 250 miles still further towards the interior. These fields have been described by the late Mr. Thomas Baines, F.R.G.S., in his work on ‘ The Gold Regions of South-eastern Africa’ *, and prove the extension of auriferous veins through at least 73 degrees of latitude, 7. @. from the Kaap Valley to Hartley Hill (18° to 25° 30’ §.). ‘From the gold-lodes west of Pretoria to the site of Herr Carl Mauch’s discovery near the Olifant’s River in 1868, a space intervenes cover- ing three degrees of longitude (28° 30’ to 31° 30’ E.). Gold has been found at many points within, as it must also be found beyond, the area thus arbitrarily limited. which certainly covers not less than 100,000 square miles. § 2. Lyprensure anp Dr Kaap GoLprreps. The Lydenburg and De Kaap Goldfields, as at present known, are included within a line passing W. from the northern point of Swazi- land, through the Tefelkop mountains, thence N. through Lydenburg and along the Orighstad River to its junction with the Blyde. Now turning S., the line follows the edge of the berg, or eastern face of the Drakensberg mountains, to near Spitzkop, and thence back to its starting-point on the border-mountains of Swaziland. (See Map, Quart. Journ. Geol. Soc. vol. xl. p. 658; and Map in the Journ. Soc. Arts, vol. xxxii. 1884, p. 609.) This area extends over about 1 degree of latitude (24° 35’ 8. to 25° 50’S8.), and, on the average, half a degree of longitude (30° 30’ to 30° 45’ on the N., 31° 15’ on the S.), thus being about 3000 square miles. For some notes on this country see a paper by the author in Journ. Soc. Arts, vol. xxxil. 1884, p. 608. * Stanford, London, 1877. 570 W. H. PENNING ON THE GOLDFIELDS OF The physical features of the triangular tract of country occupied by the Lydenburg and De Kaap goldfields, between Swaziland, the Tafelkop, and the junction of the Blyde and Orighstad rivers, may be briefly described. ‘The western side is upon the Drakensberg mountains, the highest part of the range following a nearly N. and S. line, from near the junction of the rivers, by Mauch’s Berg and Spitzkop to the Tafelberg, whence the Kaap mountains branch off to the E. towards the Makoujwa mountains, which form the N.W. boundary of Swaziland. Part of the range N. of the Tafelberg, and between it and the Krokodil River, is named the “* Godwaan Plateau.” The Drakensberg mountains fall gradually away to the W., but present a very precipitous face (or “krantz,” as it is called) to the E. This krantz overlooks the lower country, which is traversed by the Sabie and Krokodil Rivers, with their affluents, the united waters of which, with those of the Komati, fall into the Indian Ocean north of Delagoa Bay. It is a noteworthy feature that the sources of most of these rivers are a long way to the westward of the highest parts of the mountain- range. The general surface slopes W., but the rivers flow E., pass- ing through deep gorges, called ‘‘poorts,” in the mountains. The Blyde and Orighstad rivers unite at the back of the range, and pass through the “ Blyde Poort.” The Eland’s Spruit joins the Krokodil River, just behind the Godwaan Plateau and before entering the “‘Krokodil Poort.” In a similar manner the Komati and Krokodil Rivers unite (further to the east) just before passing through the “« Lower Komati Poort” in the Lebombo Mountains *. : Mauch’s Berg is the highest feature of the range, but Spitzkop is the most prominent, being an isolated peak in the midst of a com- paratively level plain or terrace which borders the low country. There are very few places, except in the valleys, from which Spitzkop cannot be seen, within a radius of fifty or sixty miles. “In the angle formed by the junction of Eland’s Spruit with the Krokodil River is the Godwaan Plateau, an elevated tract some four or five miles in width ” f. 1. The Geology of the Kaap Valley &c.—The following are the main geological features observed by me while travelling :— The oldest rocks of the goldfields are those of the Kaap Valley and those bordering the Krokodil River, as far as yet examined, also, doubtless, occupying the almost unknown region “ below the berg” in the direction of the Blyde Poort. 2. Granitic? Rocks.—An intrusive plutonic rock, geologically newer than the stratified rocks, but still in an inferior position, occupies the whole of the lower ground of the western part of the Kaap Valley. It resembles coarse granite, and consists of quartz and felspar, with but little, if indeed any, mica in its composition. Although this granite (for such it may be called) forms generally * See “A Sketch of the High-level Coalfields of South Africa,” réad before the Society on 5th March, 1884 (Q. J.G. S. vol. xl. p. 658). See also Loveday’s Map of the Lydenburg Goldfield, Pretoria, 1883. t ‘Guide to the Goldfields of South Africa,’ Pretoria, 1883, pp. 44-46. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. the lower ground of the head of the valley, it rises into hills and ridges, some of which have a con- siderable elevation. In some cases it has weathered into bare round- ed bosses bearing a striking re- semblance to roches moutonnées ; but over the greater part of the area the surface of the granite is decomposed into a soft brown substance very much like an allu- vial loam. In the Kaap Valley the surface of the granite forms an ellipse about 17 miles in length by 10 miles in width, with a narrower prolongation in a northerly direc- tion. it widens out again towards the Krokodil River, beyond which it passes in under a series of rocks which rest unconformably upon those with which it has thus far been in contact, and which will probably be found to oceupy the remainder of the Kaap Valley. This mass of granite represents a great centre of plutonic up- heaval, of course posterior to the period of the Kaap-valley rocks, which it has greatly tilted all around its margin; it was, how- ever, anterior to the deposition of the rocks of the overlying uncon- formable formation, as they are still nearly horizontal. 3. Silurian? Rocks.—Nearly all around the granite centre is a series of rocks which have been tilted by it into a more or less vertical position. These rocks are siliceous and argillaceous, rarely, and then but slightly, calca- reous, being mainly schists, shales, cherts, and quartzites. I believe them to be “Silurian” rocks; but, with the exception of an unreliable report of Graptolites haying been observed, there has been hitherto (so far as I am aware) a total absence of fossil evidence. E Kaap , Valley, 5100 ft. 238000 ft Spitzkop, De Kaa 5637 ft. Fall of the Rivers from the ** HighVeldt” re ae aT a=} b .) Das — pa ot eS 3 Ss SD = = 5 = Ee So. ES >> 3s 2 3 SA S 5 DS 3 x Ss = oe? 9 =") — m Sd 2 = a Ss 3 3 ~SS s — S = Sb) a) 3) ~ ~~» S S *-— = S = x a sy S 5s ‘~ qso 38 oe S ex R pa) S Ss S SS s > fo) ai S3 ° q a Oe ey Ee 571 = [a . Se ee > See ~~ cies BC lL eee 572 W. H. PENNING ON THE GOLDFIELDS OF Both the granite and the stratified rocks of this region are tra- versed by intrusive dykes of trap-rock, mostly diorite, some narrow, others of great width, and frequently traceable at the surface for many miles. The main dykes generally, but not always, follow a nearly N. and S. line; the branches run in various direc- tions. 4, Sections and “ Reefs,” a—f—a. At the southern extremity of the granite* some gold-mining has been carried on upon what is known as “ Moodie’s Reef.” ‘This “reef” is situated just N. of “‘ Crawford Creek” (so called on Loveday’s map) which flows here nearly E., then turns northward to join the Kaap River. This creek is really a very deep gorge; on the south side the mountain rises to perhaps 1500 feet in height; on the north a long spur branches out from the mountain, also following an easterly direction, its ridge gradually descending, but being at this point about 800 feet high. It coincides with the strike of the beds, which are vertical, as the ereek coincides with this also until it rounds the end of the spur and turns towards the flat to the north. A difference in the com- position of the beds has, doubtless, been the chief cause of the formation of this steep and peculiar gorge, roughly parallel to the boundary of the granite flat, from which it is separated only by the narrow but lofty ridge along which some of the mines are situated. The rocks of the ridge are schists, shales, cherts, and sandstones, which strike a little 8. of E., and have a dip of about 90°, that is, they are nearly vertical. A bed, or ‘‘seam,” of white crystalline quartz occurs about the centre of the ridge, coinciding with it and with the ordinary stratified rocks in strike and dip. The rocks of the mountain are principally cherts, with some highly altered shales, the same in strike and dip as those of the ridge. In the gorge are loose pieces of chlorite-schist, but that rock was not seen here in place. A few miles to the south on the high Jands, in a farm f cursorily inspected, the rocks seen along the lines traversed were, in ascend- ing order from the edge of the mountain, cherts, shales, and sand- stones, schists and conglomerates. The beds strike E.S.E. and are nearly vertical, but not quite so much so as nearer the granite ; they dip about 85° to the 8. ‘“‘ Moodie’s Reef” (so called) consists of a deposit of white crystal- line quartz, of the kind known by miners as “sugary quartz,” varying from 1 foot to 2 feet wide, and interstratified with the rocks of the district. It might possibly happen for it to occupy such position even if it were a true vein or lode; but I must consider it as a bed of auriferous quartz. Itis just as much so as the schists and cherts are beds, because in so many instances, and over so large an area, gold-bearing deposits of quartz, whatever may be the strike and dip of the beds, occupy asimilar position. This is not by any means the usual mode of occurrence of gold, which is mostly found in veins, * In Farm no. 492 on Loveday’s map. tT No. 505 on Loveday’s map. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. 573 although “it is also more rarely met with in the form of grains in the shales and other unaltered stratified rocks” *: and “ bands of different kinds of iron-ores are said to occur in some of the clay- ironstone interstratified with the slates, and associated with these are certain conformable beds, from which the greatest riches of gold have been obtained ” 7. Mr. J. A. Phillips (quoting Mr. R. B. Smyth) says :—*‘ Gold is now found to occur not only in the quartz-veins and in the alluvial deposits derived from them and the surrounding rocks, but also in the clay- stone itself; and, contrary to expectation, flat bands of auriferous quartz have been discovered in dykes of diorite, which intersect the Upper Silurian or Lower Devonian rocks. Quartz of extraordinary richness has been obtained from these bands” +. In the former case, bands are said to occur, but would appear to be exceptional; in the latter the flat bands are in dykes of diorite, therefore veins, and not beds at all. The auriferous beds now described are numerous and rich, in both the Silurian (?) and Devonian (?) formations, and possess an additional interest from their (so far as I am aware) novel mode of occurrence. One side of the quartz seam called “ Moodie’s Reef,” which would be its north wall if a true vein, but is what was originally its under- side as a bed, is plentifully sprinkled with specks of gold, rather fine, but still quite visible to the naked eye. There is gold also in the body of the quartz; but, so far as I have been able to ascertain, only in small quantity. The abundance of the metal on one side must, however, give a good average yield of gold per ton. On the same side of the quartz there is also a streak of green mineral, not carbonate of copper, which at first sight it resembles, but probably chlorite or some form of serpentine, traces of which are also apparent in the body of the quartz. There are other seams of auriferous quartz in the immediate vicinity ; some of these, discovered before the time of my visit, did not come under my notice—others have been opened since, and -some of them, the ‘‘ Ivy Reef” for example, are said to be very rich indeed in gold. 6. Some miles east of Moodie’s Reef the ‘‘ Umvoti Reef” occurs as a seam of dark-grey quartz, sometimes almost black and flint-like in appearance. This seam is also in the bedding of the rocks, which are hard dark-coloured schists, quite vertical, but here striking to N.E, The “ Umvoti Reef” is also a seam (in the bedding) of dark- grey quartz, varying from 6 to 12 inches in thickness, and contains fine gold; the sample assayed by myself, and in which no gold was visible, yielded the metal at the rate of 160z. 13 dwt. 8 grs. to the ton §. a Barber’s Reef” is close by the Umvoti, but appears to be a true lode, as it is transverse to the strike of the stratified deposits. * Jukes’s ‘ Manual of Geology,’ 3rd edit. 1872, p. 303. t Ibid. p. 305. { ‘Elements of Metallurgy,’ 1874, p. 693. § Described in the author’s Report, November 1884, as yielding gold in the proportion of from 1 to 140 oz. per ton of 2000 lbs. OS eee 574 W. H. PENNING ON THE GOLDFIELDS OF It is of a different character—a creamy-white compact quartz-reef, from 4 to 6 feet wide, dipping E. 70° and striking E. of N., whilst the stratified rocks here strike N.E., a difference of upwards of 30 degrees. d. Still skirting the granite, but now in a northerly direction, we come to the ‘‘ Caledonia Reef,’ on the southern or right-hand bank of the Kaap River. The rocks here are schists, shales, cherts, and quartzites, nearly vertical and striking N.N.W. by N. In one place, upon an isolated hill some 700 or 800 feet above the river, the reef was exposed. It is a seam of quartz, which may or may not be exactly in the bedding, in close contiguity to a large dyke of trap-rock. The “Caledonia Reef” apparently strikes with the strata, and is a vein of grey quartz, slightly honeycombed, the cavities generally filled with limonite and sometimes enclosing crystals of carbonate of copper and other minerals. The vein passes down vertically, varies trom 12 to 18 inches in width, and is auriferous throughout. Although this reef strikes almost, or quite, in the same direction as the schists, I am inclined to regard it as a true vein rather than as a seam or bed, because there are smaller veins, or “ leaders,” branching from it with a different direction; also because there is, on the west side, another reef of quartz, greatly resembling that of Moodie’s Reef and following a somewhat transverse direction. As both cannot coincide with the local strike, one, at least, must be a true vein; of the two, I think, for the reasons given, that one is the Caledonian reef. The other reef “gave a prospect of coarse gold upon being simply crushed and washed ” on the ground. e. Some 7 or 8 miles due north from the Caledonia Reef, the rocks on two other gold-bearing properties were found to “ consist _of siliceous beds so highly altered and contorted as to have been, in part, converted into jasper. Further east, and probably higher in the series, shales come in, then another series of hard grey schists ; the same strike, W.N.W., and the same vertical position being still maintained. These old stratified rocks are traversed by dykes of diorite and other plutonic rocks in various directions”*. Just west of Kaffir Spruit a seam has been opened of “ grey quartz, much stained by oxide of iron. This vein can be followed for a considerable distance, striking W.N.W.—it is almost vertical, but hades slightly to the eastward. It is 18 or 20 inches wide, and carries gold, as tested, in the proportion of 2 oz. 1 dwt. 1 gr. to the ton of 2240 lbs. Two other trials of the same stone gave a mean yield of 1 oz. 15 dwt. 14 grs. to the ton. “‘T'o the west of the above lode are some leaders of black quartz, which gave ‘good prospects’ of gold. On the east side of Kaffir Spruit is a vein of grey quartz, 18-24 inches wide, apparently a continuation of the above lode, being just in the line, and having the same width and direction tT”. This is evidently an interstratified seam, being coincident with the shales in dip and direction of strike. * The author’s Report, Noy. 1884. tT Report, Nov. 1884. Ley | LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA, 57: f. Several miles to the N.W., and still bordering the granite, we come to the so-called “‘ Welcome Reef,” on the south bank of the Lam- pongwana river, and 10 or 12 miles due east of De Kaap. Here the rocks are similar to those of the Caledonia reef, a soft talcose or steatitic foliated schist being also exposed—still vertical, but now striking N.W. The reef is a seam of quartz, apparently striking with the stratified rocks. The ‘** Welcome Reef” appears to follow the strike of the rocks, N.W., but this is not certain, and it dips somewhat into the hill on the west, whilst the strata, being here tilted by the granite, might be expected to dip, if at all, the other way; the evidence, however, is very obscure. The lode varies from 6 inches to 6 feet, and consists of white and tinted glassy quartz, containing much earthy carbonate of copper and oxide of iron, with occasional specks of visible gold. Some veinstone, taken at a depth of 15 feet, yielded gold at the rate of loz. 4dwt. 21 grs. per ton. All stone having been rejected in which the metal could be seen, it will be within reasonable bounds to assume an average of between 17 and 14 oz. per ton. The above observations extend about two thirds around the cen- tral boss of granite, and show that thus far the strike of the stratified rocks coincides with its margin, varying, as it does, from S. of E., through N.E. and N.N.W.to W.N.W. This affords ample evidence that their upheaval into a vertical position is due to the intrusion of the granite. Along the western side of the granite the same phenomenon is evident, although not so clear, owing to slips and accumulations of talus under the high krantz; but the edges of vertical rocks may be occasionally seen, striking in a generally northerly direction. JI think there can be but little doubt, if any, that the Kaap Mountains and the Godwaan Plateau nearly coincide with the margin of the granite. The north-westerly strike, which was the last observed, appears to be continued, but rather more westerly, beneath the Godwaan Plateau, as vertical schistose rocks, with W.N.W. strike, are seen in the bottom of the Eland’s Spruit valley. Between those points there is a ridge or spur jutting out from the “ berg” a little N. of De Kaap, in an E.N.E. direction. The beds forming this ridge are quartzose foliated schists, of a peculiar character and different from anything I have seen elsewhere. The strike of the beds coincides with the ridge, W.S.W., and they dip very sharply to the N., in- deed are almost vertical. To the north of the ridge the granite again comes to the surface, and, as stated before, widens out towards the Krokodil River, and then passes in under a series of rocks newer than those above briefly described. It probably forms the low country ‘‘ below the berg,” or rather perhaps the flank of the mountains to the north, and sweeps round by the Olifant’s River,— at any rate granite has been observed far away to the northward. “Beyond the Limpopo both Jeppe’s and Baines’s maps indicate ‘Granite’ up the Bubye River, and the latter portrays a ‘ high Q.J.G.8. No. 164. 28 ee ee ee is Eee —— 576 W. H. PENNING ON THE GOLDFIELDS OF granitic range’ running in a N.E. direction from lat. 20° 30’ to WicsaQs en 5. Devonian? Rocks.—After the rocks which I have referred to as Silurian had been tilted into their present vertical position by the upheaval of the central mass of granite of the Kaap Valley, they were cut down to a “ plain of (probably) marine denudation.” This old plain is at an elevation of 1700 or 1800 feet above the present general level of the Kaap Valley, which has, of course, been much more recently excavated. Upon the upturned and denuded edges of the Silurian rocks, those which I here provisionally term ‘“‘ Devonian” were deposited. (The “ Megaliesberg Beds” of my paper on the Coalfield, Q. J. G. 8. vol. xl. p. 660.) At the base of these Devonian rocks is frequently seen a series of conglomerates and sandstones (with some shales), which is fairly well exposed about De Kaap, “ formed from the waste of the under- lying Silurian beds, and of any quartz veins that they may have enclosed” 7. The Kaap sandstones are highly erystalline, some coarse, others fine in texture, in thick beds which have weathered into massive tabular blocks, which impress a peculiar distinctive cha- racter upon the appearance of the country. These sandstones and conglomerates thin out to the north, as the immense series of shales (with occasional sandstones), by which they are overlain, rests directly upon the granite on the other side of the Krokodil River. At De Kaap they afford additional evidence that rich gold-lodes exist below them, or at no great distance, in the Silurian rocks from which they were derived ; for they are frequently auriferous, containing not only fine gold but nuggets, especially the conglomerates. An analogous case, but of course one of recent date, is the occurrence of fine gold in the sand of the sea-shore (and probably, of course, gold in the gravels) upon the west coast of New Zealand. Above the sandstones comes a very large series of shales and flag- stones, fissile and thin-bedded, which generally are grey, but weather to yellow or dirty yellow or dirty brown. In some localities, as along the valley of the Eland’s Spruit, there occurs a series of cherts and quartzites, which appear to replace the lower shales. High up in the shales, but not by any means near the top of them, are two or more series of a peculiar, blue, fine-grained, calcareo- siliceous rock, to which Mr. A. C. Cruttwell and myself have given the name of “ chalcedolite.” We adopted this term in consequence of the chalcedonic texture frequently displayed—indeed, some por- tions of the rock are true chalcedony. Sometimes it occurs in amorphous masses, weathered to a grey colour, and to a peculiar, rough, trachyte-like surface ; but mostly in thin beds, 2 or 3 inches in thickness, with earthy partings, the lines of lamination being wavy and indistinct, except where exposed by weathering. The rock appears to be the result of intermittent deposition, probably * Guide to the Goldfields, p. 62. + Report, Dec. 1884. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. O77 in an inland sea, from water holding much silica and some lime in solution. The chief exposure of these chalcedolites is along the Blyde-river valley, best seen on its western side or escarpment, where the rock occurs in two series, the lower several hundred feet in thickness, with shales above, below, and between. It contains fine gold in places, and, where in a decomposed state, it has been worked as so- called ‘‘ rotten-reef” to a considerable extent. There are numerous old workings in it, following fissure-veins or old weathered crevices, frequently on an extensive scale, as in Rotunda Creek, which opens to the Blyde River, and again a few miles to the west of Pretoria. Still higher up in the shales, there are series of sandstones, some compact and very highly metamorphosed, others more coarsely crystalline, and resembling those of De Kaap. These and the asso- ciatad conglomerates are sometimes found to be auriferous. These Devonian rocks moreover are traversed by dykes of diorite and other trap rocks ; and immediately upon them, with an uncon- formity not very strongly marked, but still probably representing an extended period, rest the ‘‘ High-Veldt Beds” *. 6. Sections and Auriferous Deposits, a'—q'.—The following are brief notes of sections, commencing on the south at De Kaap, and ending on the north in the Orighstad Valley :— a. At De Kaap “ the lowest rocks of this series are highly crys- talline sandstones and conglomerates....Immediately above the sandstones is a series of shales;” these are overlain by another series of sandstones on the higher ground to the west, succeeded by more shales which pass in under, or are replaced by, the cherts and quartzites of the Eland’s-Spruit Valley. The conglomerates here, and in a less degree the sandstones, are auriferous (see above, p. 576). The shales above the sandstones enclose veins of auriferous quartz, one of which yielded gold at the rate of upwards of an ounce to the tony. 6!—The Godwaan Plateau is on the upper of the two series of sandstones, which are exposed to a considerable depth in many natural sections, such as krantzes and caves, as well as in the mines. Shales occupy the surface, sloping down towards Eland’s- Spruit Valley; both these and the sandstones are crossed by quartz reefs and dykes of diorite. There are several “‘ reefs” on this plateau, some of them being very richin gold. (1) The ‘‘ Homeward-Bound Reef,” which, so far as opened, isa vein of soft saccharoid quartz, with some hard quartz, much earthy matter, and oxide of iron, several feet in width, striking N. and §., and enclosed in fairly well-defined walls. The lode, héwever, is much split up, and, as it were, spread out near the surface, becoming more compact and regular below. I have no data for estimating the yield of gold from this lode, which is certainly rich, for some hundreds of ounces are obtained every week by small machinery. The gold is remarkably fine, like flour, and requires, * Quart. Journ. Geol. Soc. vol. xl. (1884), p. as t Report, Dec. 1884, 282 —— 578 W. H. PENNING ON THE GOLDFIELDS OF therefore, great care in manipulation. There is a casing of grey, honeycombed quartz, several inches thick, on the west side of the lode, which contains silver. I have made no assay of this, but was informed that Messrs. Johnson and Matthey had certified 16 oz. to the ton. (2) Three or four hundred yards to the east is “ Rautenbach’s Reef,” a mass of soft, earthy, auriferous ground, which appears to occupy nearly the whole of the ridge parallel to that of the ‘ Home- ward Bound Reef.” There are in it, however, numerous quartz strings, dipping from either hand towards a central line, and seeming to indicate a downward extension of the lode in a more restricted form. Some spots are very rich in fine gold, others poor and even barren, the metal not being at all equally distributed. - Since my last visit to this place, I have received a letter, dated 13 Dec., 1884, from which the following is a short extract :—‘“ In continuing the large cutting....I have come on a very large lode of rich quartz ; it is about 13 feet wide, and runs to all appearance due E.; it seems to branch out from the Homeward Bound Reef. I have taken out of it to-day about 60 tons, and it is very easily worked.” There are other auriferous reefs on the plateau, some rich in gold, but only the above are yet opened to any extent. c’. About 14 miles to the westward of the Godwaan Plateau, I have examined a block of farms on the table-land between Eland’s Spruit and the Krokodil River, finding the rocks to be :—‘‘ Sandstones on the higher ground....resting upon grey thin-bedded shales, which, in turn, rest upon a series of beds of chert, quartzite, and arenaceous shales ” *. | Upon the block of farms between Eland’s Spruit and the Kro- kodil River I traced the outcrop of several quartz-reefs ; these have not been opened up, but the surface-specimens yielded gold in pro- mising quantity. About 10 miles still further west the main road from Natal passes down a very steep hill into the Krokodil Valley, and shales are exposed from top to bottom of the descent, except where intersected by some large diorite dykes. About thirty miles further down the valley, and on the opposite side of the Krokodil River, the road from Spitzkop also comes down a very steep incline. This shows shales in its upper portion, which, part way down the hill, rest directly upon the granite of the Kaap Valley. re head of the Stadt’s River, which about here joins the Krokodil, I went over a farm, finding it to consist of shales, except on the highest ground to the N.W., which is sandstone. The whole country from here to Lydenburg is nearly all shale, with sandstone on the higher ridges. d'. Around Lydenburg the rocks consist principally of a series of shales, several hundred feet in thickness, with occasional beds of sandstone, dipping to the westward. .On the Lydenburg town- lands “a reef of quartz, 2 feet in width, crops out along the top of * Report, March 1884. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. 579 the ridge on the west side of the Dorps River, striking N.N.E., and having an easterly dip of about 80°. This reef is in a diorite dyke, to the depth already proved of over 50 feet, and will yield gold at the rate of 9 dwt. to the ton*. .... The shales and sandstones are highly metamorphosed throughout, but especially so where in contiguity to the numerous dykes of diorite and other plutonic rocks by which they are traversed in various directions. As a rule, such dykes are more or less vertical in relation to the strata through which they pass; but there are several on the town-lands that almost if not quite coincide with the stratification.” Six miles north of the town the Pilgrim’s-Rest road winds down a steep hill to the “ drift” across the Spackboom River. The road- cutting exposes grey shales all the way down, except where they are broken through and locally displaced by a diorite dyke, which the section shows plainly in the various stages of concentric weather- ing. The shales below the dyke are black, like slate in appearance and composition, but without any sign of cleavage. (The absence of true slate is somewhat remarkable. I have not yet seen it in any part of South Africa.) é’. From Lydenburg the country and the beds rise to the east- ward with a long “ dip-slope,” and a few miles in that direction hes the “‘ Paarde-Plaatz,” or Horse-farm, belonging to the town. ‘‘ The rocks of Paarde-Plaatz are altered shales on the western margin, which overlie a series of crystalline false-bedded sandstones that crop out along the edge of the mountain, and form the higher grounds in the centre and on the east side of the farm. These sandstones, in turn, rest upon another series of shales that occupy the lower grounds, and stretch away to the eastward” Tf. ‘There are numerous seams of quartz, varying from 2 to 18 inches in thickness, inter- stratified with these sandstones and lower shales, and these will be referred to presently, as they are rich auriferous deposits. There are also vertical veins of quartz which contain gold. Paarde-Plaatz.cIn June last year, when examining this ground, I picked up a loose piece of crystalline quartz, very promising in appearance, and in such a position that it must have come from a reef within ashort distance. It yielded gold at the rate of upwards of 5 oz. to the ton. There was no sign of the outcrop of a true lode, so trenches were cut under my direction, and by this means the source of the loose lumps of quartz was discovered. It proved to be a flat seam of red-brown crystalline quartz, perfectly interstra- tified with the bedded rocks. Numerous other auriferous quartz- seams coincident with the stratification were afterwards opened a few feet apart in the shales and sandstones. These seams extend over a considerable area, and vary in thickness from 13 to 18 inches, and in yield of gold(some barren) from 9 dwt. 1 gr. to 6 oz. 17 dwt. 10 gr. per ton. The average of fourteen assays of stone from these flat seams, and calculated upon their various thicknesses, is 3 oz. 6 dwt. 16 gr. per ton. * For this and neighbouring reefs see the author’s Report, Dec. 1884. + Report, Sept. 1884. 580 W. H. PENNING ON THE GOLDFIELDS OF There are also auriferous lodes here, transverse to the bedding ; one “a nearly vertical reef, consisting of alternate quartz and are- naceous streaks, much decomposed, but presenting the general ap- pearance of a fissure-vein. This lode varies in width from a few inches to several feet, is locally irregular, but upon the whole follows a well-defined course for several hundred yards along: the face of the krantz.... The stone yields gold at the rate of 18 dwt. 16 gr. to the ton”’*. f'. Still further east is “‘ Mount Joker,” where the rocks “ consist principally of crystalline false-bedded sandstones overlying a series of shales, which, in turn, rest upon another set of similar sand- stones. In the sandstones shales also occur as well as conglo- merates, and frequent seams of quartz, some of which, where tested, have been found auriferous” +. ‘‘ Upon Mount Joker a seam of quartz crops out, or it may be ‘two or more seams, as the rugged nature of the ground renders it difficult to trace the line from one prospecting hole to another. The quartz is bluish-white, much broken up at the outcrop, and contains much oxide of iron and some oxide of manganese. It occurs interstrati- fied between an altered shale (almost a schist) below, and sandstone, also highly altered, above. At the base of the sandstone there is generally a coarse auriferous conglomerate, resting directly upon the quartz, and varying from 6 to 15 inches in thickness. The quartz also varies in its thickness from 2 to 9 inches, the average being about 5 inches.” The yield of gold varied from 5 dwt. to 4 oz. 18 dwt. per ton, ‘equal to an average on this seam (or these seams) of very nearly 1 oz. 7 dwt. to the ton” t. g'. On the south of Mount Joker is the farm ‘“‘ De Kuilen,” where the beds are similar to those at the lower levels of that mountain, viz. shales, sandstones, and shales, with a westerly dip of from 5° to 7°. From here all along the Spitzkop road only shales are seen, with the exception of intrusive dykes, until near Ross Hill, a few miles west of the Spitzkop mountain. On De Kuilen “a quartz reef can be traced from the head of the small gully, under the marshy ground by the road, rising again beyond the flat.” Its yield is estimated at little less than an ounce to the ton. Just beyond where the road passes down a steep incline a quartz-reef occurs, with an estimated yield of not less than 1 oz. of gold to the ton §. rn’. About Ross Hill the rocks become siliceous im character. Sandstones, cherts, and quartzites, previously seen in the deeper valleys, now come to the surface. Here also chalcedolites are seen, but not in great force. The mines of Ross Hill are partly in “rotten-reef” and partly in diorite. I have no definite data respecting the gold-veins here, but they must be rich, as three diggers, after working upon them for about two years, took away 6000 ounces of gold, chiefly derived, I believe, from quartz-leaders in the “rotten-reef.” I have seen fine specimens of gold in quartz from these mines. * Report, Sept. 1884. — t Report, Jan. 1885. t Report, Jan. 1885. § Report, Feb. 1884. ee LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. 581 7. South of the Spitzkop mountain is ‘“‘ Grey’s Creek,” near the mouth of which is an old heading, driven 60 feet into the hill. This shows a seam of quartz from 1 foot to 2 feet thick, between decomposed chalcedolite above and brown sand (? decomposed dio- rite) below. These beds dip W. at an angle of 5°, and underlie the shales that form the high ground on the west. The quartz seam here, interstratified with the beds, varies (where opened) from 1 foot to 2 feet in thickness, and yields an average of 3 oz. 12 dwt. of gold to the ton. j. Upon the farm called ‘‘Spitzkop,” north of the mountain of that name, are numerous cuttings made by the miners, nearly all in shales and flagstones. Towards the east side, however, the more siliceous beds come in, and where exposed in some open mines, they are much decomposed, especially the lower few feet resting upon the saddle of a decomposed diorite dyke. On the east side of the farm the so-called “ rotten-reef” has been rather exten- sively worked in two claims, where it rests upon the saddle-back of a decomposed diorite dyke. The numerous quartz-leaders in the shales ‘“‘vary even in a few feet from 3 inches to 3 inch in width ; they vary slightly also in dip and direction. Their average width may be taken as 14 inch; their general dip 8. 50° to 55°; and general direction E.to W. ‘The direction of the dyke being W.N.W., the leaders strike it at an angle of about 20 degrees.” In the shales are very many thin veins of quartz, more or less vertical, which, in the lower 3 to 5 feet, are broken up and indis- criminately mixed with the matrix, thus forming a so-called “ rotten- reef.” This term is also applied to the several feet of strata exposed above, although less decomposed. Fig. 2.—Sectron of “ Rotten-Reef,” Spitzkop. Shaft, 25 ft. deep. a. Tilted shales. 6. Diorite Dyke. c. The “ rich layer.” The section, fig. 2, shows a shaft 25 feet deep down to the dyke, along which a drive has been made 35 feet to the N.N.W., following the downward dip of the “rich layer,” here consisting of 3 feet of “ rotten-reef,” with from 1 to 2 feet of poorer ““wash” between it and the dyke. The shaft is sunk through contorted and partly decom- posed shales, with auriferous quartz-leaders. 582 W. H. PENNING ON THE GOLDFIELDS OF Three assays made gave :— No. 1. Quartz, with oxides of iron and manganese, 1 oz. 10 dwt. 11 gr. of gold to the ton of 2000 lb. No. 2. 302. 6 dwt. 16 gr. of gold to the ton of 2000 Ib. No. 38. 9 dwt. 2 gr. of gold to the ton of 2000 lb. An open section at Spitzkop shows the upper part, consisting of soft shales, contorted by the irruption of the dyke from below (as in fig. 3), with quartz leaders averaging about six feet apart. Between the shales and the dyke occurs the “rich layer” of black decomposd shale, traversed irregularly in every direction by broken-up veins of quartz. Of this layer, 5 feet thick and conformable to the dyke below, the upper 3 feet are very rich ; it dips N. by. E. into the hill at an angle of 10°. Average samples were taken from this layer by picking down through its whole thickness in several places. The relative proportions by weight were 27 oz. of decomposed shale and oxide of iron to 1 oz. of quartz. Upon assay, the average sample of the rotten-reef was found to yield 16 dwt. 5 gr. of gold to the ton (2000 Ib.). Other neighbouring sections of ‘rotten-reef,’ shales, quartz- leaders, and “ pay-dirt,”’ are described in the author’s Report, July 1883. ‘Some shafts are sunk through what appears to be an interstratified mass of decomposed diorite; if so, it is an intrusion, probably from the main dyke, as the shales are seen dipping under it from either side, and disclose beneath it 2 feet of very rich ‘ pay- dirt’ ” One of these shows :— 3 feet surface-soil. 2 ,, rich “ pay-dirt.” 6 ,, decomposed diorite. 16 ,, partly decomposed shales with six leaders passed through, the lowest one nearly horizontal. A similar belt of rocks occurs from Spitzkop down to the Sabie River, where the fine falls by the roadside are slowly cutting their way back in a mass of sandstone, in which their waters have already formed a ravine many hundred yards in length. Thence to the ““Mac Mac diggings” similar rocks prevail, indeed all along the - level plateau which borders the low country. k'. The farms “ Lisbon ” and “ Berlyn,” formerly called “ Water- fall,” are situated on this plateau, and are now being worked by a gold-mining company. The rocks here are shales, occasionally arenaceous; on the east side are crystalline sandstones, faulted against the shales*. Some of the hills around are capped with chalcedolite. The shales are nearly horizontal, and are intersected at frequent intervals by veins of quartz, varying from 2 to 6 inches in thickness, and dipping at a high angle. These thin veins are auriferous, and appear to be “leaders ” from the main quartz-reefs, which run in a nearly N. and S. direction across the property. * See Geol. Mag., April 1885, p. 171. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. 583 The gold lodes consist of main quartz-reefs and transverse leaders ; “These leaders are thin (a few inches only in thickness), and consist partly of white quartz, partly of oxide of iron and man- ganese. Two of them sometimes merge into one, and occasionally two or more unite to form a main lode close to or in contact with the dyke. Almost without exception the gold-mines of this district are in such leaders in proximity to diorite dykes.” An average yield of 4 oz. of gold to 2000 Ib. of quartz was the estimated result of several examinations. Several main and branch dykes of diorite are traceable for long distances, and in some instances are well exposed in the open mines. In two cases the shales are sharply tilted by the dykes on the west Fig. 3.—NSection of Diorite Dyke, Lisbon-Berlyn. W. oe es rs BYTE TTAB CUT TAT (Dn eee a. Tilted shale. 6. Dyke. side, and in one on the east they are slightly contorted on the other side. In the section the weathering leaves hard kernels of blue diorite with concentric rings, semidecomposed, shading off into the soft brown mass, which otherwise resembles an alluvial loam.., l'. A few miles S.W. of Waterfall are the farms about ‘‘ Pilgrim’s Rest,” belonging to the Transvaal Gold-Land-and-Exploration Company. The rocks here are higher in the series and are more siliceous in character, the lower main mass of chalcedolites being in considerable force. Their chief outcrop, however, is along the west side of the Blyde River. Here, also, are many diorite dykes, one of which, a small branch dyke in Pilgrim’s-Rest Creek, has tilted the adjacent beds inversely to the usual position. With the exception of the rich alluvial deposits in the creek, the ground chiefly worked here for gold has been the “ rotten-reef,” similar to those previously described. The chief of these are at Brown’s Hill and Ophir Hill; but I have no data upon which to base an opinion as to their value, which is regarded as high. Crossing the Blyde and mounting the steep escarpment to the west, we find shales cropping out from top to bottom, with the ex- ception of the upper of the two main series of chalcedolites inter- vening part way up the hill. The shales have generally a small westerly dip, but are locally thrown to high angles and into various positions by plutonic dykes. The chalcedolites are much decom- posed, and-a bed of quartz, at least one foot in thickness, is seen amongst them. On the summit of the hill is a series of crystalline sandstones. ee aa CO Oe eee 584 W. H. PENNING ON THE GOLDFIELDS OF m'. Just south of the road passing up the escarpment is a piece of ground called “ Peach Tree,” nearly all on shales, but also with sandstones on the top of the hill. There is on the table-land a highly ferruginous bed, which has been worked by the natives for iron. The shales are intersected by plutonic dykes and by two nearly vertical quartz-reefs, about 12 inches wide, which strike nearly N.E., and yield gold at the rate of upwards of an ounce to the ton. n'. Following the upper series of chalcedolites a few miles north, we come to “ Rotunda Creek,” which affords sections at intervals from the top of the hill to the Blyde River; and here we find the rocks following the usual order of the escarpment. Rotten-reefs, containing fine gold, have been worked here. ‘There is also a large main reef, consisting almost entirely of coarse crystals of quartz, and very ferruginous; it is at least 4 feet wide, and yields coarse gold, upon the average not less than 4 oz. to the ton. o'. Still further north, “ Kaspar’s Neck” is on shales and quartz- ites. The lower series of chalcedolites crops out on the east; the upper series in the small valley on the west. p'. The small stream west of Kaspar’s Neck joins the Orighstad River; and in that valley, a few miles above the junction, the rocks are, In ascending order, quartzites and cherts, crystalline sand- stones, shales, conglomerates, shales, quartzites, and cherts, all dip- ping W. ata low angle. In the Orighstad Valley are some highly crystalline sandstones, 40 feet or more in thickness, which yield gold several pennyweights to the ton, as do also the conglomerate beds associated with them. g'. Towards the head of the Orighstad Valley the rocks are chiefly shales with sandstones, having a well-defined conglomerate at their base, on the hills and ridges. From this point back to Lydenburg the surface is occupied by shales, sometimes arenaceous, which extend almost without intermission to the High Veldt, where they pass beneath the coal-bearing formation. About the head of the Origh- stad Valley there are many quartz-reefs, one of which, over 2 feet in width, strikes almost E. for Pilgrim’s Rest, and carries gold in the proportion of more than an ounce to the ton. About the Speckboom River, near the “ drifts,” are numerous thin veins of quartz, some in diorite, others in shale, all of which, so far as examined, contain more or less gold. § 3. Attuvrat Avrirerovs Deposits. In the Lydenburg goldfields some few patches of very rich allu- vial deposits are known; but, considering the great extent of the gold- bearing area, and the quality of the reefs in some places, it is remarkable that no large alluvial field, like those of Australia and California, has yet been discovered. Two years since, when writing of the Kaap goldfields*, I offered some observations on the river- * Guide to the Goldfields, pp. 51, 57. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. 585 valleys and alluvia, and the probable occurrence of gold in those that came from rich quartz-reefs. Alluvial gold has since been discovered about James Town on the Lampongwana, or Northern Kaap River, and near other streams in the Kaap Valley; still the area of payable ground, as far as thus known, is not sufficiently extensive to support a large digging popu- lation. A few of the chief alluvial deposits may be noticed in the same order as the more permanent lodes have been. e. KaffirSpruit (p. 574).—There is a large quantity of loam, gravel, and similar alluvial deposits, along the margin of the river and spruit, as also in their tributary valleys*. Imay add that extensive diggings have been carried on during the last two years, near James Town, with a fair measure of success, in the Lampongwana River. A digger has secured rights to a large quantity of water (15 heads) from the river above; and as he proposes to bring it to his ground by cutting a race from 15 to 18 miles in length, it is evident that he has found the deposits rich enough to warrant such an undertaking. In several places along the Kaap rivers, and even up to their sources about the mountains on the west, good alluvial gold has been found. a’. De Kaap (p. 577).—* In all the creeks good alluvial gold has been found ”—at one point in the Kantoor creek “ the numerous , large nuggets for which the first ‘ rush’ to the Kaap was celebrated ” —at another, “ several claims were worked with wonderfully good returns.” At a spotsouth-west of the Kantoor “ there is a very rich alluvial, yielding a small proportion of reef-gold from the vein just above ... and large quantities of waterworn gold from the waste of the conglomerates.” Work is being carried on in alluvial wash, and from the fact of a long race and a dam having been recently con- structed to bring on the water, it may be assumed with very good returns7. b'. Godwaan Plateau (p. 577), “ Barrett's Rush.”—About six miles north of the Kantoor is one of the small depressions, falling in a westerly direction, where nuggets were found, just where the road crosses the hollow. The ground here is almost bare sandstone, covered with a few inches only of soil, in which, and amongst the grass roots, the nuggets were discovered. “ Poverty Creek.” In the main or northern branch of Poverty Creek, some good gold has been found. . . There has been more alluvial ground worked here, in better form and to better advantage, than anywhere else on the plateau. There are two distinct kinds of gold found at this spot, the position of each kind being clearly defined. From this fact and other circumstances it seems probable that two lodes here cross each other or effect a junction” t. “ Willey’s Creck.”—Many nuggets were found here; one that I saw weighed just under a pound. * See Report, Nov. 1884. Tt Report, Dec. 1884. { Guide to the Goldfields, p. 55. t| \ i | 586 W. H. PENNING ON THE GOLDFIELDS OF d'. Lydenburg (p. 578).—At a point on the Dorps River; about half a mile south of the town, good coarse gold has been taken from the gravel bordering the stream; and a large piece was found in gravel along the stream that comes in from the §.E. and near this point joins the Dorps River. “ The alluvial deposits around the town are exten- sive, as well as of considerable depth and richness. The upper part of these deposits consists, in places, of a hard ferruginous ‘ cement- stone,’ or fine gravel cemented by oxide of iron, and containing gold. Beneath this there are several feet of sand and loam, also auriferous, and at the base is an extensive bed of coarse gravel and pebbles, which, wherever it has been tried, has yielded coarse gold, in some places even in payable quantity ’”*. h’. At Ross Hill (p. 580), as would naturally be expected, the alluvial soil is rich in fine gold. vu. Grey’s Creck (p. 581) opens into the same valley as the small stream from Ross Hill, and here both coarse and fine gold occur. On the east side of the creek is a mass of broken quartz in a black sandy soil (apparently the shedding from the contiguous quartz veins in chalcedolite), which is auriferous. Further down the stream good coarse gold occurs in the alluvium. j.. Spitzkop (p. 581).—On the east side of this farm a claim “ has been worked down about 15 feet on to the bed-rock, which here con- sists of shale. At this point there is also an old channel beneath the alluvial ground, which is brown loam, and has hitherto proved rich in gold. ‘The loam carries a small proportion of fine gold throughout, but is, of course, much richer just above the bed-rock ; in the old channel especially it has proved very rich, 57 ounces of gold having been taken out (as I am informed) from one paddock, about 36 feet by 45 feet, after three weeks’ ground-sluicing”’ f. ; k'. Berlyn-Lisbon ( Waterfall) (p. 582).—The surface of the ground upon and west of Howse’s claims, and for some distance to the north and south, is occupied by a terrace of sandy loam. On the opposite side of the river is another terrace, which extends a long distance S., on the west side of a stream; and there is another large patch, bordering another stream that flows into the river east of the Falls. *“‘ All this alluvial yields gold”, and is now being removed by hydraulic appliances. U. Pilgrim’s-Rest Creek (p. 583) is occupied from end to end by a mass of coarse gravel and fine loam, the gold from which at one time supported many hundred diggers. The creek is very steep and narrow, and is but three miles or so in length; its containing so much water-worn gold is therefore good evidence of the existence of rich lodes in the immediate vicinity. m'. Peach Tree (p. 584).—Good alluvial ground has been worked in the creek, also upon Columbia Hill, where long races were cut merely for the purpose of sluicing away the surface soil, to the depth of about a foot, for the sake of its gold. * Report, Dec. 1884. Tt Report, July 1883. t Report, May 1883. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. 587 n'. Rotunda Creek (p. 584).—The alluvial ground has been worked, although not to any great extent *. q'. Orighstad Valley (p. 584).—Upon the farm “ Klipheuvel” there is a “large body of alluvial wash, which covers the part of the farm bordering the stream ” 7. Good alluvial wash has also been found on the farm *“ Nauwpoort,” a few miles nearer to the head of the valley. Terraces.—The above notes refer to the alluvial deposits in the bottoms and on the immediate margins of the valleys; but in many instances the terrace-gravels, which are relics of an earlier stage of denudation, are also gold-bearing. In Willey’s Creek (6') and at Pilgrim’s-Rest Creek (7) are high terraces of rich alluvial wash. I have also observed patches of river-gravel at least 800 feet above the present Speckboom River; but these, so far as I am aware, have not yet been proved auriferous. § 4. Gotp anp Nueeets. The character of the gold obtained from these fields in the Transvaal varies almost with every locality, whether from the reefs. or from the alluvium. Some of the reefs in the Kaap Valley (a—f) carry coarse, others fine gold. At De Kaap (a’) the gold is fine in the reefs and coarse in the conglomerates ; on the Godwaan Plateau (6') the reef-gold is very fine. Near Lydenburg (d') the reets produce generally rather coarse gold, although some on Paarde- Plaatz (e') is very fine. At Ross Hill (%') and Spitzkop (/’) there are large specimens, but the bulk of the gold is very fine; at Lisbon-Berlyn (k') itis coarse, as a rule, with occasional nuggets and some fine gold. Pilgrim’s Rest (7) produces fine, and Rotunda Creek (n') coarse gold. In some cases, as at Spitzkop, Pilgrim’s Rest, and Ross Hill, the gold is very fine indeed, like flour, of which the grains can scarcely be distinguished even with a lens. This very fine flour-gold seems to be confined to the “ rotten- reefs ;” the moderately fine to the flat quartz seams; and the coarse to vertical reefs or true lodes. The gold from the alluvium in the Kaap Valley, as at Kaffir Spruit (e), is mostly ‘‘ scaly” (in small flat pieces), rather pale in colour, not very much waterworn, and with occasional nuggets. At De Kaap (a’) it is mostly coarse rich gold, extremely waterworn, having been subjected at least twice to alluvial action-—first into the old conglomerates, then from them into the recent deposits. Upon the Godwaan Plateau (4’), there is fine as well as coarse gold in the alluvium, the wash having been partly derived from the reefs that carry fine gold. At Lydenburg (d’) the wash yields gold of a rather light colour, in scales and grains; about Spitzkop (f’, 7’, 7) _ the gold is of good quality, fine in the wash on the higher lands, and coarse below. At Lisbon-Berlyn (X') it occurs in a similar manner; and at Pilgrim’s Rest (/') the gold is very rich, coarse, and with nuggets in abundance. * See the ‘ Guide to the Goldfields,’ pp. 17, 18. t ‘Report,’ May 1884. 588 W. H. PENNING ON THE GOLDFIELDS OF The following may be given as examples of the occasional rich “ finds ” in these fields :— In 1873, at New Caledonia, four large nuggets with a number of smaller ones, collectively weighing 13 Ib. 8 oz. In 1874, at Barrington’s claim, a nugget weighing upwards of 87 ounces. : In the same year, nuggets of 48 ounces and 69 ounces were found. In 1875, at head of Creek, Pilgrim’s Rest, one of 8 pounds and another of 57 ounces. In the same year were found nuggets of 213, 69, 294, 57, and 47 ounces, A nugget of 123 ounces was found in a terrace-claim, Upper Creek, at about 30 feet below the surface *. § 5. Orner Metats anp MInERALs, A few other metals and their ores observed in this district are :— Godwaan Plateau (b').—Silver inthe Homeward-Bound Reef. Here, and also at De Kaap (a’), pieces of metal, soft and white, but oxidized on the outside and generally resembling lead in appearance, are frequently found in the gold-washing sluice-boxes of the diggers. I have tested some of these pieces from both places and found them to be zinc. If my tests be supported by others at home, the existence of native zine will be confirmed. Paarde Plaatz (e').—In the auriferous quartz seams here the metal platinum occurs, certainly not in large quantity, but fairly constant, in connexion with the gold. Lydenburg (d').—Good copper-ores, sulphide and carbonate, have been worked here; near the town on the north side, there are extensive old workings, now overgrown; others also are seen near the Speckboom River. Rotunda Creek (n').—There is rich copper-ore here, both car- bonate and black oxide: and grains of native copper have been found in the alluvial gold-washing operations. Kaap Valley, Welcome Reef (f).—There is a large percentage of copper-ore in the quartz here; but no tests have been made of its value. . Argentiferous galena occurs between the goldfields and Pretoria. Iron in many forms, including hematite, is abundant in the Transvaal. § 6. Tae Diorrre Drxzs. Frequent mention has been made of the diorite dykes by which this region is traversed, and of the rocks being tilted and otherwise disturbed by their intrusion. There are other points in connexion with them also worthy of notice. Refractory as diorite is in its normal state, it disintegrates much more readily than the softer * See also ‘ Guide to the Goldfields,’ p. 8. LYDENBURG AND DE KAAP, TRANSVAAL, SOUTH AFRICA. 589 shales and sandstones through which it often passes ; and this fact gives rise to definite physical and surface-features. Very prominent objects in the immense plains of South Africa, as also indeed amongst the mountains, are the long narrow ridges of what at first sight would appear to be waterworn boulders, but which are really cores from the concentric weathering of diorite dykes. Beneath them the whole of the dyke is often entirely disintegrated into a soft but compact argillaceous mass, passing gradually down into hard unchanged diorite. I have seen a good iulustration of this where one of the head streams of the Krokodil River passes through a deep gorge, the almost vertical sides of which expose a good section of decomposed diorite, capped by a mass of rounded cores that spread out beyond the walls of the dyke on either side to some distance. I think the rock weathers more rapidly below the surface; it gets washed away beneath the harder cores, which settle down and accumulate along the line, repre- senting probably several hundred feet of the dyke, gradually weathered and removed by denudation. When no line of cores has been left, which frequently happens on sloping ground, the course of a dyke may still be traced merely by changes in the vegetation: a greener tint in the grass—which is sometimes quite verdant, whilst that on the shales has been parched to a yellow or brown colour—by lines of bushes, by the growth of different kinds of plants, and so on. Single or parallel lines of dykes may sometimes be detected, even at a great distance. Where a dyke crosses a watershed from one valley to another, a tributary stream usually cuts its course along the weathered surface into each main valley until the two nearly meet at the watershed, leaving only a narrow “neck” or ‘“ pass” between. The rain-collecting area of such necks being reduced to a minimum, they are now subject, as ridges often hundreds of feet above the valleys below, to the least possible action of denudation. A good illustration of this phenomenon is the neck, about a hundred yards wide, at the head of two very deep gorges, one opening north, the other south, just east of the townlands of Lydenburg. On the road to Spitzkop there are four or five such necks (or weathered dykes) almost close together, being perhaps a hundred yards apart, many hundred feet above the ravines, and just wide enough for a waggon- road, with small rounded hills between them ; these are called the ** Devil’s Knuckles.” 590 ON THE GOLDFIELDS OF LYDENBURG AND DE KAAP, 8, AFRICA. Reerrs &e. Page a. Moodie’s Réel sso. 572 Bb! Aorvoti Reel 22e ee ee 573 e- Barber's Reek-2). 225s 573 d. Caledonia Reef ...:....-..5..-.6- 574 6. (Kaflir Spraitys 22.235. 2 BYE: f.. Welcome Reet .2. 1. hk ese 575 ws Deine ee 577 6’. Godwaan Plateau............... Bie 1. Homeward-Bound Reef 577 2. Rautenbach’s Reef ...... 578 c'. (Farms between LEland’s Spruit and Krokodil River) 57 de Ayydenburgi aS. to. he A 578 els Paartle-Blaaiz, {.5.22-csce.-sosece 579 F2) Mount doker a...) te 580 9). De Katlens. 2g... sesccsvoreesn 5 580 LS NO gs A cee ee cnnance 580 a’. Grey’s Creek (near Spitzkop I 5 Hi) eee eree aera Sian aae de 581 ot. SpuZkOp Parma. 622%. ess .ece 581 k'. Lisbon and Berlyn (Water- Ll) Ieee a 582 Z. (Near Pilgrim’s Rest) ......... 585 qs eae NETO 855 ele nes hate 584 n'. Rotunda Creek........:....-0++ 584 o'> Waspar's ‘Neck *..2.2-c=..2-n00 684 p'. Orighstad Valley ............... 584 g'. Head of Orighstad Valley ... 584 ALLUVIAL DEposits. Page e, Kaffir Spruit .....cccceseeeeee 585 gs De Kap swt essccn oor 585 6’. Godwaan Plateau............... 585 Poverby Creek) 20. 2st t 585 Willey’s:Creek 253. cascccc- a 585 d'. Lydenburg............. ereeeeenees 585 hs ROSS AA Teac ee cee ence 586 a's Grey's Greek 20 erecssaeeew 586 7’. Spitzkop Warm ... 0. s24--.5-2 586 k'. Berlyn and Lisbon (Water- cel ee ae se el ay et 586 l’. Pilgrim’s-Rest Creek ......... 586 a. Peach Weee 5 ih. SUR 586 m'. Rotunda Oreek ...........-..060- 586 p'. Orighstad Valley ............... 587 Discussion. Mr. C. Tuomas said that, having just returned from the country, he was able to state that the goldfield extends beyond the limits mentioned by the Author. It stretches into Swaziland, to the south and east of the district described. Mr. Baverman remarked that the occurrence of gold in small quartz-grains immediately associated with diorite masses, as repre- sented in the Author’s diagram, was a condition well known in the Ural, Australia, and elsewhere. ON THE ERRATICS IN THE BOULDER-CLAY OF CHESHIRE. o9l1 44, On some Errarics in the BountpEr-ctay of Cuxsuire, gc., and the Conprrions of Oxrrmate they denote. By Cuartes Rickerts, M.D., F.G.S. (Read May 27, 1885.) [Abridged.] Tue glacial phenomena in the valley of the Mersey indicate that, though during that period the country was entirely covered with ice and snow, these accumulations were no greater than were derived from the snowfall on the water-slopes of this and its tributary valleys. The glacier-striz on the surface of the Triassic rocks coincide in direction with those of the respective valleys, or they have a direct reference to the contour of the ground. Taking ‘‘ Happy Valley” (now Borough Road), Birkenhead, as a typical example, the bottoms of the valleys, where channels have been in pre-Glacial times, are filled to a limited height with irregularly stratified beds of sand and gravel, their presence in other valleys being revealed by excavations and borings for wells, &.* The sands have been derived from disintegration of the Trias; whilst the pebbles are similar to the erratics so abundant in the Boulder- clay, excepting that all traces of strie &c. have been removed, it is presumed, by water which, holding sand in suspension, issued from beneath glaciers. On these gravels &c. is situated Boulder- clay containing a much larger proportion of sand and pebbles than the Boulder-clay proper. The flanks of the valleys frequently have rock-surfaces covered with unstratified sands and angular fragments of sandstone, without intermixture of erratic pebbles ; they are considered to be moraine accumulations left by glaciers which extended into the sea. The whole is covered with Boulder- clay, a reddish-brown unstratified clay containing pebbles and boulders irregularly dispersed through it. Besides the accumulations of Triassic fragments already alluded to, others occur at from 125 to 150 feet above ordnance datum, which must have been formed above the then sea-level, and have resulted from the action of strictly local glaciers ; one was uncovered a few years ago at the Birkenhead School, and another occurs near the cemetery. The clay of the Boulder-clay may be attributed to the abrasion of adjacent rocks by glaciers, beneath which it issued in subglacier rivers highly charged with mud and sand. Such a condition occurs in Greenland, where the rocks are of granite or of equally in- destructible material; the quantity of sediment must therefore be immensely increased when the strata passed over are so easily disintegrated as the Trias and Coal-measures. The water being * «Buried Valley of the Mersey,” by T. Mellard Reade, C.H., F.G.S. (Proc. Liverpool Geol. Soc. 1872-78, p. 42). + “ Physics of Arctic Ice,” by Dr. Robert Brown, F.R.G.S. (Quart. Journ. Geol. Soc. vol. xxvi. p. 682). Q. dG. 8: No. 164 2T 592 C. RICKETTS ON THE ERRATICS IN THE thus surcharged with mud may account for the entire absence of marine life; fractured, rarely perfect, shells occur sparsely scattered in the clay, but never under such circumstances that it could be imagined they had lived where found. The pebbles and boulders imbedded in the clay, and from which the formation derives its name, consist of fragments of hard rock from the size of minute grains to two or three feet or more in diameter, such as may have been derived from lands encompassing the Bay of Liverpool and the adjoining portion of the Irish Sea— from Cumberland, the south-west of Scotland, the north and east of Ireland, andNorthWales. Their surfaces are very generally flattened, smoothed, and polished, and a large proportion are covered with striz, grooves, and scratches, universally acknowledged to have been caused by abrasion beneath glaciers. If it is conceded that they have dropped into the clay from floating ice, their number is such as would indicate that the whole bay was sufficiently packed with bergs and floes to prevent altogether the formation of waves *, and therefore, in the absence of other currents, no evidences of strati- fication are afforded. Amongst the erratics in the Boulder-clay may be included masses of unconsolidated sands and gravels, often alluded to by local geologists as “‘ pockets of sand,” &. The materials resemble accumu- lations already referred to as situated in the bottoms of valleys as a bed upon which the Boulder-clay reposes; their general shape is comparable to that of the section representing masses containing a remarkable collection of dark green blocks of disintegrated traps, unmixed with other boulders, exposed in 1878 during the con- struction of the Bootle Docks (fig. 1). These were imbedded in a Fig. 1.—Section in Bootle Docks, Liverpool. (Length about 28 feet.) PE eae = = = = SS A Le ee a a. Trias. b. Gravel. c. Boulder-clay. d. Masses containing disintegrated Trap. . light green sandy matrix, and formed accumulations which were very conspicuous, the colour being in marked contrast to that of the Boulder-clay ; their disintegration must have been due to the same * « However great the agitation of the sea may be in the open ocean, and though it may dash its waves with wild fury on the edge of the ice, within the ice-girdle it is undisturbed ” (‘New Lands within the Arctie Circle,’ by Lieut. Julius Payer: chap. i. § 23). In January 1881 the Mersey was covered with floating ice, or rather snow, for nearly its whole width; on the waves reaching the ice they terminated in a swell for a short space, whilst inside the surface was perfectly unmoved. BOULDER-CLAY OF CHESHIRE. 598 . causes as that of some boulders of granite and trap to be alluded to hereafter. When brick-making was in progress behind the Mission House in Borough Road, Birkenhead, several blocks (five or six) of sand and clay were exposed; they contained a few erratic pebbles as well as bands, an inch or so thick, of vegetable mould. In one the clayey and carbonaceous beds were doubled on themselves, being so bent at the flexure as to squeeze away the clay. In this case also the loose sand has fallen away and spread from the mass as it settled down in the Boulder-clay. One piece exhibited spots of carbonaceous matter, which are probably the, rootlets of plants ; these are the only examples of vegetable life met with in the Boulder-clay*. Being in close proximity to each other, they pro- bably all dropped from the same iceberg stranded at this spot. The only locality affording evidence of vegetation, in situ, during the Glacial Period is at Leighton Hall, Yealand, Lancashire ; it occurs as a band, ten or twelve inches thick, of Carboniferous-Limestone pebbles, each of which is covered with an intensely black car- bonaceous powder ; this bed separates a lower from an upper por- tion of an accumulation forming a moraine mound, and indicates the recession, for a series of years, of the glacier by which the mound was formed. Blocks of the Boulder-clay itself, which would escape notice should they occur in the Boulder-clay proper, in consequence of its identity with them, have been frequently observed in those stratified sands and gravels, previously referred to, which cover the bottoms of preglacial valleys such as Happy Valley (fig. 2); similar blocks Fig. 2.—Section in Happy Valley, Birkenhead. (Height 10 feet.) a a, Trias. 6. Sand. c. Gravel. d. Boulder-clay. é. Blocks of Boulder-clay in gravel and sand. _ * Mr. D. Mackintosh, F.G.S., found plant-remains in the Boulder-clay near Crewe; and Mr. T. Ward of Northwich presented me with a fragment of wood obtained at a depth of 35 feet in undisturbed Boulder-clay. 27 2 | { | 594 C. RICKETTS ON THE ERRATICS IN THE also occur in the sandy Boulder-clay which immediately overlies these sands and gravels. Mr. A. Strahan, F.G.S., of H.M. Geolo- gical Survey, informs me that he has observed them under similar conditions in other places. It is more particularly desired to direct attention to the occurrence of other boulders which frequently bear evidence of glacier-action, and have also been exposed to other influences before they were floated away and dropped into the clay. Some, of granite, are weathered all over, their entire surface beirg roughened and so far disintegrated that fragments can be broken off by the fingers *; others in the same state have also had a portion split off. Some, having ‘their surfaces glaciated, crumble into fragments by slight pressure ; whilst others cannot be removed without separating into their component crystalline particles, though when in situ each granule retains its relative position, and a careful removal of the clay may even show their surfaces to be smoothed and polished. A somewhat similar kind of weathering is often observed in various kinds of volcanic rock. In some it peels off in concentric laminz ; where this disintegration has not penetrated the whole mass, the central nucleus remains solid and unaffected. Examples of a different kind are frequent in which the mass is disintegrated throughout, being easily crushed or broken and the granules sepa- rated. The strie formed previous to weathering in a few cases remain visible. Mr. G. H. Kinahan, of H.M. Geological Survey of Ireland, has informed me that blocks of disintegrated granite are frequent in the glacial deposits, especially those of Wicklow and south-east Wex- ford, being more prevalent in moraine-drift than in the Boulder- clay. There are granite boulders, imbedded in moraine accumu- lations, near Shap, Westmoreland, which have become disintegrated in various degrees, and to an extent as great as those occurring in the Boulder-clay of Cheshire, whereas at the present time the Shap granite, both. in the well-known blocks and 7 situ, weathers only on the exterior. What Mr. Kinahan states respecting the granite boulders of Co. Wicklow is equally applicable to some of volcanic origin in the glacial deposits of Co. Antrim, where they occur in every stage of disintegration, but modified according to their structure. Examples are met with in moraine- and esker-mounds, and in the Boulder- clay, exactly corresponding with some in the Boulder-clay of Cheshire. Rocks of various kinds are coated with a powder, derived from their disintegration, generally of a light-green colour, having mixed with it minute fragments of the same. In some, the general sur- face of which affords proof of glacial erosion, channels or hollows have been formed subsequently, these being filled with similar disintegrated materials. In other instances the weathering has so * The condition of these granite blocks coincides with the account given of some in Spitzbergen and Sweden, “split up whilst im st¢w by the action of the frost” (‘ Arctic Voyages of Prof. Nordenskidld,’ by Alex. Leslie, p. 238). BOULDER-CLAY OF CHESHIRE. 595 extended throughout the whole substance that, on removal, they break up entirely. A large proportion of Carboniferous-Limestone pebbles bear evi- dence of atmospheric and chemical erosion in a variety of ways. Occasionally they are weathered all over, and portions of organisms stand in relief; more frequently they are eroded in the same way over a considerable surface, whilst the remainder continues intact, with its ice-marks unaffected. A frequent feature is the formation of channels or hollows in the blocks; this occurs without affecting other portions, which may still retain marks of glaciation. This weathering of limestone appears as if caused by chemical erosion ; but the results so resemble those of other rocks to which this theory cannot apply, that it is rendered doubtful whether it can be entirely accounted for by that cause. In many instances limestone pebbles have been split into fragments which are occasionally in apposition, but being generally obtained from stone-heaps, they are more fre- quently detached. A glaciated one found in situ in the Boulder- clay is split into four fragments, which remain in apposition ; the split surfaces, as well the outer portion close to them, have sub- sequently been somewhat eroded since their fracture. It is evident that these various forms of weathering have occurred subsequently to glacier-action; and an examination of what is now in progress fails to explain these peculiar phenomena. It is only in Carboniferous- Limestone pebbles containedin morainic accumulations that examples occur similar to, and even identical with, those found in the Boulder-clay. Several pebbles of limestone are not only glaciated, but also perforated by mollusca and sponges ; as a rule, no shells are retained in the cavities. There is generally, if not always, evidence that the borings have been made subsequently to glaciation. In some in- stances they have afterwards also been again exposed to glacial friction, and fragments have likewise been broken off prior to their deposition in the clay. In two instances glaciated and perforated blocks were found to be afterwards weathered, one over the per- forated surface, the other as a channel-like groove on the portions covered with strie. A solitary example of borings in softer lime- stone (it may be of Antrim chalk) contains many shells entire, and its surface is covered with Serpule. A very frequent form of weathering in stratified, slaty, and other rocks is produced by their splitting into pieces, the surfaces thus formed having undergone little, if any, change; the fragments are more frequently detached and separated, but sometimes are in exact apposition ; or, when split into many parts, some may be contiguous, whilst others belonging to the same pebble are absent. Occasionally, but necessarily very rarely, pebbles have the split fragments separated for a small space, having fallen from each other as they dropped into the clay. In a glaciated one of Silurian sandstone found at Little Eye, Hilbre (an island at the mouth of the Dee), the fragments were an inch and a half from each other with their relative position changed. Another, at Rock Ferry, had the a> * ape’ . >>the. “an + 596 C. RICKETTS ON THE ERRATICS IN THE greater axis somewhat removed from the perpendicular with a small detached portion lying nearly at a right angle to its original position, the thinner and lower part not being entirely displaced, through resting on a slight projection at the lower end of the fracture (fig. 3). Similar glaciated pebbles “ split and shattered by the frost” into fragments which still remain exactly in apposition are, in many districts, buried in moraine accumulations formed on land. These fractures must have occurred subsequently to the envelopment of the blocks in glaciers, otherwise the pieces could not have eon- tinued so accurately in position whilst moving beneath such a burden. - Fig. 3.—Silurian pebble split, separated, and displaced, as in situ in Boulder-clay, Rock Ferry. (One third natural size.) Some erratics are so sculptured into forms dependent on differences in their texture, that the less easily disintegrated portions, and the harder materials filling shrinkage-joints, stand prominently in relief ; some are so fashioned and modelled that every bed, however thin, is Fig. 4.— Weuthered block from Fig. 5.— Weathered block with Boulder-clay. (One third smoothed surfaces from natural size.) Boulder-clay. (One third natural size.) Yj UYfep GZ, LY YY GIP £4 MULE: Cnt, hin VE x. Smoothed surfaces. conspicuous. There exists a great similarity between some such spe- cimens from the Boulder-clay and others in moraine accumulations (compare figs. 4—7). This is remarkably the case with two from a BOULDER-CLAY OF CHESHIRE. 597 moraine mound at Leighton Hall ; and another, of fantastic shape, is hardly distinguishable from an example near Shap, whilst others of a similar kind bear a striking resemblance to each other. Fig. 6.— Weathered block Fig. 7.— Weathered block from from Moraine. (One Moraine. (One third natural third natural size.) size. ) Several blocks, subsequently to being weathered, have had portions of their surface rubbed; this generally occurs over a very limited space, and leaves adjoining and even more prominent parts entirely untouched (fig. 5). No example has yet been found in moraines ; but it may be concluded that this attrition could not have been caused by propulsion along the rock-surface over which the glacier moved. Itis more probable that, carried forward by an accumulating glacier, thin pebbles have rubbed against others imbedded in the same moraine-heap. Pieces of flint occur in the Boulder-clay, but they are rare. Some have had flakes forcibly broken off, it may be several from the same specimen: occasionally the depression is formed which is the counterpart to the ‘“ bulb of percussion ;” and at this point the flint 1s sometimes crushed as if from the intensity of the pressure by which a flake has been splintered off. In others the more prominent and rounded portions of the nodules bear evidence of being rubbed and chipped as by a grinding motion under pressure. There are none which have been rounded by the rolling motion caused by waves or currents. The rarity of flints in the Boulder-clay is not surprising if it is considered that they have been carried into the Bay of Liverpool by means of icebergs and floes which ploughed their way across through closely packed ice, distributing their load of boulders in the passage ; even in the glacial accumulations in the neighbourhood of Belfast, in close proximity to the Chalk formation, they are not found to be very abundant. Many of the flints in the Eskers and —— 598 ON THE ERRATICS IN THE BOULDER-CLAY OF CHESHIRE in the Boulder-clay near Belfast have chips and flakes broken off, and the resulting angles crushed in a similar manner to some in the Boulder-clay of Cheshire and Lancashire. The most probable explanaticn of the separation of the chips and flakes is that the tlints, whilst enveloped in glaciers, passed over the platforms formed of layers of flints so constantly interstratified with the Chalk or White Limestone of Co. Antrim. The peculiar instances of weathering which rocks of different kinds have undergone prior to their deposition in the Boulder-clay appear to have escaped notice almost entirely, with the exception of blocks of disintegrated granite and trap; these are too conspicuous to be overlooked. The consideration of all these phenomena tends to prove that, during the glacial périod, though the climate was always of an arctic character, with perennial snow resting on the ground, there were frequent variations in the severity of the seasons—that a less amount of snow fell during one series of years than during another, so that for a considerable time glaciers receded, leaving the contents of moraines exposed to vicissitudes of the weather, to repeated successions of frost and thaw, probably re- curring daily during several months in the year. Again they in- creased in size and carried forward the accumulations as an integral part of their volume, so that they eventually reached the sea, and icebergs were formed, ‘forced off from their parent glaciers by the buoyant action of the sea” and floated away. They cannot be con- sidered to represent an interglacial period such as the examination of certain deposits in Scotland and elsewhere is supposed to indicate ; for these weathered erratics are found in all situations in the Boulder- clay. The changes in climate which took place appear to have been not unlike those which occur in Greenland, where it is recorded that the glaciers have been observed to successively recede and advance to the extent of several hundred yards *.. Insome respects they may be compared to changes of climate in our own country, where some winters are mild and others severe, some remarkable for abundance of rain or snow, others for frost and fine weather. DIscussIon. Dr. Evans thought the observations of Dr. Ricketts were of very great interest, whatever interpretation was put upon them. Dr. Hicxs asked if it were not possible that some of the changes indicated were due to the percolation of water through the sandy boulder-clays. = The AvrHor, in reply, said the evidence was entirely in favour of the decomposition having taken place before the imbedding of the fragments. * * —~ aie. 602 GENERAL INDEX. Cyprione Bristovii, 344.. Cypris purbeckensis, 347. Cythere retirugata, 390. transiens, 349. Dalton, Mr. W. H., on specimens of Voluta Lamberti and Cyprina angu- lata, Proc. 2. Darwinula leguminella, 346. Davies, Mr. D. C., on the North-Wales and Shrewsbury coal-fields, Proc. 107. Dawkins, Prof. W. Boyd, note on the mammalian fauna of the Val d’ Arno, 8. , on a skull of Ovibos moschatus from the sea-bottom, 242. De Kaap and Lydenburg, Mr. W. H. Penning on the goldfields of, 569. Derbyshire, South, fossiliferous no- dules and fragments of hematite from the Permian breccias of, Proc. 106. Diabase of the Rio-Tinto district, 250. Diabases of the Breidden Hills, 544. Dicranograptus shales near Haver- fordwest, 478, 487. Didymograptus shales near Haver- fordwest, 477, 486. Diluvial epoch in New Zealand, 213. Dimorphastrea fungiformis, 185. Dinornis, distribution of the species of, 214. Dinorwig railway, section along part Oe Diorite, Prof. Bonney on the so-called, of Little Knott, 511. Diorite-dykes of the Lydenburg and De Kaap Goldfields, 588. Diorite-dyke, section of, at Lisbon- Berlyn, South Africa, 583. Diplopodia Malbosit, 447. versipora, 444. Diporula, 296. Dolerite, Mr. J. J. H. Teall on the metamorphosis of, into hornblende- schist, 133. from Scourie Dyke, analysis of, 135. Dolerites of the Hebrides, 358; struc- of, 360. Donations to the Library and Museum, Prociga3: Donegal, Northern, Dr. C. Callaway on the granitic and schistose rocks of, 221. Doocashel, section through, 255. Downes, Rev. W., on the Cretaceous beds at Black Ven, near Lyme Regis, with some supplementary re- marks on the Blackdown beds, 23. Drift-deposits of Colwyn Bay, 102. Drumahoe quarry, 231; section through, 235. Dunaff Head, 234; granite of, 228; section from Londonderry to, 281, 235. Dunean, Prof. P. Martin, on the structure of the ambulacra of some fossil genera and species of regular Echinoidea, 419. | Dunfanaghy, section from, to Kilma- crenan, 235, 236. Dunites and gabbro, intersecting veins of, in olivine rock, 359. Dunlewy Church, 237; section north of, 226. Dunree Head, 233, 234; section through, 235. Echinoidea, Prof. P. Martin Duncan on the structure of the ambulacra of some fossil genera and species of regular, 419, Elephas primigenius from the Creswell- crag bone-caves, 30, 31. Enallohelia socialis, 175. England, Mr. R. F. Tomes on some Madreporaria from the Cretaceous formation of, Proc. 111. and North America, correlation of fish-bearing strata in, 59. Enstatites of the Hebridean gabbros, 370; analyses of, 372; changes in, in Hebridean rocks, 377 ; in palzo-. zoic peridotites, 397. Eocene plant-beds of the basaltic for- mation of Ulster, 82. Erratics in the Boulder-clay of Che- shire &e., Dr. C. Ricketts on some, 591. Eruptive rocks in New Zealand, 196, 215. Ettingshausen, Baron C. von, on the fossil flora of Sagor in Carniola, - 565. Eusmiline, table of genera of, 178. Fahan station, 232; section through, 235. Farnborough, well-section at, 4995; railway section at, 500. Faugher, Upper, section through, 239. Fault bringing shell-beds over lig- nites, near Husavik, 96. Felsites, Silurian, from Llanberis Pass, hollow spherulites in, 167. Felspar, structure of, in andesites of Moel-y-Golfa, 540. Felspars of Hebridean gabbros, analy- GENERAL INDEX. 603 ses of, 363; changes in, in Hebridean rocks, 375. Ffestiniog, Mr. T. M. Reade on boul- ders wedged in the falls of the Cynfael, Proc. 7. Fish-bearing strata, correlation of, in England and North America, 59. Fish, traces of, in the Onondaga red shale, 58. Flora, fossil, of Sagor in Carniola, 565. Foliation in the granite of Donegal, 228. Foraminifera of the Cambridge green- sand, Mr. Vine on the, Proc. 101. Forest, submerged, of Torbay, 9. Frimley, Mytchett Place, well-section at, 496. Fulgurite from Mont Blane, 152. Gabbro and dunite, intersecting veins of, in olivine rock, 359. Gabbros of the Hebrides, 357. Gardner, Mr. J. S., on the Lower Eocene plant-beds of the basaltic formation of Ulster, 82. , on the Tertiary basaltic forma- tion in Iceland, 93. Gault of Black Ven, fossils of the, 24, 25. . Gippsland, picrite from, 520. Glacial period in Australia, Dr. R. von Lendenfeld on the, Proc. 103. series in Lincolnshire and York shire compared, 131. Glenarm leaf-bed, 85. Gloucestershire, Madreporaria from the Great Oolite of, 170. Gneissic structure in Donegal granites, 230. Gold and nuggets in the Lydenburg and De Kaap goldfields, 587. Goniocora, 184. Goodrington Bay, map of, 11. beach, section of, 17. Granitic rocks of Northern Donegal, 221 ; supposed metamorphic origin of, 228. of the Kaap Valley and Lydenburg, 570. Gravels, rearranged, in Colwyn Bay, 105. Great Crosby, Lancashire, Mr. T. M. Reade on the evidence of the action of land-ice at, 454. Great Ooiite, Madreporaria from the, of the counties of Oxford, Glouces- ter, and Somerset, 170. Trigonie, 44. Green, Prof. A. H., on a section -near Llanberis, 74. Greenan, Lough, section through, 235. Gresley, Mr. W. S., on certain fos- siliferous nodules and fragments of hematite (sometimes magnetite) from the (so-called) Permian brec- cias of Leicestershire and South Derbyshire, Proc. 109. Grey marl of New Zealand, palzon- tology of the, 275. Groves’s Quarry, near Milton, section 1 EZ Ae ; Hematite, fossiliferous nodules and fragments of, Proc. 109. Hain, picrite of, 520. Haldon fossils, supplementary list of, 26. Halicore australis, 467. Halitherium Schinzi, 465, 466, 467. Happy Valley, Birkenhead, section in, 593. Hatcliffe, plan of the country near, £19: Haverfordwest, Messrs. Marr and Roberts on the Lower Palzozoic rocks of the neighbourhood of, 476. i on Hills, section through the, Hayle, section across the valley of the, 67. Hebridean gneiss, fold in, near Scou- rie dyke, 142. Hebrides, Tertiary peridotites of, 356; gabbros of, 357; dolerites of, 358. Hegarty’s rock, 233. Heliocenia oolitica, 181. Hemicidaris crenularis, 437. granulosa, 442. intermedia, 437. Hemipedina Bowerbankit, 423. Jardinii, 423. marchamensis, 424, tuberculosa, 425. Hessle Clay, 118. and Purple Clays, divisional tee between the, in Lincolnshire 126. Hof, Iceland, 99. Hofsgil, Iceland, cliff and ravine about 7 miles from, 100. Hokanui system, 202; eruptive rocks of the, 215. Homersham, Mr. C., and Prof. J. W. Judd on the deep boring at Rich- mond, Surrey, 523. Horn Head, 236. Hornblende-piecrite of Little Knott, Cumberland, 511. Hornblende-schist, Mr. J. J.H. Teall on the metamorphosis of dolerite into, ’ 604 GENERAL INDEX. 133; from Scourie dyke, analysis of, 137. Hot springs in New Zealand, 219. Howick, Auckland, section from, to the Wairéa river, 210. Hredevatn, Iceland, 101. Hughes, Mr. G., on some West-Indian phosphates, 80. Hulke, Mr. J. W., on the sternal ap- paratus in Iguanodon, 473. Hungarian lava and lithophyses, 163, 165. Hisavik, marine and freshwater beds of, 95; cliff-section on coast 9 miles N.E. of, 95; fault near, 95; section showing the position of the marine series of, 97. Hutton, Capi. F. W., on the correla- tion of the “Curiosity-Shop bed ” in Canterbury, New Zealand, 547. , on the geology of New Zealand, 191. , on the geological position of the “Weka-pass Stone” of New Zea- land, 266. Hyopsodus, 529. Iceland, Tertiary basaltic formation in, 93; hollow spherulites in ob- sidian from, 166. Igneous and associated rocks of the Breidden Hills, 532. matter, Dr. H. J. Johnston- Lavis on the injection, extrusion, and cooling of, Proc. 103. Iguanodon, Mr. J. W. Hulke on the sternal apparatus in, 473. Incheolm, picrite of, 520. Inferior Oolite Trigoniz, 37. Tron, metallic, in Hebridean gabbros, 374. Tron-ores of the Rio-Tinto district, 258, 255. Iron sandstone, traces of fish in the, 58. Irving, Rev. A., on a general section of the Bagshot strata from Alder- shot to Wokingham, 492. Jasper of the Rio-Tinto district, 249. ‘ Jeffreys, Dr. J. Gwyn, list of. fossil shells from Iceland, 96. Johnston-Lavis, Dr. H. J., on the physical conditions involved in the injection, extrusion, and cooling of igneous matter, Proc. 103. Jones, Prof. T. Rupert, on the Ostra- coda of the Purbeck formation, with notes on the Wealden species, 311. Judd, Prof. J. W., on the Tertiary and older peridotites of Scotland, 34. , and Mr. C. Homersham, on eee boring at Richmond, Surrey, Jukes-Browne, Mr. A. J., award of the Lyell Geological Fund to, Proc. 34. , on the Boulder-clays of Lincoln- shire; their geographical range, and relative age, 114. Kaap Valley, geology of the, 570; granitic rocks of the, 570; Silurian rocks of the, 570; Devonian rocks of the, 576. Kaihiku series, 203. Kaikoura formation, 201. peninsula, section of east head of, 275; plan and section of south beach of, 273. Kakanti series, 199. Kanieri series, 209. Kéreru series, 211. Kidstou, Mr. R., on the relationship of Ulodendron, Lindl. and Hutt., to Lepidodendron, Sternb., Bothroden- dron, Lindl. and Hutt., Sigillaria, Brongn., and Rhytidodendron, Bou- lay, Proc. 98. Kilmacrenan,section from Dunfanaghy to, 235, 236. series of schistose rocks, 230. Lancashire, Mr. T. M. Reade on the evidence of the action of land-ice at Great Crosby, 454. Land-ice, evidence of the action of, at Great Crosby, Lancashire, 454. Land’s End, Cornwall, Pliocene de- posit at St. Hrth, near the, 65. Lavas, ancient British, Mr. G. A. J. Cole on the occurrence of hollow spherulites in, 162. Leaf-beds, Ballypalady, 85; Glenarm, 85; Ballintoy, 86; Ardtun, 92. - Leicestershire, fossiliferous nodules and fragments of hematite from the Permian breccias of, Proc. 109. Lekythopora hystrix, 308. Lendenfeld, Dr. R. von. on the gla- cial period in Australia, Proc. 103. Lepidodendron, relationship of Ulo- dendron to, Proc. 98. Lepralia confinita, 299. depressa, 298. — edax, 297. ——- escharella, 298. subimmersa, 299. GENERAL INDEX. 605 Liassic Trigoniz, 35. Lichenopora paucipora, 113. Lincolnshire, Mr. A. J. Jukes-Browne on the Boulder-clays of, 114. , 8ketch-map of, showing the range of the Boulder-clays, 115. and Yorkshire, glacial series in, 131. Lingula flags near Haverfordwest, 476, 486. List of fossil shells from Iceland, 96. Lithophyses, 163, 164, 165. Little Knott, Prof. Bonney on the so-called diorite of, 511. Liverpool, section in the Bootle Docks, 592. Llanberis, Prof. A. H. Green on a section near, 74. Pass, hollow spherulites in felsites from, 167. Llandeilo limestone near Haverford- west, 477, 486. Llandovery beds, Lower, near Haver- fordwest, 485, 489. Llyn Padarn, section along part of the Dinorwig railway, on the north- east side of, 75. Lodes, pyrites, of the Rio-Tinto dis- trict, 255; manganese, of the Rio- Tinto district, 259. Londonderry, section from, to Dunaff Head, 231, 235. Lough-Foyle series of schistose rocks, 230. Lough Greenan, section on, 223, 224; section through, 235. Lough-Neagh formation, 87. Lough Salt, section through, 235. Low Barf, section through, 125. Ludlow rocks in the Breidden Hills, 538. Lydekker, Mr. R., on the zoological position of the genus Microcherus, Wood, and its apparent identity with Hyopsodus, Leidy, 529. Lydenburg and De Kaap, Mr. W. H. Penning on the goldfields of, 569. Lyell Geological Fund, award of the, to Mr. A. J. Jukes-Browne, Proc., 34- —— Medal, award of the, to Prof. H. G. Seeley, Proc., 33. Lyme Regis, Cretaceous beds at Black Ven near, 23. Madreporaria, Mr. R. F. Tomes on some, from the Cretaceous forma- tion of England, Proc. 111. , Mr. Tomes on some, from the Great Oolite of the coun- ties of Oxford, Gloucester, and Somerset, 170. Maerewhenua limestone, list of fossils from the, 558. Magnetite, Proc. 109. Maitai system, 200; eruptive rocks in, 215. Major, Dr. O. J. Forsyth, on the mammalian fauna of the Val d’Arno, 1. Malin and Malin Head, 234. Head, granites of, 228. Mammalian fauna of the Val d’Arno, Dr. C. J. Forsyth Major on the, 1. Manapouri system, 198; eruptive rocks in, 215. Manatus senegalensis, 468. Manganese lodes of the Rio-Tinto district, 259. Map of Lincolnshire, showing range of boulder-clays, 115; of Paignton and Goodrington Bays, 11; showing the western extension of the Clifton fault, 147; of the South Island of New Zealand, 195; of the Valley of the Waitaki and neighbouring region, 561. Marr, Mr. J. E., and Mr. T. Roberts, on the Lower Paleozoic rocks of the neighbourhood of Haverford- west, 476. Mastigophora Dutertrei, 301. Matakéa series, 204. Matatra series, 204. May-Hill beds in the Brefdden Hills, 536. Membranipora aperta, 286. circularis, 286. —— Flemingu, 288. —— Michaudiana, 289. parvicella, 288. radicifera, 287. rhynchota, 287. Savartii, 286. temporaria, 288. trifolium, var. propinqua, 289. Mesa de los Pinos, section in railway- cutting on the west side of the, 253; analysis of iron-ore from the, 253. Metacypris Forbesti, 345. , var. verrucosa, 345. Metals and minerals in the Lydenburg and De Kaap goldfields, 588. Metcalfe, Mr. A. T., on the discovery in one of the bone-caves of Creswell Crags of a portion of the upper jaw of Hlephas primigenius, containing im situ the first and second milk- molars, 31. Microcherus, Mr. R. Lydekker on the 606 GENERAL INDEX, zoological position of the genus, 529. Microcherus erinaceus, 529. Micropora patula, 290. perforata, 290. Microporella elevata, 296. —_— grisea, 294. magna, 295. magnirostris, 296. pociliformis, 295. Microsolena excelsa, 188. Middletown Hill, section across, 535 ; section from, to Purton Wood, 537. Milton, section in Groves’s quarry near, 171. Minerals composing the peridotites and allied rocks in the Western Islands, 362. of New Zealand, 219. , constituent, of picrites, 520. and metals of the Lydenburg and De Kaap goldfields, 588. Moel-y-Golfa, igneous rocks of, 539. Moldauthein, in Bohemia, Bouteillen- stein of, 152. Monoporella sexangularis, 291. Mont Blane, fulgurite from, 152. Montgomeryshire, East, the igneous and associated rocks of the Breidden Hills in, 532. Montlivaltia, 182. ; Moorhey brick and tile works, section at, 459. Morgan, Prof. C. L., on the S.W. ex- tension of the Clifton fault, 146. Motunau Creek, section across the south branch of the, 270. Mount Arthur series, 199. Brown, section through, 209. —— Hamilton, section through, 203. Torlesse formation, 201, 203. Mucronella mucronata, 293. nitida, 293. coccinea, var. mamillata, 294, Mull, Ardtun leaf-bed, 92. Murchison Geological Fund, award of the, to Mr. H. B. Woodward, Proc. 32. Medal, award of the, to Dr. F. Romer, Proc. 31. Neoplagiaulax, comparison of teeth of, with those of Tritylodon, 28. cocenus, molar teeth of, 28. New Zealand, Capt. F. W. Hutton on the geology of, 191. , on the geological position of the ‘‘ Weka-pass stone” of, 266. —, correlations of the “ Cu- riosity-Shop bed,” 547. New Zealand, raised beaches in, 212; section from the west coast of, to Tasman’s Bay, 200; table of sedi- mentary formations in, 194. Niagara group, fossils of, compared with those of the Wenlock lime- stone, 57. North America and England, correla- tion of fish-bearing strata in, 59. and Britain, correlation of Silurians of, 57. North Island of New Zealand, 196. North Wales coal-field, Mr. D. C. Dayies on the, Proc. 107. os list of Ototara fossils from, 556. system, 206; eruptive rocks of the, 215. Obsidian with hollow spherulites from Beaver Lake, 164, 165; from Ice- land, 166. Olivine in palzozoic peridotites, 397. Olivine-rock, intersecting veins of gabbro and dunite in, 350. Olivines of the Hebridean gabbros, 373; analysis of, 374. Onchus clintoni, 61. pennsylvanicus, 61. Onondaga Red Shale, traces of fish in the, 58. Oolitic Trigoniz, 37. Ophitic structure of dolerites, 360. Oreti river, section from the, to the Takitimi mountains, 203. Ormond series, 211. Oroseris Slatteri, 187. peteran ofthe Purbeckand Wealden, 11. Ovibos moschatus, 242. Owen, Sir Richard, cn remains of Elephas primigenius from one of the Creswell bone-caves, 31. , on the resemblance of the upper molar teeth of an Eocene mammal (Neoplagiaular, Lemoine) to those of Tritylodon, 28. Oxford clay, occurrence of, in deep well-boring at Chatham, 526. Oxfordshire, Madreporaria from the Great Colite of, 170. , North, Mr. E. A. Walford on the Trigonie of the Lower and Middle Jurassic beds of, 3d. Paignton Bay, map of, 11. Paleaspis, 54, 56, 62. americana, 62. bitruncata, 62. Palzozoic rocks, Lower, of the neigh- bourhood of Haverfordwest, 476. GENERAL INDEX. 607 Pareora system, 209; eruptive rocks of the, 216. Parton Wood, section from Middle- town Hill to, 537. Peat-deposits, Pleistocene, on Beh- ring’s Island, Dr. H. Woodward on a skeleton of Rhy ytinag gigas from the, 457. Peat-mosses in New Zealand, 213. Pebbles, split, from Boulder-clay, 596 Pedina Smithii, 433. Penarfynydd, picrite of, 517. Pengorphwysfa, picrite of, 516. Penmaenmawr, till at, 105. Penning, Mr. W. H., on the goldfields of Lydenburg and De Kaap, in the Transvaal, South Africa, 569. Peridotites, Prof. J. W. Judd on the Tertiary and older, of Scotland, 354. , Tertiary, 356 ; Palseozoie, 395. , Palzozoie, alteration of minerals in, 396; varieties of the, 398. Permian breccias of Leicestershire and South Derbyshire, fossiliferous nodules and fragments of hematite from the, Proe. 109. Pétane series, 211. Phosphates, Mr. G. Hughes on some West-Indian, 80. Phyllopora tumida, 109. Picrite-boulder near St. Davids, 518. Picrites, altered palzeozoic, of Scotland, 400. —, occurrence of, in Wales, 511; of Anglesey and Caernarvonshire, 515; paragenesis of minerals of, 520 Pidgeon, Mr. D., on some recent dis- coveries in the submerged forest of Torbay, 9. Plan of country near Hatcliffe, 119. Plant-beds, Lower Eocene, of the basaltic formation of Ulster, 82. Platastreea Conybeari, 184. Pleistocene peat-deposits, skeleton of Rhytina gigas from the, on Behring’s Island, 457. series in New Zealand, 212. Plesiodiadema Michelini, 430. Pliocene deposit at St. Erth, near the Land’s End, Cornwall, 65. Plutonic rocks, deep-seated, changes of the minerals in, 383. Polyzoa of the Cambridge Greensand, Mr. Vine on the, Proc. tot. Porfido-rosso antico, breeciated, 157. Porphyries of the Rio-Tinto district, 250. Porphyritic masses in the Rio-Tinto district, section, 252. Q.J.G.8. No. 164. Porphyritic schists of the Rio-Tinto district, 251. Porphyro-granulitie structure of do- lerites, 361. Preston Sands, plan of outcrops observed on, 12. Prorastomus, 465. Pseudo-chrysolite, or Bouteillenstein, of Moldauthein in Bohemia, 152. Pseudodiadema depressum, 429. hemisphericum, 428, 429. Pteraspidian fish from the Upper Silurian rocks of North America, 48. Pteraspis, 50. Purbeck formation, Prof. T. Rupert Jones on the Ostracoda of the, 311. Purple and Hessle clays, divisional line between the, in Lincolnshire, 126. Putatika series, 202. Putiki series, 211. Pyritic region of the Sierra Morena, Mr. J. H. Collins on the, 245. Pyrites deposits of the Rio-Tinto dis- trict, 245. of the Rio-Tinto district, 255; analyses of, 258, 259. Pyroxenes in andesites of Moel-y- Golfa, 541. in diabases of the Breidden Hills, 544. , rhombic, in_ paleozoic peri- dotites, 397. : ace in, in Hebridean rocks, ‘of the Hebridean gabbros, 366. Raised beaches in New Zealand, 212. Reade, Mr. T. Mellard, on the drift- deposits in Colwyn Bay, 102. , on the evidence of the action of land-ice at Great Crosby, Lan- cashire, 454. , on boulders wedged in the Falls of the Cynfael, Ffestiniog, Proc: 7. Redcliffe Towers, section of the ex- posure at, 20. Redhill shales, 482, 488. Reefs” of the Lydenburg and De Kaap goldfields, 572, 577. Renard, Prof., award of the Bigsby Gold Medal to, Proe. 35. Rhynchopora bispinosa, 302. Rhytidodendron, relationship of Ulo- dendron to, Proc. 98. ZG "| 6908 GENERAL INDEX. Rhytina gigas, skeleton of, from the Pleistocene peat-deposits on Beh- ring’s Island, 457. Richmond, Surrey, Prof. Judd and Mr. C. Homersham on the deep boring at, 525. Ricketts, Dr. C., on some erratics in the Boulder-clay of Cheshire &c., and the conditions of climate they denote, 591. Rimutaka series, 201. Rio-Tinto district, general description of the, 246; stratigraphy of the, 261; ore deposits of the, 262; sur- face geology of the 263. mines, Mr. J. H. Collins on the geology of the, 245. River-Murray cliffs, Chilostomatous Bryozoa from the, 279. Riwaka mountains, section through the, 200. series, 198. Roberts, Mr. T., and Mr. J. E. Marr, on the Lower Palzozoic rocks of the neighbourhood of Haverford- west, 476. Robeston Wathen limestone, 479, 487. Romer, Dr. F., award of the Mur- chison Medal to, Proc. 31. Rotten reef, Spitzkop, section of, 581. Rum, peridotites of, 390. Rutley, Mr. Frank, on fulgurite from Mont Blanc; with a note on the Bouteillenstein or pseudo-chrysolite of Moldauthein in Bohemia, 152. , on brecciated porfido-rosso antico, 157. Sagor, in Carniola, fossil flora of, 565. St. Davids, picrite boulder near, 518. St. Erth, Pliocene deposit at, 65. , section in pit near the vicarage, , section across the Hayle valley at, 67. Salt, Lough, section through, 235. Sandafell, Iceland, 98. Scaphaspis, 50. Schillerization, 383, 408. Schistose rocks of Northern Donegal, 221, 230. Schists, porphyritic, of the Rio-Tinto district, 251. Schizoporella Cecilii, 301. fenestrata, 301. —— phymatopora, 300. —— protensa, 301. simplex, var. aldingensis, 300. -—— striatula, 301. Schriesheim picrite, 520. Scotland, Prof. J. W. Judd on the Ter- tiary and older peridotites of, 354. Scourie Dyke, analysis of andesine from, 135; analysis of dolerite from, 135; analysis of hornblende- schist from, 137. , metamorphism in the, 139. Scyelite of Caithness, 401; analyses of, 402. Sections of Goodrington beach, 17; of the exposure at Redcliffe Towers, 20; in pit near St. Erth vicarage, 66; across the valley of the Hayle at St. Erth, 67; along a part of the Dinorwig railway, on the north-east side of Liyn Padarn, 75, 76; on coast nine miles N.E. of Hiusavik, 95; showing the position of the marine series of Husavik, 97; in ravine seven miles from Hofsgil, Iceland, 100; in Colwyn Bay, 102, 103; through Low Barf, 125; showing the erosion of the chalk-wolds, 129; of a fold in Hebridean gneiss, 142; from the west coast of New Zealand to Tas- man’s Bay, 200; from Howick, Auckland, to the Wairéa river, 210; from the Areti river to the Tak- timti mountains, 203 ; in Barnesbeg Gap and on Lough Greenan, 223; west of Croagh, 225; north of Dun- lewy Church, 225; from Dunaff Head to Londonderry, 235; from Dunfanaghy to Kilmacrenan, 235 ; showing porphyritic masses in the Rio-Tinto district, 252; in railway- | cutting on west side of the Mesa de los Pinos, 252; of the south lode at Rio Tinto, 260; showing kernels of cobaltiferous oxide of manganese, near Bella Vista, Rio- Tinto district, 261; across the river Waipara, 269; along Weka Pass, 269; on south bank of Con- way river, 271; through Amuri South Bluff, 272; of east head of - Kaikoura peninsula, 273; of south beach of Kaikoura peninsula, 273 ; at Moorhey brick and tile works, 455; in deep boring at Wellington College, 494; on South-eastern Railway near Wellington College, 498 ; across the valley of Aldershot town, 502; in cutting north of Wokingham station, 505; across Middletown Hill, 535; in small tributary of Belleisle Brook, 545; of Curiosity-Shop on the left bank of the Rakaia river, 547; showing the general form of the country and the fall of the rivers from the High Veldt, 571; of rotten reef, Spitz- kop, 581; of diorite dyke, Lisbon- GENERAL INDEX. Berlyn, S. Africa, 583; in Bootle Docks, Liverpool, 592; in Happy Valley, Birkenhead, 593. Sedimentary formations in New Zea- land, table of, 194. Seeley, Prof. H. G., award of the Lyell Medal to, Proc. 33. Selenaria maculata, 308. Shells, fossil, collected by Mr. J. S. Gardner in Iceland, 96. Shiant Isles, peridotite of the, 393. Sholeshook limestone, 480, 487. Shrewsbury coal-field, Mr. D. C. Davies on the, Proc. 107. Shropshire, West, the igneous and associated rocks of the Breidden Hills in, 5382. Sierra Morena, pyritic region of the, 245 Sigillaria, relationship of Ulodendron to, Proc. 98. Silurian rocks of the Breidden Hills, 536. -, Lower, of Welshpool, species of Phyllopora and Tham- niscus from the, 108. , Upper, of North America, Pteraspidian fish from the, 48. Silurians of North America and Britain, correlation of, 57. Sirenia, list of fossil, 470; biblio- graphy, 471. Slade beds, 483, 488. Slates of the Rio-Tinto district, 246 ; analyses of, 247. Smittia Landsborovii, 300. Milneana, var. cozquata, 300. Tate, 299. Somersetshire, Madreporaria from the Great Oolite of, 170. South Africa, goldfields of Lydenburg and De Kaap, in the Transvaal, 569. Island of New Zealand, 194. lode at Rio Tinto, sections of the, 260. Spherulites, hollow, Mr. G. A. J. Cole on, 162. Spinellids of the Hebridean gabbros, 374. Spitzkop, section of rotten reef, 581. Stafholt, Iceland, 101. Steganoporella magnilabris, 292. Rozieri, var. indica, 292. Sternal apparatus in Jguwanodon, Mr. J. W. Hulke on the, 473. Stomechinus bigranularis, 435. Stonyhurst, 271. Strongylocentrotus, 421. Stylosmilia excelsa, 180. reptans, 179. Syenite of the Rio-Tinto district, 249. 609 Takaka river, section crossing the, 200. system, 198. Takitimii mountains, section from the Oreti river to the, 203. Tasman’s Bay, section from the west coast of New Zealand to, 200. Tawhiti series, 209. Teall, Mr. J. J. H., on the meta- morphosis of dolerite into horn- blende-schist, 133. Te Anau series, 201. Tertiary basaltic formation in Ice- land, 93. Thamniscus antiquus, 111. Thamnocenia oolitica, 177. Thrust, lateral, evidence of, in granites and schists of Northern Donegal, 238. Thrust-plane, section of, 233. Till, bluish-grey, in Colwyn Bay, 103, 108. Tjarnir, Iceland, 98. Tomes, Mr. R. F., on some imper- fectly known Madreporaria from the Cretaceous formation of Eng- land, Proc. 111. , on some new or imperfectly known Madreporaria from the Great Oolite of the counties of Oxford, Gloucester, and Somerset, 170. Torbay, Mr. D. Pidgeon on some recent discoveries in the submerged forest of, 9. Transvaal, goldfields of Lydenburg and De Kaap, 569. Tricycloseris, 187. Trigonia Lycettit, 42. , var. corrugata, 43. northamptonensis, 30. pullus, 45. sp-, 45. Trigonie, Mr. E. A. Walford on the, of the Lower and Middle Jurassic beds of North Oxfordshire and ad- jacent districts, 35. Trigoniz from the Lias, 35; from the Inferior Oolite, 37; from the Great Oolite, 44. Trinucleus-seticornis beds, 480, 487. Tritylodon, comparison of teeth of, with those of Neoplagiaulax, 28. Turanganti series, 207. Twinning, lamellar, in felspar-crystals, 364. Ulodendron, Mr. R. Kidston on the relationship of, to Lepidodendron, Bothrodendron, Sigillaria, and Rhy- tidodendron, Proc. 98. 610 Ulster, Lower Eocene plant-beds of the basaltic formation of, 82. Ultra-basic rocks, Tertiary, of the Hebrides, 389. Val d’Arno, mammalian fauna of the, ie Vine, Mr. G. R., on species of Phyl- lopora and Thamniscus from the Lower Silurian rocks of Welshpool, Wales, 108. , on the Polyzoa and Forami- nifera of the Cambridge Greensand, Proc. tol. Voluta Lamberti, Proc. 2. Waihao limestone, fossils from the, 559. ; Waipara river, section across the, 269 system, 204; eruptive rocks of the, 215. Wairda series, 202. Waitaki, valley of the, fossils from the, 558; map of the valley of the, and neighbouring region, 561. Waitemata series, 209. Wales, occurrence of picrites in, 511. Walford, Mr. EH. A., on the strati- graphical positions of Trigonie of the Lower and Middle Jurassic beds of North Oxfordshire and ad- jacent districts, 35. Wanaka series, 199. Wanganti system, 211; rocks of the, 217. Waters, ferruginous, from Rio-Tinto mines and works, 255. Waters, Mr. A. W., on Chilostomatous Bryozoa from Aldinga and the Murray-River cliffs, South Aus- tralia, 279. Watts, Mr. W. W., on the igneous and associated rocks of the Breidden Hills, in East Montgomeryshire and West Shropshire, 532. Wealden Ostracoda, Prof. T. Rupert Jones on the, 311. Weka Pass, section along, 269. ‘‘Weka-pass Stone” of New Zealand, Capt. F. W. Hutton on the geo- logical position of the, 266. ——, list of fossils from the, 54. ——, paleontology of the, 275. eruptive GENERAL INDEX. Well-boring, deep, at Richmond, 523; at Chatham, 526. Wellington College, section across the valley north of, 503; road-section north of, 504. lakes, sections at, 499. —— ——.,, well-section at, 493, 494. station, railway-cuttings at, 496, 498. Well-sections in Bagshot area, 493. Welshpool, Mr. G. R. Vine on species of Phyllopora and Thamniscus from the Lower Silurian rocks of, 108. Wenlock limestone and Niagara group, fossils of the, compared, 57. 2 shale in the Breidden Hills, te Western Isles, Tertiary peridotites of, 396; gabbros of, 357; dolerites of, 308. West-Indian phosphates, Hughes on some, 80. Westland formation, 201. Wokingham, Rev. A. Irving on a general section of the Bagshot strata from Aldershot to, 492. , Bagshot series at, 504; section in cutting at, 505. Wollaston Donation Fund, award of the, to Dr. C. Callaway, Proc. 31. Gold Medal, award of the, to Mr. George Busk, Proc. 30. Wood, Mr. Searles V., table of dis- tribution of fossil shells from Ice- land, 96. , on a new deposit of Pliocene age at St. Erth, near the Land’s End, Cornwall, 65. Woodward, Mr. H. B., award of the Murchison Geological Fund to, Proc. 32. , Dr. H.,on an almost perfect skele- ton of Rhytina gigas (Rhytina Stel- leri, ‘* Steller’s Sea-cow’’), obtained _ by Mr. R. Damon from the Pleis- tocene peat-deposits on Behring’s Island, 457. —e Mr. G. Yateley Green, well-section at, 500. Yorkshire and Lincolnshire, glacial series in, 131. York Town and Camberley, sections at, 499. END OF VOL. XII. Printed by TaYLoR and Francis, Red Lion Court, Fleet Street. ‘ PROCEEDINGS OF THE GEOLOGICAL SOCIETY OF LONDON. SESSION 1884-85. November 5, 1884. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. William Lower Carter, Esq., B.A., Emmanuel College, Cambridge, was elected a Fellow of the Society. The Secretary announced,that a water-colour picture of the Hot Springs of Gardiner’s River, Yellowstone Park, Wyoming Territory, U.S.A., which was painted on the spot by Thomas Moran, Esq., had been presented to the Society by the artist and A. G. Renshaw, Esq., F.G.8. The List of Donations to the Library was read. The following communications were read :— 1. “On anew Deposit of Pliocene Age at St. Erth, 15 miles east of the Land’s End, Cornwall.” By 8S. V. Wood, Esq., F.G.S. 2. “The Cretaceous Beds at Black Ven, near Lyme Regis, with Some supplementary remarks on the Blackdown Beds.” By the Rey. W. Downes, B.A., F.G.S. 3. “On some Recent Discoveries in the Submerged Forest of Torbay.” By D. Pidgeon, Esq., F.G.S. The following specimens were exhibited :— Specimens exhibited by Searles V. Wood, Esq., the Rev. W. Downes, B.A., and D. Pidgeon, Esq., in illustration of their papers. ? a 2 PROCEEDINGS OF THE GEQLOGICAL SOCIETY. A worked Flint from the Gravel-beds (? Pleistocene) in the Valley of the Tomb of the Kings, near Luxor (Thebes), Egypt, ex- hibited by John EH. H. Peyton, Ksq., F.G.S. Specimens of Voluta Lamberti from the Coralline Crag, and of Cyprina angulata from the Blackdown beds, exhibited by W. H. Dalton, Esq., F.G.S8. Upon these specimens the following note by Mr. Dalton was read :—“ The attention of the Society being directed to the Blackdown beds, it may be worth while to note a peculiar feature in the specimen exhibited of Cyprina angulata, Fleming, belonging to the Museum of Practical Geology, and brought here to- night by the kind permission of the Director-General of the Geolo- gical Survey. “The valve, lying with its concavity downwards, has but partially imbedded itself in the sediment, and in subsequent silicification a film of chalcedony has been deposited on the free surface of the matrix within the shell. “Similar surfaces are shown by the casts of Voluta Lamberti, Sowerby, also here exhibited, from the collection of Mr. H. Stopes, F.G.8. These were found in a small quarry of the Coralline Crag rock-bed at Aldborough. ‘They show that as the shells lay on the sea-bed, the upper part of each whorl was occupied by gases arising from the decomposition of the animal, to the exclusion of the cal- careous mud, which could only rise to the crest of the arch of each ‘successive suture. Its surface within the shell was not a plane, like that of the Blackdown specimen, but shows, for each whorl, an upward bulge in the centre, an annular depression near the edge, and a rise from this hollow to the interior surface of the shell, indi- cating the effect of alternating pressures (probably tidal) acting, through the mouth of the shell, on the elastic cushion of imprisoned gases, which would have escaped by the spiral, had the shells been rolled over two or three times only by currents.” November 19, 1884. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. Nicol Brown, Esq., 34 Canonbury Park, N.; James Charles Chaplin,’ Esq., 10 Earl’s Court Square, 8.W.; Herbert W. Hughes, Esq., Assoc. R.S.M., Priory Farm House, Dudley ; and Rev. Samuel Pilling, Osborne Terrace, Regent Road, Blackpool, were elected Fellows; Professor A. L. O. Descloizeaux, of Paris, a Foreign Member; and Professor Hermann Credner, of Leipzig, a Foreign Correspondent of the Society. The List of Donations to the Library was read. The following communications were read :— 1. “Note on the Resemblance of the Upper Molar Teeth of an Eocene Mammal (Weoplagiaulaz, Lemoine) to those of Tritylodon.” By Sir Richard Owen, K.C.B., F.R.S., F.G.S. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 3 2. “On the Discovery in one of the Bone-caves of Creswell Crags of a portion of the Upper Jaw of Hlephas primgenws, con- taining, in situ, the first and second Milk-molars (right side).” By A. T. Metcalfe, Esq., F.G.S. 3. “Notes on the Remains of Elephas prinugenius from one of the Creswell Bone-caves.” By Sir R. Owen, K.C.B., F.RBS., HG.S., GE. 4, **On the Stratigraphical Positions of the Trzgonie of the Lower and Middle Jurassic Beds of North Oxfordshire and adjacent districts.” By Edwin A, Walford, Esq., F.G.S. The following objects were exhibited :— Micro-photographs, illustrating secondary structures in some Sutherland rocks, exhibited by J. J. H. Teall, Esq., F.G.S. A specimen of Silver Glance incrusting Calcite, from Rabbit Mountain, Lake Superior, exhibited by H. Bauerman, Esq., F.G.S. A new substage Condenser for the Microscope, exhibited by Dr. G. C. Wallich. Specimens exhibited by Messrs. Metcalfe and Walford, in illus- tration of their papers. December 3, 1884. Prot. T. G. Bonnzy, D.Sc., LL.D., F.R.S., President, in the Chair. Walter Henley Bartlett, Esq., F.R.A.S., 4 Great George Street, Westminster, 8.W.; Thomas Brook, Esq., Assoc. M. Inst. C.E., Hartley, Kirkburton, near Huddersfield ; Charles Ziethen Bunning, Esq., Warora, Central Provinces, East Indies; Thomas Edward Candler, Esq., Canton Club, Canton, China ; Orville Adelbert Derby, Esq., Rio de Janeiro, Brazil ; Colin Docwra, Esq., Balls Pond Road, N.; Charles Eastwood, Esq., Linacre Works, Bootle, Liverpool ; Frank Lynwood Garrison, Esq., 1523 Girard Avenue, Philadelphia, U.S.A.; Richard Charles Hills, Esq., 448 Welston Street, Denver, Colorado, U.S.A.; Frank Johnson, Esq., Rio Tinto, and 379 Euston Road, N.W.; Sir Herbert Eustace Maxwell, Bart., M.P., Monreith, Whauphill, N.B.; W. J. E. de Miller, Esq., Landhof, Bern, Switzerland ; James Sterling, Esq., F.L.S., District Surveyor, Omeo, Victoria; Thomas Henry Ward, Esq., E.I.R. Collieries, Giridih, Bengal; Rev. Brownlow J. Westbrook, Greymouth, New Zealand ; and W. Hoffman Wood, Esq., 14 Park Square, Leeds, were elected Fellows of the Society. The List of Donations to the Library was read. - The Secretary announced that the following specimens had been presented to the Society’s Museum :— Specimens illustrating a paper on the Serpentines of Porthalla Cove (Q.J.G.8. vol. xl. p. 458), presented by the author, J. H, Collins, Esq., F.G.S. 4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Two slides with Cretaceous Lichenoporide, illustrating a pap in the Q. J.G.S. vol. xl. p. 850, presented by the author, G. R. Vin Esq. Specimens of Fossil Bryozoa from Muddy Creek, Victoria, pre- sented by J. Bracebridge Wilson, Esq., of Geelong. Casts of Footprints in the Lower New Red Sandstone of Penrith, illustrating a paper in the Q.J.G.S8. vol. xl. = £79, presented by the author, G. Varty Smith, Ksq., F.G.S. The Presipent announced the great loss which the Society had sustained in the decease of Mr. R. A. C. Godwin-Austen, F.R.S., which took place at his country seat, Shalford House, near Guild- ford, on the 25th November, in his 76th year. He became a Fellow of the Society in the year 1830, so that he had belonged to it for 54 years. For three years he filled the office of Foreign Secretary; he had been a Vice-President and an active Member of the Council ; but he always refused to be nominated as President, although several times urged to accept that honour. He was a Wollaston Medallist and the author of sixteen papers in the Society’s publications. His writings were remarkable for their clear and masterly character, and displayed that peculiar insight into geological structure which almost amounts to foresight. The following communications were read :— 1. “Note on a Section near Llanberis.” By Professor A. H. Green, F.G.S. 2. “The Tertiary Basaltic Formation in Iceland.” By J. Starkie Gardner, Esq., F.L.S., F.G.S. 3. “On the Lower Eocene Plant-beds of the Basaltic Formation of Ulster.” By J. Starkie Gardner, Ksq., F.L.S., F.G.S. The following objects were exhibited :— Rock-specimens and Microscopic Sections, exhibited by Prof. A. H. Green, F.G.S., in illustration of his paper. Specimens, exhibited by J. 8. Gardner, Esq., F.G.S., in illustra- tion of his paper. Specimens from Iceland, exhibited by Prof. J. W. Judd, F.R.S., Sec. G.S., in illustration of Mr. Gardner’s paper. A photograph of Paleophoneus nuncius, Torell and Lindstrom, from the Upper Silurian of the Isle of Gotland, exhibited by Dr. H. Woodward, F.R.S., F.G.S. Clay Ironstone Slabs from the Forest-bed of Happisburgh, ex- hibited by E. T. Newton, Hsq., F.G. 8. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 5 December 17, 1884. W. Carrvuruers, Esq., F.R.S., Vice-President, in the Chair. David Llewellin Evans, Esq., The Gold Tops, Newport, Mon- mouthshire, was elected a Fellow of the Society. The List of Donations to the Library was read. The following communications were read :— 1. “On the South-western Extension of the Clifton Fault.” By Prof. C. Lloyd Morgan, F.G.S., Assoc. R.S.M. - 2. “On the Recent Discovery of Pteraspidian Fish in the Upper Silurian Rocks of North America.” By Prof. E. W. Claypole, B.A., B.Se. (Lond.), F.G.S. 3. “ On some West-Indian Phosphate Deposits.” By George Hughes, Esq., F.C.S. (Communicated by W. T. Blanford, Esq., LEDs P-S., See, 6.8.) 4. “Notes on species of Phyllopora and Thamniscus from the Lower Silurian Rocks, near Welshpool, Wales.” By George Robert Vine, Esq. (Communicated by Prof. P. Martin Duncan, F.R.S., F.G.8.) Specimens and photographs were exhibited by George Hughes, Esq., F.C.8., in illustration of his paper. January 14, 1885. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. Ewan Cameron Galton, Esq., B.A., Shelsley Grange, Worcester ; Henry Brougham Guppy, Esq., M.B. Edinb., R.N., Surgeon on Board H.M.S. ‘ Lark,’ 17 Wood Lane, Falmouth ; Henry G. Hanks, Esq., State Mineralogist, California State Mining Bureau, San Francisco; and William Elliott Howe, Esq., Matlock Bath, Derby- shire, were elected Fellows of the Society. VOL. XLI. b 6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. The List of Donations to the Library was read. The following communications were read :— 1. “The Metamorphism of Dolerite into Hornblende-schist.” By J. J. Harris Teall, Esq., M.A., F.G.S. 2. “ Sketch of the Geology of New Zealand.” By Captain F. W. Hutton, F.G.S8., Professor of Biology in the Canterbury College, University of New Zealand. 3. “The Drift-deposits of Colwyn Bay.” By T. Mellard Reade, Ksq., F.G.S. The following objects were exhibited :— Life-sized photographs of the fruit of the recent Cycads, Encephal- artos latifrons and E. longefolius, from South Africa, exhibited by Prof. W. T. Thiselton Dyer, F.R.S. Objects shown with simple illumination, dark-ground illumina- tion, and polarized light, by means of Dr. Wallich’s new Condenser, exhibited by Dr. G. C. Wallich. Specimens and microscopic rock-sections, exhibited by J. J. H. Teall, Esq., F.G.S., in illustration of his paper. January 28, 1885. Prof. T. G. Bonnry, D.Sc., LL.D., F.R.S., President, in the Chair. Frederick John Cullis, Esq., 28 Claremont Road, Handsworth, Birmingham ; Henry Dewes, Esq., 19 Duchess Road, Edgbaston, Birmingham ; Henry Hutchins French, Esq., Grove Road, Sutton, Surrey ; Jacob Hort Player, Esq., F.C.S., Calthorpe Road, Birming- ham; and the Honourable Donald A. Smith of Montreal were elected Fellows, and Professor F. Fouqué of Paris and Dr. Gustav Lindstrom of Stockholm, Foreign Correspondents of the Society. The List of Donations to the Library was read. The Prusrpent called attention to the great loss the Society had sustained in the sudden and unexpected death of Dr. J. Gwyn Jeffreys, F.R.S., &c., who had been for twenty-one years continuously a Member of the Council, and for fourteen years of that time had performed most valuable services to the Society as. Treasurer. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 7 The following communications were read :— 1. “The Boulder-Clays of Lincolnshire: their Geographical Range and Relative Age.” By A. J. Jukes-Browne, Esq., B.A., F.G.S. 2. “On the Geology of the Rio-Tinto Mines, with some general remarks on the Pyritic Region of the Sierra Morena.” By J. H. Collins, Esq., F.G.S. 3. “On some new or imperfectly known Madreporaria from the Great Oolite of the Counties of Oxford, Gloucester, and Somerset.” By R. F. Tomes, Esq., F.G.S. Specimens of Flint implements were exhibited by John Evans, Esq., LL.D., F.R.S., F.G.S. February 11, 1885. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. Arthur William Clayden, Esq., M.A., North Lodge, Bath College, Bath; Samuel Rideal, Esq., B.Sc. (Lond.), F.C.S., Devon Lodge, Mayow Road, Forest Hill, 8.E.; and H. W. Williams, Esq., Solva, Pembrokeshire, were elected Fellows of the Society. The List of Donations to the Library was read. The following communications were read :— 1. “The Tertiary and Older Peridotites of Scotland.” By Prof. John W. Judd, F.R.S., Sec.G.S. 2. “Boulders wedged in the Falls of the Cynfael, Ffestiniog,” By T. Mellard Reade, Esq., F.G.S. [ Abstract. | This paper briefly described certain phenomena of stream-denu- dation observed in the bed of the Cynfael, which has cut a deep channel through the Lingula Flags, the course of the channel being mainly dependent on the jointing of the rock. In one spot the upper beds at the top of the gorge have slid upon the lower along their dip, about 10° to north by east, so as to project over the stream like a corbel; and advantage has been taken of this to form a bridge by means of a slab of rock laid trom the projecting mass to the top of the opposite bank. At another point several very large a ag 8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. boulders are wedged fast in the channel, and suspended over the stream, which flows about 6 feet beneath them. The boulders could not possibly have been carried down the existing gorge, and they did not, the author believed, fall from above. He suggested that they might have been carried down by the aid of ice, probably in the glacial period, when the stream ran in a wider channel at a higher level, and that the stream had since deepened its bed at least 6 feet below them. The following objects were exhibited :— Rock-specimens and Microscopic Sections, exhibited by Prof. J. W. Judd, F.R.S., in illustration of his paper. Platinotype Photographs of Views in various parts of England, illustrating the features of the different Geological Formations, ex- hibited by R. H. Tiddeman, Esq., F.G.S. ANNUAL REPORT. 9 ANNUAL GENERAL MEETING, February 20, 1885. Prof. T. G. Bonnry, D.Sc., LL.D., F.R.S., President, in the Chair. REPORT OF THE CouNcIL FoR 1884. In presenting their Report for the year 1884, the Council of the Geological Society regret to have to state that the improvement which they thought might be recognized in the position of the Society when they drew up their last Annual Report has not been maintained. They can only once more express the hope that this state of things is due chiefly, if not entirely, to the wide-spread depression which still prevails, and that in the course of a year or two a revival of the general prosperity of the country may place the affairs of the Society once more upon a satisfactory footing. The number of Fellows elected. during the year is only 48, of whom 34 paid their fees before the end of the year, making, with 9 previously elected Fellows who paid their fees in 1884, a total accession during the year of only 43 Fellows. Against even this small number we have to set the loss by death of 32 Fellows, and by resignation of 18 Fellows, while 8 Fellows were removed from the list for non-payment of contributions, making a total loss of 58 Fellows. There is thus a decrease of 15 in the number of Fellows. Of the 32 Fellows deceased 6 were compounders, and 7 non-contributing Fellows, and as 1 non-contributing Fellow became Resident, and another resigned, the number of contributing Fellows is reduced by 6, being now 816. The total number of Fellows and Foreign Members and Corre- spondents was 1434 at the close of the year 1883, and 1420 at the end of 1884. At the end of the year 1883 there were 2 vacancies in the list of © Foreign Members; and during 1884 intelligence was received of the decease of 2 Foreign Members. Four Foreign Members were elected during the year to fill up these vacancies. In the list of Foreign Correspondents there was 1 vacancy at the close of 1883, and intelligence was received of the death of 2 more during the year 1884. These losses, with the fillmg up of the above-mentioned vacancies in the list of Foreign Members, pro- VOL. XLI. ¢ Io PROCEEDINGS OF THE GEOLOGICAL SOCIETY. duced in all 7 vacancies in the list of Foreign Correspondents, 5 of which were filled up during the year. Thus at the close of the year 1884, the list of Foreign Members was complete, and there were 2 vacancies in that of the Foreign Correspondents of the Society. The total Receipts on account of Income for the year 1884 were only £2527 1s. 8d. being £87 9s. 5d. less than the estimated Income for the year. The total Expenditure, on the other hand, amounted to £2699 17s. 6d., or £109 13s. more than the estimated Expenditure for the year. The excess of the Expenditure over the Income of the year was therefore £172 15s. 10d. Out of the Balance in the Society’s hands at the beginning of 1884, the Council have invested the sum of £100 in the purchase of £99 Os. 2d. Consols. The Council have to announce the completion of Vol. XL. and the commencement of Vol. XLI. of the Society’s Quarterly Journal. The Council have also to announce that a valuable picture of the Hot Springs of Gardiner’s River, Yellowstone Park, painted on the spot by T. Moran, Esq., has been kindly presented to the Society by that gentleman and A. G. Renshaw, Esq., F.G.S8. The Council have awarded the Wollaston Medal to George Busk, Esq., F.R.S., F.G.8., in recognition of the valuable services he has rendered to Geological Science by his long-continued researches among the Recent and Fossil Polyzoa, and the Mammalia of the Post-Tertiary deposits. The Murchison Medal, with the sum of Ten Guineas from the proceeds of the Fund, has been awarded to Dr. Ferdinand Romer, For. Memb. G.S., in testimony of appreciation of his researches in Paleontology and Stratigraphical Geology, especially among the rocks of Paleozoic age, in both the Old and the New World. The Lyell Medal, with the sum of Forty Pounds from the proceeds of the Fund, has been awarded to Professor H. G. Seeley, F.R.S., F.G.S., in recognition of his numerous and valuable contributions to Vertebrate Paleontology and General Geology, and to aid him in the further prosecution of his researches. The Bigsby Medal has been awarded to M. Alphonse Renard, For. Corr.G.8., in token of appreciation of the great value of his petrographical researches among the older formations of Belgium, and his studies of the nature and origin of Deep-sea Deposits. The balance of the proceeds of the Wollaston Donation Fund has been awarded to Dr. Charles Callaway, F.G.S., in recognition of the value of his investigations among the Archean rocks, and to aid him in the further prosecution of his researches. The balance of the proceeds of the Murchison Geological Fund has been awarded to Horace B. Woodward, Ksq., F.G.S., in testimony of appreciation of his critical study of the Geology of England and Wales, and to aid him in completing his accurate digest of informa- tion upon the subject. The balance of the proceeds of the Lyell Geological Fund has been awarded to A. J. Jukes-Browne, Esq., F.G.S., in recognition of the OL ——— ANNUAL REPORT, EE value of his investigations concerning the subdivisions of the Cre- taceous Rocks of this country, and to aid him in their further prosecution. Report oF THE LIBRARY AND Museum ComMMITTER. L[nbrary. Since the last Anniversary Meeting a great number of valuable additions have been made to the Library, both by donation and by purchase. As Donations the Library has received about 219 volumes of separately published works and Survey Reports, and about 300 Pamphlets and separate impressions of Memoirs, besides about 134 volumes and 148 detached parts of the publications of various Societies, and 16 volumes of independent Periodicals presented chiefly by their respective Editors, and also 16 volumes of News- papers of various kinds. This will constitute a total addition to the Society’s Library, by donation, of about 420 volumes and 300 pamphlets. A considerable number of Maps, Plans, and Charts have been added to the Society’s collections by presentations, chiefly from the Ordnance Survey of Great Britain, and from the French Dépét de la Marine. These amount altogether to 832 sheets, but of them 788 sheets, large and small, are from the Ordnance Survey. Of the remainder, 26 sheets are from the Dépét de la Marine, 6 from the Geological Survey of Saxony, 6 from that of Sweden, 5 from that of Norway, and 1, a large Geological Map of Canada, from the Canadian Geological Survey. The Books and Maps above referred to have been received from 154 personal Donors, the Editors or Publishers of 15 Periodicals, and 172 Societies, Surveys, and other Public Bodies, making in all 341 Donors. By Purchase, on the recommendation of the Standing Library Committee, the Library has received the addition of 32 volumes of Books, and of 55 parts (making about 18 volumes) of various Periodicals, besides 33 parts of certain works published serially. Of the Geological Survey Map of France 9 sheets have been obtained by purchase. The cost of Books, Periodicals, and Maps purchased during the year 1884 was £83 14s. 3d., and of Binding £54 9s. 8d., making a total of £138 3s. 11d. a a ~~ > sie I2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Museum. The Collections in the Museum remain in much the same con- dition as at the date of the last Report of the Committee. During the year 1884 several interesting Donations were made to the Museum, the chief among them being a series of fossil Chilo- stomatous Bryozoa from Muddy Creek, Victoria, Australia, illustrative of Mr. A. W. Waters’s papers in the ‘ Quarterly Journal,’ presented by J. Bracebridge Wilson, Esq., of Geelong. The others were :—A specimen of Trowlesworthite, presented by R. N. Worth, Esq., F.G.S.; specimens of “ Iron-amianthus,” presented by the Rev. J, Magens Mello, F.G.S.; specimens illustrative of his paper on Por- thalla Cove, presented by J. H. Collins, Esq., F.G.S.; two slides of Cretaceous Lichenoporide, presented by G. R. Vine, Esq.; and casts of Footprints in the Lower New Red Sandstone of Penrith, presented _ by G. V. Smith, Esq., F.G.8. ANNUAL REPORT. 13 CoMPARATIVE STATEMENT OF THE NUMBER OF THE SOCIETY AT THE CLOSE OF THE YEARS 1883 anv 1884. Dec. 31, 1883. Dec. 31, 1884. Compoungers 2 1. .<\15 i0(as Fas: ey ae es Se 313 Contributing Fellows...... Sa Me ate ae ets 816 Non-contributing Fellows. . pore Mp nd He te, te! ote 213 1357 1342 Foreign Members ......... Sie! ee nie age an 40 Foreign Correspondents... . SHON Vets ter ae 38 1434 1420 Comparative Statement explanatory of the Alterations in the Number of Fellows, Foreign Members, and Foreign Correspondents at the close of the years 1883 and 1884. Number of Compounders, Contributing and pa 1357 contributing Fellows, December 31, 1883.... Add Fellows elected during former year and aa 9 LSD el Wor aVs Eh OMe Noes SE eg ep hia en Oe ee Deduct Compounders deceased .............. 6 Contributing Fellows deceased ........ 19 Non-contributing Fellows deceased .... 7 Contributing Fellows resigned ........ Lie Non-contributing Fellow resigned 1 Contributing Fellows removed ........ 8 1342 Number of Foreign Members, and Eee at Correspondents, December 31, 1883 .... J Deduct Foreign Members deceased .. ..... 2 Foreign Correspondents deceased 2 Foreign Correspondents elected 4 Foreien: Members; <2). sek } 69 Add Foreign Members elected ........:..... Foreign Correspondents elected ........ Ou 1420 | a. -_ ——_ °°» » » — €or i4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. DEcEASED FELLOWS. Compounders (6). Adams, G. F., Esq. Milligan, J., Esq. Bragge, W., Esq. Osborne, Lieut.-Col. W. Lyon, W., Esq. Wood, 8. V., Esq. Resident and other Contributing Fellows (19). Beanland, Rev. A. Murray, Alex., Esq. Browne, W. K., Esq. Pease, T., Esq. Forbes, J. E., Esq. Richardson, R., Esq. Godwin-Austen, R. A. C., Esq. Silver, Rev. F. Henty, G. M., Esq. Tomlison, H., Esq. Herapath, 8., Esq. Tylor, A., Esq. Hunter, W., Esq. Vennor, H. G., Esq. Hutt, Rev. T. G. Williams, C. O., Esq. Iselin, J. F., Esq. Williams, J. J., Esq. Jones, Sir W., Bart. Non-contributing Fellows (7). Buckman, J., Esq. Lancaster, J., Esq. Colthurst, J., Esq. Stokes, Rev. W. H. Curley, T., Esq. Wright, Dr. T. Jenner, R. F. L., Esq. Foreign Members (2). Sella, Il Com. Q. | Géppert, Prof. H. R. Foreign Correspondents. Hochstetter, Dr. F. von. | Jager, Dr. G. F. Fellows Resigned (18). Cockburn, W., Esq. Morris, D., Esq. Cooke, Maj.-General A. C. Neate, P. J., Esq. Fox, C. J., Esq. Preston, L., Esq. Gibson, Dr. G. A. Rogers, A., Esq. Greaves, Rey. R. W. Ross, Lieut.-Col. W. A. Hardwick, P. C., Esq. Sainter, J. D., Esq. Harris, W. H., Esq. Stair, A., Esq. Ladell, H. R., Esq. Ward, J., Esq. Marshall, J., Esq. Willis, J., Esq. ANNUAL REPORT. 15 Fellows Removed (8). Bevan, G. P., Esq. Mellor, T. R., Esq. Byrom, W. A., Esq. Parsons, Sergeant W. Coates, J., Esq. Randell, J. E., Esq. Kemshead, Dr. W. B. Shaw, Dr. J. The following Personages were elected from the List of Foreign Cor- respondents to fill the vacancies in the List of Foreign Members during the year 1884. Professor G. Capellini of Bologna. Professor A. L. O. Des Cloizeaux of Paris. Professor G. Meneghini of Pisa. Professor J. Szabo of Pesth. The following Personages were elected Foreign Correspondents during the year 1884. Dr. Charles Barrois of Lille. M. Alphonse Briart of Morlanwelz. Professor Hermann Credner of Leipzig. Baron C. von Ettingshausen of Gratz. Dr. E. Mojsisovies von Mojsvar of Vienna. 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 Lg and distributed among the Fellows. 16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. It was afterwards resolved :— That the thanks of the Society be given to Professor J. Prestwich retiring from the office of Vice-President. That the thanks of the Society be given to Colonel H. H. Godwin- Austen, Professor T. M*Kenny Hughes, Professor J. Prestwich, and F, W. Rudler, 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 :— ANNUAL REPORT. 17 OFFICERS. PRESIDENT. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S. VICE-PRESIDENTS. W. Carruthers, Esq., F.R.S. John Evans, D.C.L., LL.D., F.R.S. J. W. Hulke, Esq., F.R.S. J. A. Phillips, Esq., F.R.S. SECRETARIES. W. T. Blanford, LL.D., F.R.S. _ Prof. J. W. Judd, F.R.S. FOREIGN SECRETARY. Warington W. Smyth, Esq., M.A., F.R.S. TREASURER. Prof. T. Wiltshire, M.A., F.L.S COUNCIL. H. Bauerman, Esq. W. T. Blanford, LL.D., F.R.S. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S. W. Carruthers, Esq., F.R.S. Prof. W. Boyd Dawkins, M.A., BR.S: John Evans, D.C.L., LL.D., F.R.S. A. Geikie, LL.D., F.R.S. Henry Hicks, M.D. Rev. Edwin Hill, M.A. G. J. Hinde, Ph.D. John Hopkinson, Esq. W. H. Hudleston, Esq., M.A., ERS. J. W. Hulke, Esq., F.R.S. Prof. T. Rupert Jones, F.R.S. Prof. J. W. Judd, F.R.S. J. E. Marr, Esq., M.A. J. A. Phillips, Esq., F.R.S. W. W. Smyth, Esq., M.A., F.R.S. J.J. H. Teall, Esq., M.A. W. Topley, Esq. Prof. T. Wiltshire, M.A., F.L.S. Rey. H. H. Winwood, M.A. H. Woodward, LL.D., F.R.S. 18 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. LIST OF THE FOREIGN MEMBERS OF THE GEOLOGICAL SOCIETY OF LONDON, mw 1884. Date of Election. 1827. Dr. H. von Dechen, Bonn. 1848. James Hall, Esq., Albany, State of New York. 1850. Professor Bernhard Studer, Berne. 1851. Professor James D. Dana, New Haven, Connecticut. 1851. General G. von Helmersen, St. Petersburg. 1853. Count Alexander von Keyserling, Raykiill, Russia. 1853. Professor L.G. de Koninck, Liége. 1856. Professor Robert Bunsen, For. Mem. R.S., Heidelberg. 1857. Professor H. R. Goppert, Breslau. (Deceased.) 1857. Professor H. B. Geinitz, Dresden. 1857. Dr. Hermann Abich, Vienna. 1859. Dr. Ferdinand Romer, Breslau. 1860. Dr. H. Milne-Edwards, For. Mem. R.S., Paris. 1864. M. Jules Desnoyers, Paris. 1866. Dr. Joseph Leidy, Philadelphia. 1867. Professor A. Daubrée, For. Mem. R.S., Paris. 1871. Dr. Franz Ritter von Hauer, Vienna. 1874. Professor Alphonse Favre, Geneva. 1874. Professor E. Hébert, Paris. 1874. Professor Albert Gaudry, Paris. 1875. Professor Fridolin Sandberger, Wiirzburg. 1875. Professor Theodor Kjerulf, Christiania. 1875. Professor F. August Quenstedt, Tiibingen. 1876. Professor E. Beyrich, Berlin. 1877. Dr. Carl Wilhelm Giimbel, Munich. 1877. Dr. Eduard Suess, Vienna, 1879. Dr. F. V. Hayden, Washington. 1879. Major-General N. von Kokscharow, St. Petersburg. 1879. M. Jules Marcou, Cambridge, U. S. 1879. Dr. J. J. S. Steenstrup, For. Mem. R.S., Copenhagen. 1880. Professor Gustave Dewalque, Lvége. 1880. Baron Adolf Erik Nordenskidld, Stockholm. 1880. Professor Ferdinand Zirkel, Leipzig. 1881. Il Commendatore Quintino Sella, Rome. (Deceased.) 1882. Professor Sven Lovén, Stockholm. 1882. Professor Ludwig Ritimeyer, Basle. 1883. Professor J. S. Newberry, New York. 1883. Professor Otto Martin Torell, Stockholm. 1884. Professor G. Capellini, Bologna. 1884, Professor A. L. O. Des Cloizeaux, For. Mem. BS., Parvs. 1884. Professor G. Meneghini, Pisa. 1884, Professor J. Szab6, Pesth. ANNUAL REPORT. 19 LIST OF THE FOREIGN CORRESPONDENTS OF THE GEOLOGICAL SOCIETY OF LONDON, rn 1884. Date of Election. 1863. Dr. G. F. Jager, Stuttgart. (Deceased.) 1863. Count A. G. Marschall, Vienna. 1863. Professor Giuseppe Ponzi, Rome. 1863. Dr. F. Senft, Evsenach. 1864. Dr. Charles Martins, Montpellier. ; 1866. Professor J. P. Lesley, Philadelphia. 1866. Professor Victor Raulin, Bordeauz. 1866. Baron Achille de Zigno, Padua. 1872. Herr Dionys Stur, Vienna. 1872. Professor J. D. Whitney, Cambridge, U. S. 1874. Professor Igino Cocchi, Florence. 1874. M. Gustave H. Cotteau, Auverre. 1874. Professor G. Seguenza, Messina. 1874. Dr. T. C. Winkler, Haarlem. 1875. Professor Gustav Tschermak, Vienna. 1876. Professor Jules Gosselet, Lille. | 1877. Professor George J. Brush, New Haven. 1877. Professor E. Renevier, Lausanne. 1877. Count Gaston de Saporta, Arx-en-Provence. 1879. Professor Pierre J. van Beneden, For.Mem.R.S., Lowvain. 1879. M. Edouard Dupont, Brussels. 1879. Professor Guglielmo Guiscardi, Naples. 1879. Professor Gerhard Vom Rath, Bonn. 1879. Dr. Emile Sauvage, Paris. 1880. Professor Luigi Bellardi, Turin. 1880. Dr. Ferdinand yon Hochstetter, Vienna. (Deceased.) 1880. Professor Leo Lesquereux, Columbus. - 18806. Dr. Melchior Neumayr, Vienna. 1880. M. Alphonse Renard, Brussels. 1881. Professor EK. D. Cope, Philadelphia. F 1882. Professor Louis Lartet, Toulouse. a 1882. Professor Alphonse Milne-Edwards, Paris. i 1883. M. Francois Leopold Cornet, Mons. 1883. Baron Ferdinand von Richthofen, Leipzig. 1883. Professor Karl Alfred Zittel, Munich. 4 1884. Dr. Charles Barrois, Lille. a 1884. M. Alphonse Briart, Morlanwelz. 1884. Professor Hermann Creduner, Lezpzig, 1884, . Baron C. von Ettingshausen, Gratz. 1884. Dr. E. Mojsisovics von Mojsvar, Vienna. 20 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. AWARDS OF THE WOLLASTON MEDAL ESTABLISHED BY UNDER THE CONDITIONS OF THE “© DONATION FUND” WILLIAM HYDE WOLLASTON, M._D., E.RB.S., B.GS., &e. “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. 1835. 1836. 1837, 1838. 1839. 1840. 1841. 1842, 1845. 1844, 1845. 1846. 1847. 1848. 1849. 1850. 1851. 1852. 1853. 1854. 1855. 1856. 1857. 1858. Mr. William Smith. Dr. G. A. Mantell. M. Louis Agassiz. ae T. P. Cautley. Dr. H. Falconer. Sir Richard Owen. Professor C. G. Ehrenberg. Professor A. H. Dumont. M. Adolphe T. Brongniart. Baron L. von Buch. M. Elie de Beaumont. M. P. A. Dufrénoy. Rey. W. D. Conybeare. Professor John Phillips. Mr. William Lonsdale. Dr. Ami Boué. Rey. Dr. W. Buckland. Professor Joseph Prestwich. Mr. William Hopkins. Rev. Prof. A. Sedgwick. Dr. W. H. Fitton. M. le Vicomte A. d’Archiac. M. E. de Verneuil. Sir Richard Griffith. Sir H. T. De la Beche. Sir W. E, Logan. M. Joachim Barrande. Mee Hermann von Meyer. Mr. James Hall. 1859. 1860. 1861. 1862. 1865. 1864. 1865. 1866. 1867. 1868. 1869. 1870. 1871. 1872. 1873. 1874. 1875. 1876. ES? 7%. 1878. 1879, 1880. 1881. 1882. 1883. 1884. 1885, Mr. Charles Darwin. Mr. Searles V. Wood. Professor Dr. H. G. Bronn. Mr. R. A. C. Godwin-Austen. Professor Gustav Bischof. Sir R. I. Murchison. Dr. Thomas Davidson. Sir Charles Lyell. | Mr. G. Poulett Scrope. Professor Carl F. Naumann, Dr. H. C. Sorby. Professor G. P. Deshayes. Sir A. C. Ramsay. Professor J. D. Dana. Sir P. de M. Grey-Egerton. Professor Oswald Heer. Professor L. G. de Koninck. Professor T. H. Huxley. Mr. Robert Mallet. Dr. Thomas Wright. Professor Bernhard Studer. Professor Auguste Daubrée. Professor P. Martin Duncan. Dr. Franz Ritter von Hauer. Mr. W. T. Blanford. Professor Albert Gaudry. Mr. George Busk. . . | 1831. 1833. 1834. 1835. 1836. 1838. 1839. 1840. 1841. 1842. 1843. 1844. 1845. 1846. 1847. 1848. 1849. 1850. 1851. 1852. 1853. 1854. 1855. 1856. 1857. 1858. 1859. ANNUAL REPORT. 21 AWARDS OF THE BALANCE OF THE PROCEEDS OF THE WOLLASTON “ DONATION-FUND.” Mr. William Smith. Mr. William Lonsdale. M. Louis Agassiz. Dr. G. A. Mantell. Professor G. P. Deshayes. Sir Richard Owen. Professor C. G. Ehrenberg. Mr. J. De Carle Sowerby. Professor Edward Forbes. Professor John Morris. Professor John Morris. Mr. William Lonsdale. Mr. Geddes Bain. Mr. William Lonsdale. M. Alcide d’Orbigny. Cape-of-Good-Hope Fossils. M. Alcide d’Orbigny. Mr. William Lonsdale. Professor John Morris. M. Joachim Barrande. Professor John Morris. Professor L. G. de Koninck. Dr. 8. P. Woodward. Drs. G. and F. Sandberger. Professor G. P. Deshayes. Dr. 8. P. Woodward. Mr. James Hall. Mr. Charles Peach. 1860. 1861. 1862. 1863. 1864. 1865. 1866. 1867. 1868. 1869. 1870. 1871. 1872. 1875. 1874. 1875. 1876. 1877. 1878. 1879. 1880. 1881. 1882. 1883. 1884. 1885. Professor T. Rupert Jones. ie W. K. Parker. Professor A. Daubrée. Professor Oswald Heer. Professor Ferdinand Senft. Professor G. P. Deshayes. Mr. J. W. Salter. Dr. Henry Woodward. Mr. W. H. Baily. M. J. Bosquet. Mr. W. Carruthers. M. Marie Rouault. Mr. R. Etheridge. Dr. James Croll. Professor J. W. Judd. Dr. Henri Nyst. Mr. L. C. Miall. Professor Giuseppe Seguenza. Mr. R. Etheridge, Jun. Professor W. J. Sollas. Mr. 8. Allport. Mr. Thomas Davies. Dr. R. H. Traquair. Dr. G. J. Hinde. Mr. John Milne. Mr. E. Tulley Newton. Dr. C. Callaway. AWARDS OF THE MURCHISON MEDAL AND OF THE PROCEEDS OF “THE MURCHISON GEOLOGICAL FUND,” ESTABLISHED UNDER THE WILL OF THE LATE SIR RODERICK IMPEY MURCHISON, Barr., F.R.S., F.G.S. “To be applied in every consecutive year in such manner as the Council of the Society may deem most useful in advancing geological science, whether by granting sums of money to travellers in pursuit of know- ledge, to authors of memoirs, or to persons actually employed in any inquiries bearing upon the science of geology, or in rewarding any ee 22, PROCEEDINGS OF THE GEOLOGICAL SOCIETY. such travellers, authors, or other persons, and the Medal to be given to some person to whom such Council shall grant any sum of money or recompense in respect of geological science.” 1873. Mr. William Davies. Medal. | 1879. Mr. J. W. Kirkby. 1873. Professor Oswald Heer. 1880. Mr. R. Etheridge. Medal. 1874. Dr. J. J. Bigsby. Medal. 1881. Professor A.Geikie. Medal. 1874. Mr. Alfred Bell. (1881. Mr. F. Rutley. 1874, Professor Ralph Tate. 1882. ProfessorJ.Gosselet. Medal. 1875. Mr. W. J. Henwood. Medal. | 1882. Professor T. Rupert Jones. 1875. Professor H. G. Seeley. 1883. Professor H. R. Géoppert. 1876. Mr.A.R.C.Selwyn. Medal. Medal. 1876. Dr. James Croll. 1883. Mr. John Young. 1877. Rev. W. B. Clarke. Medal. | 1884. Dr. H. Woodward. Medal. 1877. Professor J. F. Blake. 1884. Mr. Martin Simpson. 1878. Dr. H. B. Geinitz. Medal. | 1885. Professor F.Rémer. Medal. 1878. Professor C. Lapworth. | 1885. Mr. H. B. Woodward. 1879. Professor F. M‘Coy. Medal. AWARDS OF THE LYELL MEDAL AND OF THE PROCEEDS OF THE “LYELL GEOLOGICAL FUND,” ESTABLISHED UNDER THE WILL AND CODICIL OF THE LATE SIR CHARLES LYELL, Barr., F.RS., F.G.S. The Medal “to be given annually” (or from time to time) “as a mark of honorary distinction as an expression on the part of the governing body of the Society that the Medallist has deserved well of the Science,”—“ not less than one third of the annual interest [of the fund] to accompany the Medal, the remaining interest to be given in one or more portions at the discretion of the Council for the encou- ragement of Geology or of any of the allied sciences by which they shall consider Geology to have been most materially advanced.” 1876. Professor John Morris. | 1881.. Dr. Anton Fritsch. Medal. 1881. Mr. G. R. Vine. 1877. Dr. James Hector. Medal. | 1882. Dr. J. Liycett. Medal. 1877. Mr. W. Pengelly. 1882. Rey. Norman Glass. 1878. Mr. G. Busk. Medal. 1882. Professor C. Lapworth. 1878. Dr. W. Waagen. 1883. Dr. W.B. Carpenter. Medal. 1879. Professor Edmond Hébert. | 1883. Mr. P. H. Carpenter. Medal. 1883. M. E. Rigaux. 1879. Professor H. A. Nicholson. | 1884. Dr. Joseph Leidy. Medal. 1879. Dr. Henry Woodward. 1884. Professor Charles Lapworth. 1880. Mr. John Evans. Medal. 1885. Professor H. G. Seeley. 1880. Professor F. Quenstedt. Medal. 1881. Sir J. W. Dawson. Medal. 1885. Mr. A. J. Jukes-Browne. ANNUAL REPORT. 23 AWARDS OF THE BIGSBY MEDAL, FOUNDED BY Dr. J. J. BIGSBY, F.B.S., F.G.S. To be awarded biennially “as an acknowledgment of eminent services in any department of Geology, irrespective of the receiver’s country ; but he must not be older than 45 years at his last birthday, thus probably not too old for further work, and not too young to have done much.” 1877. Professor O. C. Marsh. 1883. Dr. Henry Hicks. 1879. Professor E. D. Cope. 1885. M. Alphonse Renard. 1881. Dr. C. Barrois. AWARDS OF THE PROCEEDS OF THE BARLOW- JAMESON FUND, ESTABLISHED UNDER THE WILL OF THE LATE Dr. H. C. BARLOW, F.GS. “The perpetual interest to be applied every two or three years, as may be approved by the Council, to or for the advancement of Geological Science.” 1880. Purchase of microscope. 1884, Dr. James Croll. 1881. Purchase of microscope lamps. | 1884. Professor Leo Lesquereux. 1882. Baron C, von Ettingshausen. 24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Estimates for INCOME EXPECTED. Due for Subscriptions for Quarterly Journal .. 2 0 0 Due for Arrears of Annual Contributions ...... 160 0 0 Due for Arrears of Admission-fees ............ 8116 0 243 16 Estimated Ordinary Income for 1885 :— Annual Contributions from Resident Fellows, and Non- resideritsclSoO to 1SEl Shs) fe. Fe ieee eee 1440 0 0 Ardmission=fees * cs ace ospnc ais we Gta etre ers Ss te 2 «) 282 O-8 Compositions 2) ici. tent oee > ok Shea ee eas 168 0 0 Annual Contributions in advance ...........cceeee 200 2 Dividends on Consols and Reduced 3 per Cents. ........ ea ou Oe Advertisements in Quarterly Journal.............000 cee 510 0 Sale of Transactions, Library-catalogue, Orme- rod’s Index, Hochstetter’s New Zealand, and Pisiorstellows nr ho oa. ae we alee yee G 50"8 Sale of Quarterly Journal, including Longman’s HOCOMME hase Ss att een tee slaletat se te nd ew Math 200 0 0 Sale of Geological Map, including Stanford’s ECCT Tit a ane nee Pn ch acs eres Cees Ceres Sete 15 0 0 — 221 0 O £2581 6 0 THOMAS WILTSHIRE, Treas. 11 Feb. 1885. FINANCIAL REPORT. 25 : the Year 1885. EXPENDITURE ESTIMATED. aad. oe House Expenditure: aes an ERS UYANeG"y...a0aseasesueneneatacs nan << 34 10 0 GRAS AGA weictan’a's saicetionduts acc dank Gitar aie aeemae tae ace 22 0 0 PGE ce, sas seceen cnc adi. et nck teeters 30 0.0 Burniture and Repairs,.......0..0y-pesseeen <5 okie nee nc ne ne ec 163% 02-0 Arrears of Admission-fees.........+.2.. 56 14 0 Admission-tees, $384 “Te Pt ilo ae oe 214 4 0 —— 270 As Arrears of Annual Contributions .................. L5/ vei. iG Annual Contributions for 1884, viz.: Resident Fellows ......... 1415 8 O Non-Resident Fellows ... 18 18 0O 1434556 0 Annual Contributions in advance.................. ay 14 Dividendson Consois.. Vos ee ae DOA. boy aoe Ms Reduced 3 per Cents. ...... 380 8 10 se Ge Taylor & Francis: Advertisements in Journal, Vol.389.. 510 9 Publications : Sale of dournal, Vols: 1=39""..-3.. +2... 2-- 13s AG. 0 = Wel 20 Fp eee ees 80 378 Sale of Library Catalogue ..............-...2+ 2k Sale of Geological Map .............--s0-c0--0- 20 7 8 Salewt Ormerod’s Undex: 3.52.52 -ascsec se ie eI Sale of Hochstetter’s New Zealand ......... 012 0 pale Of Uransachions. ...spc2h2. wc wieneceessscaee 1 4 0 paleter dast of Bellows \..-.2n..c0secs-seeeP-c- 0 3 90 220 13 6 *Due from Messrs. Longman, in addition to the above, on Journal, Vol. 40, &c...............s00000. 66 39. 9 Due from Stanford on account of Geological Map as Gem f 69 10 10 £23889 3.2 We have compared this statement with the Books and Accounts presented to us, and find them to agree. (Signed) W. H. HUDLESTON, J. ARTHUR PHILLIPS, f 4¥27*- 9 Feb. 1885. FINANCIAL REPORT. Year ending 31 December, 1884. EXPENDITURE. 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CROLL OL 00 ee he ee) OL 9T Te * ‘s}ueQ aod g poonpox, UI pajseaut pun] oY} Wo spuoplAly qIOqT VW LOSSeJoLg 0} poprwme [pel POH Iaryltys Jo SOD IL PL TE “PBT Arenuvep [ ‘scoyueg 4v eouvpe "‘SLAIHO WY Joe Tee "SINGWAV 7). ak Aes ‘LNQOOOW isauy, ,,, CNA NOILVNO(T NOLSVTTO AA ,, 29 FINANCIAL REPORT. Ve OL L688F i F Vo Oigeeee. 2 aS ‘SLLAT "PSS ‘tequis00q{ 1 ono oat * £491000 OY} JO ANOAVBF UL QVUUBTe "8ST ‘947 IT "sDa4T, “AMIHSLIIM SVNOHL V OL L688 fs suoUmoNGng pjosum fo eo yoogs pup ‘aunjuung ‘hiouguy ‘sworgoapjoy 2y2 {0 ANIMA 2Y2 APNjOWL 20u sa0p an0gD YT, ‘FN | SY) @ @) woe 23" "(poo pelepistod) SMOTJNI4yM0D TeNUUY Jo sIvoLry Oe Oise ee "(poo porep{sa0o) SOOJ-MOIssIUIPW JO sIvoLIW OL L T80L ¢ @ 9S0I °° ' T6672 "sq red ubee need O} OF 7969" 7. Le G00 eee ee GO ESR ORUUG) aerate 2 —: Ayrodorg popunyy ILS OL ‘ltt P88T 99 TE ‘spuey syreTD Ur soueleg 6 FP SL “ll PEST 20 TE “‘spuey sioyueg Ur souvpeg © © & "***(poos paroprsttoa ) [eUMOL 0} SLaqriosqng Tor; ong i ts ee ie dey Jo yunodoe Uo prloyuVIG Mors ong Pn Peete ene e ns gag Tx ‘TOA ‘TeuIMor Jo yUNOIDe UO “Og 2 UBUSUOTT WOIy ong Yip age i ‘ALULLOUT ALUAIOUd S,ALHIOOG AHL LO NOITLVOTV A L1G Gls Ss | ae 0 & 9 ‘''''' "87000 ted G MON UI poysoATI puny oy} WO spusprlaArlq s| '* *FQ97 reqmmeosq [Se ‘sleyueg ye sourTeG |, G 9 ‘SINTWAV "INQOODYW LSA, 66 ‘SF PRglT Awenuve [ ‘s1oyuvg 4e coueleq ‘SLCIGO MY "aNoq AGsorg ,, KS =) > 30 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. AWARD OF THE WoLLASTON MEDAL. In handing the Wollaston Gold Medal to Dr. W. T. Branrorp, F.R.S., for transmission to Mr. Grorer Busx, F.R.S., F.G.S., the President addressed him as follows :— Dr. BLaANFoRD,— The Council of the Geological Society has awarded to Mr. George Busk the Wollaston Medal in recognition of the value of his re- searches in more than one branch of Paleontology. Polyzoa, not only fossil but also recent, he has made peculiarly his own; and his numerous separate papers, his British Museum Catalogue, and his memoir on the Polyzoa of the Crag, have entitled him to the lasting gratitude of workers at this class of the Molluscoida.. But, perhaps as a relief to the study of these minute invertebrates, he has occu- pied himself, not less successfully, with the larger vertebrata, so that to him we are indebted for much information on the fauna of Post-tertiary deposits, especially from the caves of Malta and of Brixham. Permit me, in handing you this Medal for transmission to Mr. Busk, to express my pleasure at having such a duty to dis- charge, and my earnest hope, in which I am sure all present will share, that restored health may enable him to continue his work in the cause of our science. Dr. BranForp, in reply, expressed his gratification at being selected as the medium for transmitting the Wollaston Medal to Mr. Busx, whose compulsory absence he nevertheless greatly regretted, and from whom he read the following letter :— & 39 Harley Street, W. “Feb. 19, 1885. ‘¢ Dear. Mr. PREsIDENT,— “As, much to my regret and disappointment, I find myself unable to attend the Annual Meeting, I must trespass upon your kindness to express my warmest thanks and best acknow- ledgments for the honour you and the Council have conferred upon me in the award of the oldest of the Society’s Medals, and whose recipients form such a long and distinguished roll, to which any one may indeed be proud to see his name added. ‘The honour, also, in my eyes, is doubly gratifying as being the second testimonial of the same kind, and showing the favourable estimation in which my few labours have been held by the Geo- logical Society of London, whose continued prosperity and useful- ness will always be an object of my warmest wishes. ‘«* Believe me, Yours very sincerely, Gro. Busx.” Prof. T. G. Bonney, #KS. ANNIVERSARY MEETING—-MURCHISON MEDAL. 31 AWARD OF THE WoLLASTon Donation Funp. The Prestpent then presented the Balance of the Proceeds of the Wollaston Donation Fund to Dr. CHartes Catnaway, F.G.S8., and addressed him as follows :— Dr. CHARLES CALLAWAY,— The Council of the Geological Society has awarded to you the balance of the proceeds of the Wollaston Donation Fund, in re- cognition of the value of your researches among the older British rocks. By your identification of Upper Cambrian rocks in Shrop- shire you ‘have placed beyond question the antiquity of the Rhyo- litic group of the Wrekin, our knowledge of which and of yet older rocks in that district you have greatly augmented. Your contribu- tions also to the geology of Anglesey and towards unravelling the stratigraphy of the Scotch Highlands have been of great value, and we look forward to the results of further researches, in aid of which I have great pleasure in placing in your hands the amount of the award. ‘That you receive it from a fellow-labourer will, I hope, make it not the less welcome. Dr. CatLaway, in reply, said :— Mr. PRestpEnt,— I highly value the honour which the Council has seen fit to confer upon me, and [I shall not readily forget the kind words with which vou have accompanied the award. We are told that the reward of virtue is not bread; but bread is a sustainer of virtue: and in like manner, though geology is its own reward, the geologist is conscious of discouragement if the appreciation of his fellow-workers is with- held. JI therefore regard this award as an effective stimulus to future exertion. It is a great pleasure to me to receive it at the hands of one who has so often been a kindly helper in working out difficult problems in lithology. AWARD oF THE Murcuison MEDAL. The Presipent then handed the Murchison Medal to Dr. Henry Woopwarp, F.R.S., for transmission to Dr. Frrprnanp Romer, F.M.G.S., of Breslau, and addressed him as follows :— ~ Dr. Woopwarpd,— The Council has awarded to Dr. Ferdinand Romer the Murchison Medal and a sum of Ten Guineas from the Donation Fund. His life-long and unwearied labours in the service of our science have long since made his name familiar to his fellow-workers. When I state that the Royal Society Catalogue, published now more than — SO 32 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. eleven years since, records the titles of 122 separate memoirs written by him, when I mention his other important works, such as that on the Chalk Formation of Texas, on the Silurian Hanae of Tennessee, on the Geology of Upper Silesia, and the ‘ Letheea Geognostica,’ I have said enough to prove that this memorial of an illustrious geologist could not well have been bestowed on a more illustrious recipient. In transmitting it to Dr. Romer, be so kind as to express our regret that distance and the season of the year have deprived us of the pleasure of his presence on this occasion. Dr. Woopwarp expressed his pleasure at being deputed to receive this Medal for Dr. Ferprvanp Romer, from whom he had received the following letter :— “ Mr. PresIDENT,— “‘T am deeply sensible of the honour which you and the Council of the Geological Society have conferred upon me in presenting me with the Murchison Medal. “T very much regret my inability to be present in order to receive this valuable mark of appreciation from your hands, and to express personally to you my sincere thanks for this high mark of recog- nition which the Society has bestowed on me. “ Tt is particularly gratifying to me that it is the Murchison Medal which you have been pleased to confer upon me, because the greater part of my scientific work has been directed to the study of those ancient rocks, the natural order of which was first recognized by the comprehensive genius of its founder, Sir Roderick Murchison. “Frrp. Romer.” AWARD oF THE MtuRcuison GEoLOoGICAL Funp. In presenting the balance of the proceeds of the Murchison Geological Fund to Mr. Horace B. Woopwarp, F.G.S., the Presipent addressed him as follows :— Mr. Horace B. Woopwarp,— The balance of the proceeds of the Murchison Donation Fund has been awarded to you in recognition of the good service which you hhave already rendered to geology, especially by your work among the later deposits of the eastern counties, and to aid you in further researches. But the excellent papers which you have written, in addition to the work done by you as a member of the Geological Survey, do not constitute your only claim to our recognition. You have made use of the opportunity of your official position to promote a love of science among those who live in our eastern counties, and we are indebted to you for that admirable volume the ‘ Geology of England and Wales,’ which, though in one sense a compilation, is such a one as only a skilled geologist could produce. ANNIVERSARY MEETING——-LYELL MEDAL. 33 Mr. Woopwarp, in reply, said :— Mr. PresrpEent,— IT am highly honoured by this award of the Council which you have now placed in my hands. A little more than twenty-one years ago 1 commenced geological life in the service of this Society, as Assistant in the Library and Museum at Somerset House; and I feel much indebted to that period for acquaintance with many geologists, who, for the sake of my father, extended the hand of friendship to me; and I am likewise indebted to the duties J had then to perform for a knowledge (and I may say a love) of books, which perhaps influenced the production of that volume about which you have spoken so kindly. While labour is in most cases its own reward, it is a great satis- faction and a great encouragement to be told that one’s work is useful by those who are best qualified to judge. _ AWARD oF THE LyEtt MEDAL. The PrestpEnt next presented the Lyell Medal to Professor H. G. Surrey, F.R.S., F.G.S., and addressed him as follows :— Professor SEELEY,— The Council has awarded to you the Lyell Medal and a grant of £A0 in recognition of your investigations into the anatomy and classification of the Fossil Reptilia, especially the Dinosauria. Not that you have limited yourself to this field of research; your papers on Hmys.and Psephophorus, on Megalornis and British Fossil Cretaceous Birds, on Zeuglodon, and on remains of Mammalia from Stonesfield, prove your extensive knowledge of vertebrate palwon- tology, aS your proficiency in invertebrate is evidenced by your earlier work, beth stratigraphical and directly paleontological. Furthermore, your excellent edition of the first volume of Phillips’s ‘Manual of Geology’ indicates an exceptional familiarity with the literature of our science. Since our acquaintance first began, some twenty years since, at Cambridge, we have both had our disappoint- ments and our successes ; you, undiscouraged by the one, unelated by the other, have pushed on to your present high position in science, making no enemies, Winning many friends. I trust that your future career may be even more prosperous than your past, and that this Medal may be an augury of many good gifts of fortune. You will, I know, believe me when I say that I feel an exceptional pleasure in being commissioned to piace in your hands this Medal, commemorative of the great geologist whose philosophic spirit you so well appreciate, and whose memory, I know, you so greatly revere. , 34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Professor SEELEY, in reply, said :— Mr. PREsIDENT,— No words of mine could adequately reflect my sense of the kind words and kind feelings to which you have given expression. I must, however, say that the honour of this award is one for which IT am sincerely grateful. It is needless now to say anything in admiration of Lyell, but I may give utterance to a sense of personal obligation by saying that he has always seemed to me the greatest teacher of our science. In receiving the Medal, however, which is associated with his name, I cannot but be conscious how far short what I have done has fallen of my efforts and aspirations, and that more work than I can hope to do should have been before you in justification. With regard to the new edition of Phillips’s Geology, I would say that that work, founded on the necessities of my own teaching, was undertaken to do honour to the memory of my old friend, Professor John Phillips; but it would have been more imper- fectly done without the important help which I found in your own writings. I shall find in this award a stimulus to future work, which I hope may give results more worthy of recognition than the work to which you have referred. AWARD oF THE LYELL GEoLocicaL Funp. The Presipent then handed the Balance of the proceeds of the Lyell Geological Fund to Mr. J. J. H. Teatz, F.G.S., for transmission to Mr. A. J. Juxes-Brownzt, F.G.S., and addressed him as follows :— Mr. TEeatt,— The balance of the Lyell Donation Fund has been awarded to Mr. A. J. Jukes-Browne in recognition of the excellent work that he has done on the Cretaceous formation and on Glacial geology, and to aid him in further researches. His papers on the Cambridge Greensand cleared up many difficulties connected with that in- teresting formation; and in his Sedgwick prize essay on the Post- tertiary deposits of Cambridgeshire he commenced those inyesti- gations which have since brought us more than one valuable contribution on glacial and later deposits. You can tell him that his old college tutor feels a little pardonable pride and much real pleasure in being the instrument of placing this award in your hands for transmission to him. Mr. Tent, in reply, expressed his regret that Mr. Juxes-Browne was prevented by domestic anxieties from being present, and read an extract from a letter received from him. In this Mr. Juxns- Browne said :— ANNIVERSARY MEETING——BIGSBY MEDAL. 35 ‘That my labours in the field of geology should have been thought worthy of such recognition is most gratifying and encouraging, and I am especially pleased that the award should come from the Lyell Donation Fund; for among all the departed masters of our science there is no one for whom I feel greater respect than for Sir Charles Lyell, or whose mental attitude I more desire to imitate. To be entered therefore on the roll of those who are deemed worthy of receiving the award instituted by Sir Charles Lyell will always be a source of extreme pleasure. . ‘‘T need hardly assure the Council and Fellows of the Society that such strength and powers as I possess will be spent in the service of geological science, because that must be so as long as I am connected with the Geological Survey ; but this mark of their appro- bation will stimulate me in the performance of such extra- official work as I am able to accomplish, and I only wish that my health would allow me to do more.” ' AWARD oF THE Biaspy Gotp MEDAL. In presenting the Bigsby Gold Medal to Professor Rznarp, of Brussels, the Prestpent addressed him as follows :— Professor RrnaRD,— When to a familiarity with geology in the field and a love of nature are united the skill of a finished chemist and the experience ~ of a practised worker with the microscope, the results cannot fail to be of the utmost importance to our science. These qualifications, rarely united in any one man, are in yourself combined with an untiring industry and a love of science for its own sake. Thus we are indebted to you for many important contributions to our know- ledge in geology. Your early memoir “Sur les Roches Plutoniennes de la Belgique et de ’Ardenne Frangaise,” written in conjunction with M. de la Vallée Poussin, will long be classic; your papers on various subjects connected with the Carboniferous Limestone, on the coticule, the phyllites, and other altered rocks of Belgium, and on the deep-sea deposits are too well known to need more than men- tion, and in recognition of these the Council has awarded you the Bigsby Medal. In placing it in your hands may I be allowed to express for myself and others the hope that it will be always a pleasant sowvenir of your many friends on this side of the Channel, some of whom, myself included, will not soon forget the pleasant and, to us, most profitable days spent under your guidance in geological studies by the limestone cliffs of the winding Meuse and the wooded crags of the Ardennes. 36 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Professor Renarp, in reply, said :— Mr. Presmpent and GENTLEMEN,— In rising to express my thanks to you, I labour under a great disadvantage; it would have greatly conduced to my comfort to speak in my own language, but the magnitude of the honour you have conferred upon me makes me feel that I must at all events attempt to address you in your tongue. To hold the Medal which you have awarded to me is no common distinction. I cannot but feel that you are rating my merits more highly than they deserve. Though not an Englishman, I never feel myself a stranger in your country. I have visited it so often, and had so much friendly intercourse with your scientific men, that I am not altogether without misgiving that your Council. may, uncon- sciously to themselves, have supplemented my deficiencies as a geologist by their personal friendliness towards myself. ‘The par- ticular line of study to which I have devoted myself is essentially English. Your countryman, Sorby, was the pioneer of microscopic lithology, and I have only followed the track which he was the first to open up. In conclusion, allow me to say that though sensible of my own deficiencies, | am confident that your good opinion will stimulate me to fresh exertions. I shall pursue my scientific work with renewed energy, and it will be my constant endeavour to show you that your confidence was not altogether misplaced, and make myself in the future worthy of the great honour you have conferred upon me. ANNIVERSARY ADDRESS OF THE PRESIDENT. 37 THE ANNIVERSARY ADDRESS OF THE PRESIDENT. Pror. T. G. Bonnzy, D.Sc., LL.D., F.R.S. GENTLEMEN, In referring last year to the muster-roll of death, your Presi- dent remarked that it contained the name of only one Fellow who had been a contributor to our publications. Unhappily I am unable to repeat the remark. “Earnest workers and valued friends during my year of office have been falling “thick as autumn leaves in Valombrosa.” It is now my melancholy duty to pay to these the last tribute of respect, and dwell for a brief space on their memory. In Rozsert Atrrep Croryne Gopwiy-Avsten we have lost not only a geologist of extensive knowledge and of an exceptionally philosophic mind, but also one of the links which united us with what we may almost call the “ heroic age” of British Geology. He was born at Shalford House, near Guildford, on March 17, 1808, being the eldest son of the lateSir H. E. Austen. Educated first at Midhurst School, he afterwards spent some time at a military college in France. Thence he proceeded to Oxford, where he graduated and was elected a Fellow of Oriel College. Coming thus under the influence of Buck- land, he was secured for geology, and was elected a Fellow of this Society in the year 1830. Three years afterwards he married the only daughter and heiress of the late General Sir H. T. Godwin, K.C.B., and on the death of that officer in 1854, prefixed the name of Godwin to that of Austen. Devonshire was the scene of his earlier geological labours ; for not long after his election to this So- ciety he fixed his residence at Ogwell House, near Newton Abbot. His first contribution to our publications was made in 1834, and for the next six years Devonshire formed the chief subject of his writings. The first paper relating to the south-east of England appears in the ‘ Proceedings’ for 1853, and after his removal from Devonshire to Chilworth Manor, near Guildford, the Cretaceous and Tertiary deposits, together with physical questions relating to the geology of the Channel and its vicinity received a large share of his attention, although Devonshire was not forgotten. Mr. Godwin Austen was elected a Fellow of the Royal Society in 1849. Hereceived various distinctions from Foreign Societies; and the Wollaston Medal was awarded to him in 1862.. Mr. Godwin-Austen was also an energetic Member of the British Association, and twice, at Norwich and at Brighton, presided over the Geological Section. For the greater part of his life his connexion with the Geological Society was of the closest kind; a large number of his papers were contributed to our publications ; he served as one of the Secretaries ; subsequently he was in office as Foreign Secretary and as a Vice- President; and it is well known that, had he been willing, the VOL. XLI. , is 38 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Society would have gladly elected him President. He finally quitted the Council in 1876, about which time his health became much impaired, and he was afterwards unable to take any active part in our meetings or in our work. After a lingering illness, he expired on the 25th November last, to the regret of all who enjoyed the privilege of his friendship. The name, however, of Godwin-Austen will, fortunately, not disappear from our lists, for the personal infiu- ence and the scientific ability of the father have been transmitted to his son, our friend Colonel Godwin-Austen. Of the contributions to science of the late Mr. Godwin-Austen it is impossible, within the brief space allotted to these notices, to give any adequate idea. A list of 39 papers is appended to a biography by Mr. H. B. Woodward (to which I am much indebted), published in the ‘ Geological Magazine’ for January last. In addition to these, he edited the Memoir on the Fluvio-marine Tertiaries of the Isle of Wight, left in manuscript by its lamented author, the late Professor HK. Forbes, and completed the ‘ Natural History of the European Seas,’ commenced by the same author. The whole book, after p. 126, is the work of Mr. Godwin-Austen. He also made important con- tributions to the new edition of the ‘Greenough Geological Map,’ published in 1865. His papers on the classification and correlation of the rocks of Devonshire will ever be classic in the history of that most difficult region. Mr. Godwin-Austen, as is well known, objected to the distinction of the fossiliferous rocks beneath the Culm-measures by the title of Devonian, and to the equivalence assumed between these and the Old Red Sandstone further north, considering the latter to be more nearly connected with the base of the Carboniferous series, and the former as the representative in time of the Upper Silurian, the differences of the fauna being regarded as due to the two being deposited in different and separated marine areas. Although the general tendency of subsequent research has been unfavourable to the view upheld by Mr. Godwin-Austen, still it is one which can- not wholly be neglected, and modifications in the direction of it seem likely to be made in the generally receivedtheory. But on whatever question Mr. Godwin-Austen wrote, whether on nodules in the Faringdon Sands or on boulders in the Chalk, whether on superficial or subterranean geology, whether on the physical features of the present or of past geological epochs, he not only adorned it by a clear expository style and a lucid ordering of facts, but by his philo- sophic treatment, as it were, raised the subject to a higher plane of thought. Preeminently ‘‘the physical geographer of bygone periods,” as he was most happily termed by Murchison, we may apply to him the well-worn but, in his case, most true phrase, nzhil tetigit quod non ornavit. One paper only from his pen I will, in conclusion, espe- cially mention, because, to my mind, it is most typical of all his work, namely, that ‘‘ On the Possible Extension of the Coal-measures beneath the South-eastern parts of England.” To myself, when first I read it years ago, it was like a revelation ; it showed what strati- graphy might become when it was viewed in a comprehensive spirit, ANNIVERSARY ADDRESS OF THE PRESIDENT. 39 and its facts were handled by a master in science: it proved the possibility of deciphering the physical history of the earth, even as its life-history was being reconstructed by the inductive labours of the paleontologist; so that we might hope to behold with our mental vision not only the strange forms which in long-past days had tenanted its waters and had moved upon its lands, but also the shores and the currents of its seas, the ridges and perhaps the moun- tains of its continents. Tomas Wricur was born at Paisley, in Renfrewshire, on Novem- ber 9, 1809, and educated at the Grammar School in that town. After completing his articles with a surgeon, he enteredas a student in the Royal College of Surgeons at Dublin, and was soon distinguished for his proficiency in anatomical and physiological studies ; these, however, were interrupted by the injurious effect of adissecting wound. This obliged him to decline an appointment which offered a prospect of a scientific career. After his restoration to health, he passed the College of Surgeons in the year 1832 and shortly afterwards entered upon the duties of his profession at Cheltenham, graduating as Doctor of Medicine at St. Andrews in 1864. His life was spent in active work, professional and scientific, in this pleasant Gloucestershire watering-place, where he held various appointments, among them that of Surgeon to the General Hospital. But the duties of his pro- fession were not incompatible with an energetic pursuit of science. At first he devoted much time to microscopic work, but as this threatened to injure his eyesight, he turned his attention to paleon- tology. For this study the neighbourhood of his home then offered exceptional facilities, the numerous shallow excavations, many of comparatively ancient date, affording opportunities to the collector which can never again occur. Dr. Wright thus amassed a magnifi- cent collection of Jurassic Echinodermata and Cephalopoda, which, I regret to learn, has not found a resting-place in his own country. He published several papers on the former Order in the ‘ Proceedings of the Cotteswold Field-Club’ and the ‘Annals and Magazine of _ Natural History,’ which attracted the attention of Professor Edward Forbes. Before long it was arranged that, while the latter under- took to describe for the Paleeontographical Society the British Creta- ceous and Tertiary Echinodermata, Dr. Wright should do the same with the Jurassic. But the premature death of Forbes before he had commenced upon the Cretaceous Echinodermata, caused the Council of the Palzontographical Society to request Dr. Wright to undertake an additional labour and carry into effect the purpose thus left incomplete. The description of the Jurassic and Cretaceous Echinodermata occupied him for the greater part of his life, portions of the work appearing from the year 1855 to 1882; but in 1878 he commenced a description of the Lias Ammonitide, which was barely completed at the time of his death. Dr. Wright was the author of about thirty-two separate papers on geological subjects, of which seven were contributed to our Journal ; - but the volumes above mentioned are the great work of his life and f2 i 40 : PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | : an enduring monument of his extensive knowledge and energetic 1 industry. He was zealous in promoting, by lectures and every ! personal effort, the advancement of science in his own neighbour- i hood. He was elected a Fellow of the Royal Society of Edinburgh | in 1855, of this Society in 1859, and of the Royal Society of London y in 1879, and he received acknowledgments from several foreign scientific societies. The Wollaston Medal was awarded to him in 1878. His health began to fail nearly a year ago, and, after a lingering illness, he expired on November 17th last. But even suffering could not quench his enthusiasm for science. One evening, some months since, when death seemed to be very near, he roused himself ~ and set to work on the revision of a proof-sheet, determined that, so far as lay in his power, he would not leave his task unfinished ; and the last letter which he ever wrote was on the occasion of pre- senting to the Society a lock of Dr. William Smith’s hair. He was not rarely present at various scientific gatherings, where his stalwart form, cast In northern mould, distinguished’ him from the crowd, while his hearty tones and his genial manners made him ever a welcome guest. Those who have had the privilege of his friendship valued him not only for his great special knowledge, but also for his wide general culture and his sincere earnestness of character. SEARLES VALENTINE Woop was born on February 4, 1830. Son of a geologist, Searles V. Wood, Senior, our former Fellow, so well known, to mention but one thing, for his great work on the Plio- cene Mollusca, his attention was early directed to this science, and a community of interest, doubtless, formed one of the ties which bound father and son with a more than common affection. On the death of the former, his son undertook the duty of Treasurer to the Paleontographical Society, with which the two names will ever be inseparably connected. Mr. Searles Valentine Wood was brought up to the law, and practised for some years as a solicitor at Wood- bridge, in Suffolk, but ultimately gave up his profession in order that he might devote himself wholly to scientific work. Tertiary and Post-tertiary geology was the chief subject of his study ; and in 1864 he undertook, in company with Mr. Harmer, a careful examination of the Pliocene and later deposits of the east of England. These were all laid down with conscientious minuteness on the Ordnance Survey Map, Mr. Searles Wood taking as his share Essex and nearly the whole of Suffolk. The result of this work, so far as relates to the Newer Pliocene deposits (as they were termed by Mr. Wood), has been communicated to this Society in two elaborate memoirs, pub- lished in the volumes for 1880 and 1882. But numerous minor papers, in addition to these, were the result of Mr. Wood’s untiring industry. Of course, in questions so difficult as are almost all those relating to the so-called Glacial Period, it is not to be expected that every conclusion of Mr. Wood’s will find acceptance with his fellow > = ANNIVERSARY ADDRESS OF THE PRESIDENT. 41 workers ; but all must admire and gratefully recognize his patience and industry in the collection of facts. For some years before his death his health was grievously im- paired, but neither infirmity nor debility, nor even pain, could turn him from his beloved studies. His last contribution to our Journal, read at the opening meeting of the present session, was on the remarkable fossiliferous Tertiary deposit, not long since discovered, at St. Erth, near Penzance. A portion of that paper is printed in the current number of our Journal; but Mr. Searles Wood, in deference to the advice of friends, withdrew the list of species which he had given, in order that he might again present it with full descriptions of the more novel or more important forms. It will be remembered that, in the interesting discussion which followed, Dr. Gwyn Jeffreys spoke at some length against the view favoured by Mr. Wood as to the general equivalence of the deposit with some part of the Red Crag. We little thought then that in so brief a space both these accurate observers would have ceased from their labours. In concluding this too brief notice of a most earnest worker and most amiable man, I shall venture to quote a few sen- tences from a letter to Professor Judd, written by Mr. Searles Wood only a few days* before his death, because it seems to me to give unconsciously a far better portrait of the man than I could hope to draw. Speaking of a recent severe attack from which he had in part recovered, but which was complicated by an ailment in one foot, he adds :—‘‘ This compels me to maintain a recumbent posture all day as well as night, but it has not prevented my renewing my close examination of the St.-Erth clay for several hours a day. This clay, however, is so sterile that I often work for days without finding a perfect shell or a fragment worth anything for determination ; and I fancy that no one who had not perforce the leisure that I have, and a rather exceptional perseverance, would work at it as | am doing, and as I hope for many months yet to do.” It was not so written : eight days later he passed away. Joun Gwyn Jerrreys was born at Swansea on January 18, 1809, and early displayéd a talent for natural history. At the age of nineteen he contributed to the Linnean Society a paper on the Pneumonobranchous Mollusca; and the study of this class formed at first the relaxation and afterwards the work of his life. He was elected a member of the Linnean Society in 1829, and of the Royal in 1840, not joining our Society until the year 1861. He was also an active member of the British Association, in which he held various offices, and in 1877 that of President of the Biological Section. At the last meeting, at Montreal, he contributed a valuable communication on the Mollusca of the two sides of the North Atlantic, which is being printed in ewtenso in the volume for 1884. From the University of St. Andrews he received the honorary degree * Dated December 6, 1884. a 42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. of LL.D. He was educated as a solicitor, and for many years practised with much success at Swansea; but in 1856 he was called to the bar, and soon afterwards retired from business. He then settled at Ware Priory, in Hertfordshire, at which pictu- resque old mansion he resided till about four years since; thence, shortly before the death of his wife, he removed to London, and took a house at Kensington, where he died in consequence of an apoplectic seizure on January 24, after only a few hours’ illness. On the previous evening he had been present at a lecture given by his son-in-law, Professor Moseley, at the Royal Institution ; and he was among us at the Council-table, at the Geological Club, and at the Evening Meeting on the last occasion prior to his death. Indeed his mental powers showed no signs of failure, and a slight increa- sing difficulty of hearing was almost the only indication that he had numbered full 76 years. The study of the recent Mollusca was the chief scientific work of Dr. Gwyn Jeffreys’s life. He was one of the first to perceive the importance of dredging in the British seas; and after many years’ experience in private enterprise, took charge, in 1869 and 1870, of the scientific work on board the ‘ Porcupine’ during two of her cruises. Hence Dr. Gwyn Jeffreys’s best scientific memorial will be his writings on the Mollusca, chief of which are his large and important work on British Conchology, and the papers, unfortunately left unfinished at his death, on the “ Mollusca of the ‘ Lightning’ and ‘ Porcupine’ Expeditions,” published in the ‘ Proceedings’ of the Zoological Society; but his exact knowledge of recent forms gave his opinion an exceptional value on the fossils of the later Tertiary deposits, and on these subjects he has communicated papers, more valuable than numerous, to our Journal. But his other services to our Society must not be forgotten. For sixteen years he was its Treasurer, a position for which he was peculiarly adapted by his legal knowledge and habits of business, and the duties of which he fulfilled with great assiduity and invariable courtesy. He resigned that office four years ago, but at the time of his sudden death was still a member of the Council, having served on it continuously for twenty-one years. We shall for long miss his critical acumen and extensive knowledge. especially in any question relating to the later life-history of the earth; but we shall even more deeply regret the cheery, kindly friend, and the trusty adviser, who for so many years has been a familiar figure at these and many other scientific gatherings. Atrrep Tytor was born on January 26,1824. His parents were members of the Society of Friends, and he was educated in schools connected with that body at Epping and Tottenham. At the age of fifteen, however, he entered the manufactory of brass and copper work belonging to his family in Warwick Lane. This early diversion from school to practical work was for Mr. Tylor the beginning rather than the end of his education. While singularly successful as a practical man of business, not only in the above factory, but also in ANNIVERSARY ADDRESS OF THE PRESIDENT. 43 the colliery owned by his family at Tylorstown, in the Rhondda Valley, he found time to study anatomy for a period at St. Bartho- lomew’s Hospital, and afterwards to become an accomplished geolo- gist. But even this was not all: he was an earnest advocate for technical education, and devoted no small portion of his time to various duties outside his own business. He is the author of not a few papers, published in our Journal and elsewhere ; and it may be mentioned that he was one of the first to doubt the authenticity of the celebrated Moulin-Quignon jaw. His most important and ela- borate papers are devoted to questions connected with the action of rain, rivers, and ice; and he may be regarded as the author of the name “ the Pluvial Period.” Whatever opinions may be held as to the advantage of giving a special designation to the transitional interval between the Glacial epoch and that when the climate of the northern hemisphere finally arrived at its present condition, all must admit that Mr. Tylor did excellent work in drawing attention to the heavier rainfall which must have formerly prevailed, as well as in noting many interesting facts with regard to the various fluviatile deposits. His health failed during the last two or three years of his life, overmuch work having brought on renal disease ; but, notwith- standing his malady, he was able to visit America in the autumn of 1884. On his return, however, his strength rapidly declined, and he died on December 31, “not so much from specific disease as from a collapse of the whole framework of life.’ He was married in 1850, and has left a widow and six children. It will be long before some of Mr. Tylor’s work is forgotten in the annals of geology; but he has left another—may I not say a better ?—monument in the regretful affection of many friends of his own standing, and in the enduring gratitude both of those less prosperous than himself, whom he liberally aided, and of not a few members of a younger genera- tion, to whom, before they could help themselves, he held out a hand to give them that greatest boon, a fair chance in life. James Buckman was born at Cheltenham in the year 1814. Designed for the medical profession, he studied in London, but not liking it, he returned to Cheltenham and commenced business as a chemist. But while in London he had evidenced a predilection for science, and had made a considerable collection of plants then found in the vicinity of the metropolis. In the year 1842 he was appointed to the curatorship of the Birmingham Philosophical Institute, where he remained till his election as Professor at the Agricultural College at Cirencester. There he worked assiduously for sixteen years, retiring in 1863 to a farm at Bradford Abbas, in Dorsetshire, where he died on November 23, 1884. He wrote a large number of papers on archeology, botany (especially agricultural), and geology, some of the last being contributed to our Journal; these dealt with questions concerning the paleontology and stratigraphy of the Jurassic series of the districts with which he was most familiar; the last, published in the 37th volume of our Journal, being ‘“‘ On the terminations of some Ammonites from the Inferior Oolite of Dorset and Somerset.” 44 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Ricuarp ATKINson Pracock, formerly of Lancaster and St. Helier’s, Jersey, died in London on February 2, 1885, aged 74. A civil en- gineer by profession, he took a great interest in geology, especially devoting himself to the causes of volcanic eruptions and earthquakes, and to the evidence of alterations in the level of the land in historic times. In the former he regarded saturated steam as the motive power, and on this subject he published at least one work. He was the author of a book on the sinking of the north and west coasts of France and the south-western coasts of England, published in 1868, and in the year 1876 read two papers before cur Society on sub- sidence in Jersey and Guernsey respectively. lt is to be hoped that the latter subject will not cease to attract notice now that we have lost Mr. Peacock, for it-is one of much interest. I may, however, remark that for its investigation the acumen of the his- torical critic is even more necessary than the knowledge of the geologist. Quintino Sez, elected a Foreign Member of this Society in 1881, died March 15, 1884. An admirable mineralogist and a sound geologist, a man successful alike in private and in public business, an accomplished statistician, statesman, and Minister of Finance, his death fell heavily on many circles and on many societies. To us he was known as a mineralogist, who, had he devoted himself wholly tothat study, would have attained a place among the very foremost of the time; to another band of Englishmen his name was familiar as the President of the Italian Alpine Club; to others, again, as the President of the Academy of the Lincei at Rome; to those without our scientific societies, as the successful Minister of State and the restorer of his country’s finances to a comparatively sound condition. Our generation has seen but few men of versatility so great, industry so untiring, and success so varied, few who could have been more widely regretted abroad or more deeply mourned at home. Hetrice Ropert Goprert, M.D., Ph.D., Professor of Natural History in the University of Breslau, died on May 15, 1884, at the advanced age of 84. He was elected a Foreign Member of our Society in 1857, and in 1883 was awarded the Murchison Medal in recognition of his labours in fossil botany. He was a man of unwearied industry, 245 papers from his pen being recorded in the List of the Royal Society, the first of them dating from 1828; his last work ‘On the Flora of Amber,’ a quarto volume, was published at Danzig in 1813, and an advance copy was forwarded to this Society, and laid on the table at the Anniversary meeting, when the Murchison medal was handed to his representative. In 1846 he received from the Academy of Sciences at Haarlem a gold medal and an award in money for his memoir on the Carboniferous Flora. The little band devoted to that most important but rather neglected branch of our science, Paleobotany, will feel that the disappearance from their ranks of Heinrich Robert Goppert is a loss not to be lightly repaired. ANNIVERSARY ADDRESS OF THE PRESIDENT. 45 Ferpivanp von Hocusrerrer, son ofaclerical professor at Esslingen in Wirtemberg, was born on April 30, 1829. Destined at first for his father’s calling, he was led by his love of nature to adopt a scientific career, and studied at Tiibingen under Prof. F. A. Quenstedt. After taking his doctor’s degree, he proceeded to Vienna, where he made the acquaintance of Haidinger, and from 1853 to 1856 was employed on the geological survey of Bohemia. In the following years Hochstetter was absent from his native land, being engaged as one of the scientific staff on the well-known voyage of the ‘ Novara,’ during which he quitted the ship for a time in order to study the geology of New Zealand and visit the Australian gold-fields. The results of his explorations are published in the first volume of the geological section of the work describing the expedition of the ‘Novara;’ and Dr. Hochstetter was also joint author of the small volume on New Zealand, a translation of which is in the possession of this Society. On his return he was suc- cessively Professor at the Vienna Imperial Polytechnic Institute, and Director of the United Imperial Museum of Natural History, in both of which he reorganized the collections. In 1880 he was elected a Foreign Correspondent of this Society. He was the author of alarge number of separate papers and memoirs on mineralogical and geological subjects, besides a ‘Manual of Crystallography’ and one on Mineralogy and Geology; and he was the means of discovering pile-buildings and other remains of a prehistoric race on the margins of the lakes of Carinthia. Dr. Hochstetter was much esteemed by the Imperial family of Austria, and numbered the Prince Imperial among his pupils. His health had been for some time in a failing condition, and he died, much regretted by all who knew him, on July 21, 1884, leaving the reputation of an admirable geo- logist and an indefatigable worker. The long and melancholy list is not yet ended. We lament, in sympathy with our geological brethren across the Atlantic, ALEXANDER Murray, member of the Canadian Survey, to whom we are indebted for most of what we know of the geology of Newfoundland. We have lost also from the list of Members who have contributed papers, Mr. T. Curtey and Mr. Joszru Cotruvrst, and but two days since came the heavy news of the death of Mr. J. F. Campperz. Born December 29, 1821, the eldest son of Walter F. Campbell, Laird of Islay, and cousin of the present Duke of Argyll, his prospects early in life were darkened by the loss of the family property during his father’s lifetime, and thus he found himself, immediately after attaining his majority, thrown upon his own resources. This trial was borne with a quiet magnanimity which gained him the admi- ration of his kinsfolk and friends. He was called to the Bar, but never practised. From 1854 to 1860 he was successively Private Secretary to the Duke of Argyll and Secretary to the Board of Health, the Mines Commission, and the Lighthouses Commission, and from 1861 to 1880 he held office in Her Majesty’s household. In the intervals of the above duties he travelled much. Iceland and % 46 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Scandinavia were more than once visited. In 1864 he went to America, describing the journey in ‘A Short American Tramp,’ published in 1865. In 1873-74 he travelled through the north of Europe to Archangel, thence through Russia to the Caucasus, and home by Constantinople and Southern Europe. In 1874-75 he made the journey round the world described in ‘ My Circular Notes ;’ and at later periods spent some time in India, Syria, Palestine, and Egypt. He contributed to our Journal papers on glacial subjects, and wrote also on the Parallel Roads of Lochaber and on the Gold Diggings of Sutherland. In addition to this he was an authority on Scottish Folk Lore. By geologists, however, he wiil always be best remembered in connexion with his book entitled ‘ Frost and Fire,’ published in 1865, a work which bears evidence of his skill as an artist and accuracy as an observer, is full of quiet and quaint humour, is delightfully written, and, even when not convincing, is none the less suggestive. His loss will be deeply felt, for he bore equally well adverse and prosperous fortune, and “ where he was best known, there he was also best loved.” The papers which have been presented during the last session have not, I think, been inferior in number or in interest to those of the preceding one. As in that, papers more or less stratigraphical have preponderated, and no lack of interest appears in those questions where the petrologist goes hand in hand with the field-worker ; thus rocks igneous and rocks Archean have received a large share oi attention. Dr. Callaway read an elaborate paper bearing upon the relations of the older rocks of Anglesey. His assignment of certain fossiliferous strata to the Ordovician, rather than to the Cambrian, did not seem to command the suffrages of other workers in the same field ; but it will be difficult, I think, to gainsay the evidence in favour of the Archean age of the crystalline schists and so-called granites, which he brought forward in corroboration of that laid before you last year. Mr. Hill broke ground in a field comparatively new, whose rocks have long called for investigation by the more accurate modern methods, in his paper on the rocks of Guernsey. My predecessor suggested, in his address last year, that there would be better chance of controversialists coming to an agreement on the difficult questions involved in the geology of the Archzan rocks, could they meet for discussion upon the ground. Provided that due precautions could be taken for preventing the melancholy consum- mation which was fatal to a well-known scientific society, there would be much, I think, in favour of this “ trial by a mixed commis- sion.” But pending any such gathering of the clans on the Pebidian moorland, Dr. Hicks laid before the Society his rejoinder to the criticisms made in the previous session by the Director-General. As the forces of Jermyn Street had been concentrated on him, he not unnaturally sought the alliance of others, and Mr. T. Davies’s petrological appendix to Dr. Hicks’s paper forms a valuable contr- bution to the history of these interesting Pembrokeshire rocks. Some ANNIVERSARY ADDRESS OF THE PRESIDENT. 47 x of the questions involved in this controversy cannot be settled in the present state of our knowledge; but on two of great importance, the two most vital to his theory, viz. the great antiquity of the so-called Dimetian rocks and the separability of the Pebidian from the Cambrian, Dr. Hicks brought forward evidence which it is difficult to gainsay. Henceforth it will, I think, be admitted that the Dimetian cannot be regarded as an intrusive igneous rock of Paleozoic age; and that the Pebidian has, stratigraphically, at least as good a claim to be considered a distinct formation as the Lower Silurian of the Survey. In anticipation of the meeting of the British Association in Canada, we received an excellent summary of the geology of the district traversed by the Canadian Pacific Railway from our old friend Principal Dawson, who is always a welcome visitor on this side of the Atlantic, and in whose well-earned additional dignity we all rejoice. Professor Green proposed a new reading for a well-known but admittedly difficult section at Llanberis. Mr. J.J. H. Teall has added to his reputation by his thorough and exhaustive paper “‘ On the Chemical and Microscopical Characters of the Whin Sill,” and that “On the Conversion of a Dolerite into Hornblende-schist.” Professor Judd has found time amidst his pressing duties to give us another instalment of his investigations in Scotland in the paper read at our last meeting ‘‘ On the Tertiary and older Peridotites of the Western Islands,” a paper which will not only add largely to our knowledge of some very interesting rocks, but also be a most suggestive one to the petrologist. At an earlier meeting in my year of office Professor Judd also presented a supplement to his important paper on the Rich- mond boring, when contributions were read by Prof. Rupert Jones on the Foraminifera and Ostracoda, by Dr. G. J. Hinde on the Calci- spongie, and by Mr. G. R. Vine on the Polyzoa obtained from the cores. A paper dealing with a cognate subject and of hardly less interest was that by Mr. J. Eunson on the range of the Paleozoic rocks beneath Northampton. The author laid before us the details cf four borings in the Northamptonshire area, of which three had been observed by himself. At Kettering Road, one mile N.E. of Northampton, after passing through beds of the Inferior Oolite and the whole thickness of the Lias, about 67 feet of strata were traversed, which might repre- sent some part of the Trias, after which beds of the Carboniferous series were struck at a depth of 805 ft. 6 inches and pierced for about 45 ft. At Gayton the beds assigned to the Trias were 61 feet in thick- ness, and these were followed by beds of more dubious age for 22ft. 6 inches, after which indubitable Lower Carboniferous Limestones and Shales were traversed for 190 feet, and were followed by red grits and marl, pierced for a depth of 105 feet. These rocks, be they Lower Carboniferous or Old Red Sandstone, or yet earlier, are certainly made up, in part at least, of the ruins of granitoid rocks, and.are interesting as throwing light upon the probable source of many fragments of reddish grit in the Trias of the north-east of England. It seems to me not impossible that rocks similar in composition to these may have helped to constitute the ancient uplands which probably formed the eastern boundary of the river-valley in connexion 48 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 4 with which the lower members of the Trias were deposited. In the third boring at Orton, 12 miles N.E. of Northampton, only about 24 feet of rock occurred which could be possibly referred to the Trias, shortly after which a quartz-felsite was pierced, very similar in all respects to the rock at High Sharpley (Charnwood Forest), which I was formerly inclined to refer to an altered rhyolitic ash, but now feel more disposed to regard as a true lava, once glassy, but now devitrified, greatly crushed by subsequent pressure. The remaining stratigraphical papers are not very numerous, and mostly rather brief. That by Mr. Downes on the Cretaceous beds at Black Ven has considerably augmented our knowledge of the basement-beds of the Chalk in the western area of Britain. Those by Mr. Starkie Gardner on the plant-bearing deposits in connexion with the basalts of Ireland and Iceland appear likely, when the whole evidence is published, to raise questions of importance as to the age of these deposits ; and to the extremely interesting paper by Mr. Searles Wood on the no less problematical deposit at St. Erth, I have already referred. Mr. Lamplugh added largely to our knowledge not only of the fauna, but also of the stratigraphy of the interesting fossiliferous deposit associated with Boulder-clay at Bridlington. Boulder-clays themselves have been the subject of papers by Mr. Mellard Reade and Mr. Jukes-Browne; an inter- esting paper by Col. Godwin-Austen and Mr. Whitaker on a new railway-cutting at Guildford dealt with Post-tertiary as well as Tertiary geology; and Mr. Pidgeon brought us up to historic time by his communication on the submerged forest at Torbay. On paleontology, we have had the pleasure of receiving three papers from our “ Nestor ” in that branch of geological study, Sir R. Owen. In that on Rhytidostews capensis, from the so-called Trias of the Orange River Free State, he directed our attention to certain mammalian characters in the Labyrinthodont Amphibians, and in a later communication pointed out the resemblance between the teeth of the South-African Tritylodon, described last year by him and assigned to the Mammalia, and those of the Kocene mammal, Neo- plagiaulax. In a third paper he described a portion of a skull of a youthful Elephas antiquus from Creswell Crags. Mr. KE. T. Newton introduced to our notice a new species of Gazelle from the Forest bed; Mr. Miall described a fine specimen of Megalichthys from the Yorkshire Coal-field; and Prof. E. W. Claypole showed that in America he had detected the remains of Pteraspidian fishes at a lower geological horizon than they are known to occur in Britain. A new species of Conoceras has been described by a new contributor, Mr. T. Roberts; and Mr. Walford has given us a second of his carefully worked-out essays, in that “ On the Stratigraphical Position of the Lower and Middle Jurassic Trigonie of North Oxfordshire and adjoining districts.” Mr. Vine has treated of the Cretaceous Lichenoporide, and Prof. Duncan, Mr. Champernowne, and Mr. Tomes of various corals. Professor Hughes has reduced the number of extinct creatures by destroying Spongia paradoanca ; while Dr. Hinde has shown us that it is possible to understand ANNIVERSARY ADDRESS OF THE PRESIDENT. 49 even such a difficult family as the Receptaculitide. We received only one palobotanical paper, strictly speaking, namely, that by Mr. Kidston, on Zeilleria and other forms belonging to the old genus Sphenopteris. In addition to these, several papers were read on geological subjects without the limits of the United Kingdom, dealing with localities not only on the continent of Europe, but also in regions so remote as Japan, Australia, and New Zealand. Turning for one moment from the work of our Fellows, as evidenced in our Quarterly Journal, we may assert with just pride that in other quarters also the intellectual activity of the Society exhibits no symptom of decline. Many by their contributions have aided Dr. H. Woodward in maintaining the high standard of that most valuable periodical the Geological Magazine, whose coming of age ought to be celebrated this year. The annual volume of the Palzontographical Society, edited still, as it has been so long and so well, by our Treasurer, Prof. Wiltshire, more than keeps up its high reputation, and both deserves and needs the support of all geo- logists. In it Baron von Ettingshausen and Mr. J. Starkie Gardner continue their work on the Eocene Flora; Professor Rupert Jones, with his collaborateurs Messrs Kirkby and Brady, neither of whom have we the pleasure of counting among our Fellows, conclude their monograph on the Carboniferous Entomo- straca; Dr. Woodward completes the description of the Carboniferous Trilobites; Mr. Davidson, the supplement to the British Brachiopoda, bringing thus to an end, at any rate for a time, a work of inestim- able value to every student of geology; and the volume ends with the seventh part of the description of the Ammonites of the Lias, the last contribution which we shall ever receive from the pen of our departed friend Dr. T. Wright. Mr. Bauerman has published a most useful ‘ Manual of Systematic Mineralogy,’ thus completing his treatise on the subject. The large and exhaustive volume on ore- deposits entitles Mr. J. A. Phillips, our Vice-President, to the gratitude of all students of that difficult branch of our science ; Professor P. M. Duncan has revised and augmented the fourth edi- tion of Sir Charles Lyell’s ‘Student’s Manual of Geology ;’ and the first volume of the late Professor Phillips’s ‘Manual of Geology,’ treating of Physical Geology and Paleontology, testifies the care and the erudition of Professor Seeley. On this the editor has expended fully as much labour as would be needed for the production of an entirely new book, and it is impossible to praise too highly the research which it evidences. It is far more than a text-book, it is a directory to the student in prosecuting his investigations. We await impatiently the second volume, on Stratigraphical Geology, which is in charge of our friend Mr. R. Etheridge, sometime President of this Society. Lastly, we have just received from the British Museum a copy (in advance) of Mr. R. Lydekker’s Illustrated Catalogue of the Fossil Mammalia (Part I.), and also a copy of a small illustrated Guide to the Fossil Fishes by Dr. H. Woodward. Both these books are placed upon the table. 50 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. But the event of primary importance in geology during the past year has been the abandonment on the part of the Director General and other officers of the Geological Survey, of the Murchisonian hypothesis concerning the stratigraphy and the age of the meta- morphie rocks of the Central Highlands. In his letter, published in ‘ Nature,’ Noy. 13, 1884, the Director General, ‘‘ spatiis conclusus iniquis,” was prevented from indicating the share which previous writers had taken in bringing about this result; but as in these later days the ‘‘ morning stars” of this reformation have arisen from our Society, and for the most part scintillated in our Journal, you will, I am sure, pardon me if I dwell briefly on the dawn before sunrise. Great as our gratitude should be to those who bring us the perfect light, we should not forget their harbingers in darker times, even if they could not wholly disentangle themselves from the mists of error. The view that the crystalline schists of the Gates Highlands * were, in the main, metamorphosed representatives of Lower Silurian strata, set forth in fullest detail in the classical papers of the late Sir R. Murchison and Dr. A. Geikie, was always stoutly resisted by the late Professor Nicol; but the authority of its upholders and the perspicuity of their arguments prevailed with the geological world, and opposition seemed to have expired with the death of Nicol. The Murchisonian hypothesis was endorsed by every official pub- lication ; it permeated our text-books. The first to raise the standard of revolt against authority was Dr. H. Hicks, who has devoted himself to the identification of Pre-Cambrian rocks which have been absorbed into and annexed by later formations, and their restitution to Archean, with as much energy as, and better success than, some ethnologists have displayed in the discovery of the ‘lost ten tribes.” In our Journal for the year 1878 (vol. xxxiv.), Dr. Hicks published a paper ‘‘ On the Metamorphic and Overlying Rocks in the neigh- bourhood of Loch Maree, Ross-shire.” In this, while agreeing with Sir R. Murchison and Dr. A. Geikie that there was an ascending succession from the Hebridean series, through the Torridon sand- stone, quartzites, and limestones to the flaggy series (called by those authors the Upper Gneiss), and an intrusive mass of syenitic rock (exposed on the floor of Glen Logan at the base of the last named), he maintained that they were mistaken in supposing the so-called Upper Gneiss, exhibited on the left bank of Glen Logan and in the lower part of Glen Docherty, to be a metamorphic group, and had overlooked the fact that true metamorphic rocks belonging to the oldest or Hebridean series reappeared in the floor of Glen Docherty, and by gradually rising and probably upfaulting, formed the whole mass of Ben Fyn, whence they passed southwards to constitute the major part of the Central Highlands. In the volume for 1880 appeared a paper entitled ‘* Petrological * An excellent sketch of the earlier stages of the controversy as to the age of the rocks of the Scotch Highlands is given by Mr. W. H. Hudleston, in a paper read to the Geologists’ Association in 187 9, and printed in Proceedings Geol. Assoc. vol. vi. p. 47. ANNIVERSARY ADDRESS OF THE PRESIDENT. 51 Notes on the vicinity of the upper part of Loch Maree.” The author, after emphasizing certain stratigraphical difficulties to which atten- tion had been called at the reading of the last-named paper, expressed his opinion, founded on microscopic study, that the flaggy beds, regarded as unaltered Lower Silurian by Dr. Hicks, were rightly called metamorphic and were true schists, although very different in character from the admitted Hebridean rocks ; he stated also that he had been unable to recognize any distinction between a newer and an older series in Glen Docherty, the former appearing to pass on from its escarpment at the upper end of Loch Maree towards Ben Fyn, although certainly the rock became more highly metamorphosed in this direction. The author accordingly contended that Dr. Hicks had failed to make good his criticism against the Murchisonian hypothesis. He asserted, however, that previous observers were in error in supposing the “ syenite ” of Glen Logan to be an intrusive mass of igneous rock, and maintained, on stratigraphical and petrolo- gical evidence, that it was simply a portion of the Hebridean floor brought up into its present position by faults *. The controversy was now transferred to the pages of the ‘ Geo- logical Magazine.’ Dr. Hicks obtained the valuable aid of Mr. T. Davies to examine his specimens microscopically, and published a series of papers in the volume for 1880 (vol. vi. dec. 2). In these he maintains the general accuracy of his former views, insisting much on the identity of the Ben Fyn schists with those of admittedly Hebridean age at Gairloch; a point which, though obviously of primary importance in the argument, had unaccountably in his former paper been passed over almost in silence. He also admitted that the so-called syenite of Glen Logan was not intrusive in the Lower Silurian strata, though he still regarded it as an igneous rock, but of Pre-Cambrian age, and he modified the section, which had been most open to criticism, so as to weaken the main objections. To these papers his critic briefly replied, commenting upon what appeared to him the weak points of the defence, and expressing more clearly his own position in the following words, ‘‘ It is possible there may be very much Pre-Cambrian rock in the Scotch Highlands ; my con- tention is that Dr. Hicks’s proof of this is erroneous.” _ Another paper was read by Dr. Hicks before our Society upon the age of the Scotch Highlands, which, however, was subsequently withdrawn by the author, so that only a short abstract appears in the volume for 1880; but I believe the substance of it was after- wards embodied by him in an address to the Geologists’ Association. In this Dr. Hicks deals with the district for a considerable distance on either side of Loch Linnhe, Loch Eil, and the 8.W. end of the Caledonian Canal. He shows that here also a great series of rocks occur corresponding with those of Hebridean type, both as asserted by himself and as admitted by his opponents, with which are in- folded both a schistose series, which he is disposed to correlate with * The possibility of part of this being gneiss had already been suggested (without the knowledge of the writer of the above paper) by Mr. Hudleston in his communication to the Geologists’ Association, 52 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. the Pebidian of Wales, and a group of rocks comparatively un- altered, which he regards as Silurian. - In the velume for 1881 a new combatant appears, and the debate is transferred to another region.- Dr. C. Callaway, in a short paper on ‘the Limestone of Durness and Assynt,” comes to a conclusion which perhaps may be most simply expressed in his own words. He had selected the localities ‘“‘ because they alone are alleged to have yielded fossils from the limestone, and because Murchison regarded them as of primary importance in the construction of his argument. My researches,” he says, “led me to the conclusion, not only that the sections were broken and therefore untrustworthy, but that the relations of the several rock groups were inconsistent with the supposition that the limestone passed below any part of the newer metamorphic series.” In another short paper published in the volume for 1882 he asserts the conformity of the quartzite with the Torridon Sandstone in the Loch Broom and Loch Assynt region, and on that ground maintains that the latter has more claim to be referred to the lower part of the Ordovician than to the Cambrian series. Ina paper entitled *‘ First impressions of Assynt,” published in the ‘Geological Magazine’ for 1882, Mr. Hudleston insists strongly on the evidence of folding and faulting on a vast scale, doubting the existence of the ‘‘ Upper Quartzite,” and bringing forward numerous reasons for believing that the equivalent in that district of the “‘ syenite ” of Glen Logan was, “‘ from top to bottom, the local repre- sentative of the fundamental gneiss, or something that is first cousin to it.” In the volume for 1883, Dr. Hicks returned undaunted to the attack, and, in the chivalrous spirit of one who fights for truth rather than for victory, took his old antagonist into his confidence, and obtained his aid in the examination of his collections. In this paper, which deals with an extensive district on the western side of Scotland, between parallels of latitude drawn roughly through Fort William on the south and the lower end of Loch Maree on the north, Dr. Hicks gives the results of two journeys undertaken subsequently to the year 1878, and brings forward very strong evidence in favour of the following conclusions :—that in the district between Loch Maree, the Gairloch, and Loch Torridon, the admittedly Paleozoic beds (Torridon Sandstone, Quartzites, &c.) rest upon the Hebridean series, which exhibits in ascending order three litho- logical types ; the lowest or most massive being exposed on the east shore of Loch Maree ; the middie or more banded gneisses occupying a considerable area on the west shore of the same loch, and a strip between the head of the Gairloch and the lower part of Loch Torridon ; and the upper or micaceous schist-like group occupying a strip which, starting from Ben Alligin, runs northward to the head of the Gairloch, separating the two areas of the last-named group. That the whole of the series is included in the Hebridean of Murchison has never been questioned. Dr. Hicks then points out that a group of rocks lithologically corresponding with the last- named of these passes by Loch Fannich and the head of Glen ANNIVERSARY ADDRESS OF THE PRESIDENT. 53 Logan, through Ben Fyn and the district east of it, and so broadening out occupies the coast from Loch Ailsh to Arisaig. Again it reappears, on the eastern side of a fault, near the head of Loch Kil (on the northern shore of which is asmall area of Torridon Sandstone), extending to Fort William on the Caledonian Canal. The triangular space between these two districts was occupied, as he showed, by a series of rocks corresponding lithologically with the middle zone of the Hebrideans of the Loch-Maree region. ‘To these three lithological groups Dr. Hicks gave the names respectively of the Loch-Maree, the Loch-Shiel, and the Gairloch or Ben-Fyn series, and he inclined to hold them stratigraphically distinct one from another. Dr. Hicks also admitted in this paper the gneissic charac- ter of the so-called syenite of Glen Logan, and classed it with the Loch-Maree group, stating that in the upper part of the glen he had found that it abutted on rocks belonging to the Ben-Fyn roup. ‘ The perplexing schists on the southern side of Glen Logan (named by him the Glen-Docherty beds, which occupy a consider- able area on either side of the latter glen) are separated from the rest, and their age is left by him in uncertainty. It cannot be denied that in this paper Dr. Hicks made to the controversy a contri- bution of the highest value, and may claim to have brought Highland reform into the region of practical politics. He had shown that unless lithological similarity was to be utterly disregarded as a factor in correlation in two areas almost neighbouring, a very large portion of the western Highlands north of the Caledonian Canal was occupied by rocks which were substantially identical with an im- portant series of admittedly Hebridean age, and exhibited the same lithological sequence. But this was by no means the only blow dealt in the course of the year. ‘Three months later was read a third communication from Dr. Callaway, printed in the same volume, ‘‘ On the Age of the newer Gneissic Rocks of the Northern Highlands.” This elaborate paper was the result of work done chiefly during the summers cf 1881 and 1882, in the districts around Lochs Broom, Assynt, and Erriboll. The following is a summary of Dr. Callaway’s principal conclu- sions :— | (1) The “ Upper Quartzite ” of some authors is, in these districts, simply a repetition by folding of the so-called Lower Quartzite ; the ‘“‘ Upper Limestone” on Loch Ailsh is marble and crystalline dolo- mite in the Eastern-Gueiss series (Upper Gneiss of Murchison); the Assynt series (Palzeozoic) has been doubled back upon itself in a com- pressed synclinal fold along Loch Erriboll, while along Loch Broom the dolomite (of the Paleozoic series) does not come into contact with the Eastern Gneiss at all, but is separated from it by older faulted rocks. (2) In the three areas described the Assynt series and the Eastern Gneiss display a discordant strike and dip. (3) The “‘igneous rock” of some authors, that now commonly VOL. XLI. g : | : | | 54 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. referred to as the Logan* rock, is usually the Hebridean Gneiss, which is often brought by an overthrow fault above different members of the Assynt series. (4) The Eastern Gneiss, though actually overlying the Assynt series in some localities, has been brought into this abnormal position by earth-movements subsequent to the deposition of the latter, and belongs to the Archean group, but is nevertheless widely separated © in age from the Hebridean. In his earliest paper Dr. Callaway had been disposed to acquiesce in the view which for a time found favour with several investigators, myself among them, that the apparent sequence from the base of the Torridon Sandstone to the Upper Gneiss might be a real one, but that the fossiliferous limestone of Durness might not be identical in age with the dolomitic limestone which appeared to underlie the Upper Gneiss, hence that the rocks from the Torridon Sandstone to the Upper Gneiss inclusive might all belong to the Archzean series, though to a later part of it than the Hebri- dean. This view Dr. Callaway, after more detailed work, was com- pelled to abandon, and I am myself convinced that we must accept the Torridon Sandstone, quartzite, and overlying limestone, whether dolomitic or not, as deposits of Paleeozoic age. But the untenability of the Murchisonian hypothesis had been simultaneously demonstrated by yet another investigator. Professor Lapworth, whose work in the southern uplands of Scotland had rendered him especially familiar with disturbed districts, and with the principles of mountain as opposed to lowland stratigraphy, applied himself in the summer of 1882 to the study of the coast region of Durness and Erriboll, selecting that as the one in which “a demonstrably ascending succession from the basal Hebridean Gneiss through fossiliferous Paleozoic limestones into the metamorphic gneiss and micaceous schist and slatest of the Central Highlands ” was asserted to occur. ‘The results of this work have been only in part published, because, on revisiting the country in the summer of 1883, incessant labour and continuous exposure completed the ill effects of a long period of excessive devotion to work, and brought on most serious illness, from which Professor Lapworth has hardly yet completely recovered. But you will remember that he exhibited in this room a most elaborate map and sketch section, at the meeting when Dr. Callaway’s paper was read it, and showed how his detailed work in the Erriboll region was in accordance with the main conclu- sions at which that investigator had arrived. Professor Lapworth, however, in the course of the year 1883 contributed three papers to the Geological Magazine, entitled “« The Secret of the Highlands.” These papers, the first of which was published in the March number, I may venture to assert will always hold a very high place among the contri- butions to the elucidation of a problem which for so long has been the special “crux” of British geologists. In the first, Professor Lapworth * Named from Glen Logan, near Loch Maree, also written Glen Laggan. + The Upper Gueiss of Murchison and Geikie. { May 9, 1888. ANNIVERSARY ADDRESS OF THE PRESIDENT. 55 demonstrates, by a sketch of the geology of the Durness-Erriboll region, that the ordinary principles of stratigraphy would lead obser- vers in two adjacent, districts to absolutely contradictory results viz. that in the Durness area, the Sutherland (or Newer) Gneiss series is demonstrably xewer than the (fossiliferous) Palzeozoic series, and in the Erriboll area is demonstrably older. In the other papers, published in the May and August numbers (the series was, I believe, left incomplete through his illness), he proceeds to apply to the Scotch Highlands the principles of mountain stratigraphy enunciated by Rogers, Heim, Baltzer, and others, and shows how, in the process of folding, inversions and overthrust-faults may be produced on a gigantic scale, and appearances of conformable succession and even of bedding be simulated, which are nevertheless wholly deceptive. The matter, then, before the end of the year 1883, in the summer of which a detachment from the Geological Survey took the field in Sutherland, stood thus: two or three of those whom I may call the minor contributors to this controversy, had pointed out serious mistakes and unsuspected difficulties, and had expressed, in effect, this opinion, that very clear evidence would be needed before we could accept the dominant rocks of the Highlands as of Lower Silurian age. Dr. Hicks had shown that unless lithological similarity in neighbour- _ ing districts be of no value, a very large portion of the rocks in the mountain region of South Ross-shire and Inverness must be much older than the Torridon Sandstone, and that there was evidence of faulting and folding on a gigantic scale. Dr. Callaway had shown the same for the western part of Sutherlandshire, and had proved the ex- istence of unsuspected inversions and overthrusts ; while Professor Lapworth had demonstrated the Murchisonian hypothesis to be self-contradictory in a region regarded by its upholders as typical, and had shown us that the difficulties, anomalies, and deceptive appear- ances are such as are usual phenomena in mountain-making on a grand scale*, I have dwelt but little upon the discordanees or the errors of the observers whose work I have noticed. Perfect concordance among reformers is not to be expected ; and men who are honestly struggling towards the light cannot hope to attain at one bound to the complete truth. There is always a danger lest the fascination of a new discovery should lead us too far. Men of science, being human, are apt, like lovers, to exaggerate the perfections and be a little blind to the faults of the object of their choice. Even now, great as has been the flood of light thrown upon the question by the writings of the Director General and his officers, | am sure that they would be the last to indulge in the illusion that they have solved every mystery or may not have to correct some details. It * T have omitted in the above brief sketch several papers of minor impor- tance which have appeared in the ‘ Geological Magazine’ and other publications, and a series of papers by Prof. Heddle in the ‘ Mineralogical Magazine ;’ the latter, because, notwithstanding their value as contributions to the mineralogy of the Highlands, I do not think they help us much in the elucidation of the above-named problem. g2 56 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. will need years of careful mapping in the field, supplemented by minute study of the rocks by practised and qualified microscopists (for in this matter a very special training is needed), before the whole secret of the Highlands is discovered. I am, indeed, more hopeful of the possibility of distinguishing between the results of metamor- phic action in Paleozoic and in Archean times than I believe some workers in this field to be; but to this subject I hope to return if honoured with another opportunity of addressing you from this chair. However, whatever may be the results of future work, whether official or non-official, I do not hesitate to say that this abandonment on the part of the Geological Survey of the Murchisonian hypothesis is an event of primary importance in the history of geological progress ; and we should render a just tribute of admiration to the Director General and to Messrs. Peach and Horne, the.chief mem- bers of the field-party, for their candour in investigating the question and in announcing their abandonment of opinions which only a few years since it would have seemed presumptuous to question. When Dr. Geikie declares that an hypothesis, main- tained by one whose memory is justly dear to him, in the support of which he himself in his younger days played an important part, - must be abandoned, he shows himself superior to that too common weakness which fears to admit a mistake, and he gives us the best hope for the future of the Geological Survey of Great Britain. Indeed, the importance of this step can hardly be over-estimated in regard to its future results. As a worker in petrology, I can testify how the Murchisonian hypothesis has lain like an incubus on the investigator, impeding his progress in what seemed legitimate inductions from observed facts, and being invoked by his opponents as a kind of fetish. Its abandonment, therefore, will be of moral as well as of intellectual value. I have noticed, sometimes with regret, among geologists an over-tendency to hero-worship. To question the conclusions of one of the great men now departed from among us has been regarded as sayouring of presumption. We are right, in the interest of science, to scout criticism which is founded on ignorance, and to show little mercy to rash hypothesis ; for these, by cumbering the ground, retard instead of helping progress; but a spirit of blind adoration for the past should have no place among those who are seekers after truth. So long as the facts are un- altered we are right in hesitating much before we differ from conclusions which one of our departed worthies in science has formed upon the data which were submitted to him as fully as to us; but when new facts have been discovered, when novel and more perfect methods of investigation have been devised, we are bound, — as honest men, to make full use of these and not to shrink from announcing our conclusions. I yield to no one in reverence for our great men of old; I marvel humbly at what they accomplished with the means at their disposal; but I should think it a wrong to the memory of searchers after truth did I invoke their names to arrest its progress, and use the “dead hand.” of the departed hero to paralyze the living worker. There is no revelation in science ; ANNIVERSARY ADDRESS OF THE PRESIDENT. 57 discovery did not cease when either Dela Beche, Murchison, or Sedg- wick rested from their labours; and it needs no prophet to foretell that in the days to come others will “rise on stepping stones of our dead selves to higher things.” Another good effect on geological progress is likely to result from this honest recantation. The establishment of a Geological Survey as a department of the State is an immense boon to a country; but there is always some danger lest the systematic method of their work, and a natural, 1 may say laudable, esprit de corps should lead its members to regard workers unconnected with them as intruders, and to speak with some contempt of “ amateurs.” Per- sonally I should not admit that a man who has devoted his life to the study and teaching of geology is not as fully entitled to be called a Professional Geologist as one who is an officer of a Survey. Indeed it appears to me that in the two ranks you will generally have developed capacities equally important, which can very rarely be united in any oneman. The official surveyor obtains knowledge of great accuracy and minuteness in a field which, from the nature of the case, must be rather limited; hence he becomes what we may call a specialized stratigraphist ; or, if not, he must occasionally be set to execute work for which he is imperfectly qualified, and so may make serious mistakes. The unofficial geologist, unfettered by the requirements of an office and the necessity of returning a seemly annual report of progress to his paymasters, the State, is able not onky to follow his special bent, but also to extend his experience over a wider area. ‘Travel, as it has been well said, is an essential in the education of a geologist; but to travel much requires a more liberal allowance of time and of stipend than can be obtained from an English Government. But accepting for a moment the definition of a professional geologist, as commonly un- derstood, there is and has been sometimes a danger that the class- feeling of which I have spoken should be aroused. It would be an ill day for science if the Geological Survey should ever become so narrow-minded as to resent ew officio the criticism of unattached competent observers, or one of the latter find any special pleasure in dilating upon a chance mistake which bore the imprimatur of Jermyn Street. It would be the greatest disaster if the votaries of geology became divided into “an establishment” and “ noncon- formists,” and imported into their differences a spirit too prevalent in theology. Messrs. Peach and Horne, by their unprejudiced inves- tigation into the facts in the field, and the Director General by his frank admission of a past mistake, have done their best to close a rift of which I have sometimes observed indications. In the future it will be evident that all alike are liable to err, and that the dis- covery of truth is not limited to any age or any workers. Science needs no infallible church and admits of no Pope. On these occasions you have for long past tacitly indulged your President with an opportunity of making some remarks on any department of geology in which he is specially interested. Of this 2 ee 58 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. indulgence I intend to avail myself by selecting petrology*, because of late years I have more especially devoted myself to investigating that branch of geology. In so doing I cannot hope to command the sympathies of more than a limited portion of my audience; but I venture to think that it may be of use to state, as clearly as may be in my power, some of the results at which I think petrologists have arrived, and some of the difficulties which yet remain for solu- tion. It will not, however, be my purpose to endeavour to ascer- tain whether the former category commands a majority of votes among geologists, or even among nominal petrologists; I shall venture to speak, as it has been my habit to work, with considerable independence, and you must receive my remarks as mainly the ex- pression of my own opinion, which, however, I can assure you, in all matters still the subject of controversy, has not been formed without considerable thought and labour. This method of proce- dure has been rendered inevitable by the circumstances of the case. It is now some fourteen years since, owing to a combination of causes, I drifted into studying the microscopic structure of rocks. I say ‘“‘ drifted,’’ because I did not undertake the study deliberately, nay, I refrained from it for some time through fear that a certain delicacy in my eyes would make it impossible for me to work with the microscope. That fear, however, has happily proved to some extent groundless, though I have always had to exercise considerable caution, and to use high powers only for limited times. I began the study in consequence of finding among those who professed to be authorities such a conflict of opinion, even upon the most fundamental questions, that no conclusion, upon written evidence alone, seemed possible. Hence it has always been my endeavour to work without prejudice in favour of any view, to gather my facts from observa- tions both in the field and with the microscope, to frame hypotheses as the facts accumulated, and then to continue to test these hypo- theses by further work. I believe that I may add that, at the beginning, I always took as the more probable hypothesis that which appeared to find acceptance with the best authorities. I have endea- voured, in short, to apply to this branch of geology the laws of reasoning which were taught me years ago in mathematics, and I venture to believe that this method is the safest. It will not save one from mistakes; it may happen that, notwithstanding all care, one generalizes too hastily; a wider knowledge may show that an hypothesis is inadequate or imperfectly stated; but still, I believe that this method of successive approximations, of framing working hypotheses from facts, and constantly exposing these to the test of new facts, is the right way to attain truth in science. Let me, however, first venture one or two remarks on the present position of petrology as a branch of science. It has undergone vicissitudes. To many of the early geologists it presented great * Or, as some authors prefer to call it, petrography. The word used in the text appears to me preferable on the analogy of the other designations of sciences, petrography indicating the description rather than the scientific investigation of rocks. ANNIVERSARY ADDRESS OF THE PRESIDENT. 59 attractions, and for a time paleontology was of less account than mineralogy, the fossil contents of the earth’s crust attracted less attention than its mineral structure. But some forty years ago the majority of geologists yielded to the fascination of the vast field which a study of fossils opened out before them ; and exact petrology, at any rate in England, found few followers after the death of De la Beche. I do not say this as a reproach—it is well that each generation should do the work which lies ready to its hand; and I can under- stand that the great mystery of life will always induce (and, I may say, rightly induce) the majority of thoughtful men to incline to a study of the organic rather than of the inorganic world. Further, the older generation of petrologists had gone about as far: as was possible with the means at their disposal; the revival of petrology has been due to the application of the microscope to the investi- gation of its problems. In this respect we may feel a just pride in remembering that to one of our countrymen, Dr. H. Clifton Sorby, a former occupant of this chair, belongs the honour of being among the very first to appreciate the importance of this mode of investi- gation and to place himself at its head. At the present time the study of petrology is encompassed with not a few difficulties, some inherent, some temporary. It may be useful, even at. the risk of giving offence, if I glance briefly at these. To begin, the study is not, and can hardly ever be, a popular one. To be an ideal petrologist it is necessary to be a good chemist, physicist, mineralogist, and field-geologist ; and who can hope to combine qualifications so diverse? Again and again I have found myself sharply stopped by my ignorance of chemistry, of physics, or of mineralogy, or by want of leisure to undertake along journey for the purpose of study in the field. These difficulties, however, will always more or less exist, and we must be content to do our best with the means at our disposel. But there are also difficulties of a more temporary nature. One is that geologists, as a body, under- value rather than overvalue the difficulties of the subject, and seem disposed to treat it as a playground whereon they may relax from severer studies. As regards this, I venture to assert that, at the present stage of our knowledge, crude fancies and vague hypotheses, founded on a few imperfectly observed facts, can do nothing but _ eumber the ground and impede the progress of students. No ob- servation on any point of real difficulty is of the slightest value unless it be substantiated by careful study with the microscope. Closely akin to this is another difficulty, that the evidence cannot be presented ad populum. What is seen with the microscope depends not only upon the instrument and the rock-section, but also upon the brain behind the eye of the observer. ach of us looks at a section with the accumulated experience of his past study. Hence the veteran cannot make the novice see with his eyes ; so that what carries conviction to the one may make no appeal to the other. This fact does not always seem to be sufficiently recognized by geologists at large. In similar paleontological ques- tions, such as the structure of plants or of protozoans, I have 60 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. observed that the opinion of one who is known to have devoted some years to the study is considered to outweigh that of one who has given no proofs of competency ; while I have seen in petrology, again and again, statements commanding attention, and even printed in scientific journals, which I knew not only to be unproved, but also, unless the work of years had been wasted, to be extremely difficult to prove. There is yet another impediment to progress, quite opposite to, and much mote laudable than, the last. It is that the recognition of the great difficulties of the subject causes some students to despair of arriving at the truth, and leads them to adopt what I may call an agnostic position. Now I believe that by so doing no progress ever has been or ever will be made in science. If caught in a scientific “slough of despond,” you will never get out by merely wallowing about aimlessly. Assume that there is a way out; try in turn each that seems most probable, and probably one will be found. Iam well aware that there are a vast number of questions in petrology which are not yet settled—not a few, perhaps, never will be settled in our lifetime ; but I maintain that progress is most likely to be made by endeavouring to frame a working hypothesis, if only the observer be strictly honest in recording not only the facts which are favourable to it, but also those which appear to be hostile. May I then be allowed, before proceeding further, to lay down two principles which occasionally seem to be forgotten by some earnest workers ? (a) The first is that all observations which are on record are not of equal value. This depends, as I have said, partly on the qualifi- cations of the observer, partly on the perfection of his appliances. For example, there are some difficult points in petrology in regard to which I should attach hardly any weight to the evidence of even one of our most honoured workers in “‘ premicroscopic ” days, because I know, from my own experience, that the question is one where the unaided eye cannot help us to a decision. (6) That’ one “positive” observation outweighs a large number of “‘ negative,” the latter word being used in the sense of “ leading to no definite conclusion.” Let me illustrate this by an example. Suppose I wanted to ascertain whether an igneous rock were inter- bedded with or intrusive among certain sedimentary strata, and that twelve sections were to be found. Suppose that in eleven of these the appearances were not inconsistent with either interpre- tation, but that at the twelfth the evidence could only lead to one of the two views. Clearly the absence of conclusive evidence in the eleven cases would not affect the value of the evidence in the twelfth. The rules, in short, of ordinary reasoning—and this remark has a wider application than to the case which I have just mentioned—hold in every branch of science, and in no one is it more needful to bear them in mind than in geology, where direct experiment (as in chemistry and physics) is so often impossible, and where we can never attain to more than a degree of moral certainty. ANNIVERSARY ADDRESS OF THE PRESIDENT. 61 With these preliminary remarks, for which I trust I may be par- doned, as they are the outcome of an experience gained during some eight years in your service and some fourteen in petrological work, I turn to the special subject which I intend to discuss briefly to-day —the classification and structures of the igneous rocks. By an igneous rock I mean, of course, one which has been in a state of fusion through heat. This fusion, however, differs from that which has been undergone by most rocks artificially produced, such as slags, because it has always taken place in the presence of water ; and further, the material has often solidified, and even crys- tallized, not only without the expulsion of, at any rate, all the water, but also under considerable pressure. Probably the nearest approach to solidification under conditions similar to that of a slag is given in the case of lavas, immense volumes of steam being generally disengaged from the flows as they are emitted from a volcano. I draw attention to this at the outset, because I think it possible that it may prove to be a matter of primary importance in certain of our investigations. We ought, however, before proceeding further, to glance at two objections which might be started a lmine. | (1) That no classification is possible, because nature has not made distinctions ; she is too protean to be bound by our fetters. (2) That it is impossible to draw a hard and fast line between igneous and sedimentary rocks, because the former are frequently only the result of metamorphosis of the latter carried to an extreme degree, so that the one series passes gradually into the other. As regards the former of these objections, we may remark that on the assumption that igneous rocks have solidified from a state of fusion (whether part of the original magma of the earth or stratified rocks subsequently melted), we should anticipate difficulties in classi- fication, and not expect to find very sharply defined lines of separa- tion in either chemical or mineral composition. This difficulty, however, is not confined to petrology ; the biologist, for instance, is not deterred by the admitted difficulty of distinguishing a species from a variety, or of deciding whether species have an independent origin. Hence, for all practical purposes, species exist alike for the most thorough-going evolutionist and the most confirmed believer in special creations. Classification is a necessity if progress is to be made; distinction of things is needed for distinction of thought; and over this difficulty we need not linger, for we shall find that, prac- tically, although intermediate forms may exist, the majority of rocks can be grouped around certain types. The second objection may receive a like answer; and I may add further, that if we agree upon certain characteristics as denoting an igneous rock, the antecedent history of the rock (for our special purpose) becomes immaterial. For instance, I can think of a piece of glass as an (artificial) igneous rock, even though I may have formerly seen a crucible full of the material from which it has been made. There are, moreover, as it appears to me, two rather considerable 62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. difficulties of a general character in this supposition of the derivative character, as I may term it, of igneous rocks*. The one, that chemically and even mineralogically there is a remarkable identity between igneous rocks of the most diverse geological ages. This, however, I content myself with mentioning, because I can more conveniently enlarge upon it at a later period. The other, that the chemical composition of the bulk of sedimentary and of igneous rocks is too diverse'to admit of the hypothesis of derivation being generally true. It is possible, I allow, to find certain sedimentary rocks which chemically are nearly identical with certain igneous ; but to do this we must select exceptional cases in the one to compare with general instances in the other,—the most marked difference being in the percentage of the alkaline constituents, which leads, as is well known, to the presence of such silicates as stauro- lite, andalusite, cyanite, and alumina-garnet, in indubitably metamor- phosed sedimentary rocks, instead of some members of the felspar group. Further, the argument of chemical identity holds only among the more acid of the igneous rocks; among the sedimentary it would not be easy to find representatives of the dolerites and basalts, rocks extremely abundant in nature, and almost hopeless to parallel the peridotites, which in one form or another are by no means rare. I glance only at the corroborative evidence of meteorites, because I intend on the present occasion to limit my remarks to rocks of terrestrial origin, though I am quite aware that any system of classification for the latter must be extended to the former. The tendency to a definite order of succession among the igneous rocks which has been remarked by many observers, appears to me more favourable to the idea of these rocks being integral portions of the inner part of the earth, than to their being the result of the local melting-down of sedimentary strata. This subject is so full of interest that I would gladly have discussed it, but the difficulties still inherent in it, and the collateral disquisitions into which it would lead, prevent me on the present occasion. I do not, indeed, think that we can accept subdivisions so,elaborate as those proposed by Richthofen, and used by Dutton} in his ingenious explanation of the apparent anomaly of basalt, an easily fusible rock, being com- monly later in date than rhyolite in a series of eruptions; but undoubtedly we do so frequently find this general order—andesites, sanidine-trachytes (probably these two will often be intermixed), rhyolites, and basalt, and observe gabbro cutting peridotites—that these sequences can hardly be accidental. It may suffice, then, to call attention to Captain Dutton’s valuable dissertation and to two papers by Mr. Teall (which appeared just after the reading of this address) wherein this subject is discussed more fully?. * The frequent occurrence of sharply defined junctions between igneous and sedimentary rocks of various kinds, and of fragments of all sorts of rocks in the former with boundaries no less sharply defined, is to me also a very strong argument against the “ melting down” hypothesis. tT Geology of the High Plateau of Utah, ch. iii. t Geol. Mag. Dec. 3. vol. ii. p. 106. Nature, vol. xxxi. p. 444. ANNIVERSARY ADDRESS OF THE PRESIDENT. 6 3 Further, the asserted passages between igneous and sedimentary rocks rest at present on evidence which, I have already stated, we are justified in putting out of court. They require confirmation, and we know that many instances, once confidently asserted, have broken down on strict examination*. Indeed, I may venture to assert that, so far as my experience goes, the difficulties at present existing either are due to obliteration of the original structure by subsequent mechanical or mineral change, or occur among the very earliest rocks of which we are cognizant; the latter are not only likely to have undergone such changes, but also may have been formed under circumstances which haye never recurred in the history of the earth. These, for the present, I put on one side, hoping on a future occasion to return to them, and limit myself to the great body of rocks which all admit to have solidified from a state of fusion, and to those which (although field-evidence may be wanting) we may reasonably believe, through their close structural correspondence, to have been so formed. So much controversy, however, has existed as to the origin of granite, that I shall venture a few additional remarks on this subject. To me it appears to a very large extent a dispute about the two sides of a shield. On the one hand, the phenomena exhibited by granite masses intrusive into other rocks, z. e. sharply defined junctions, contact-metamorphism, the sending off of dykes and veins which gradually assume the structure of normal felsites, perhaps even of rhyolites, justify us in asserting that granite cannot be separated from the other plutonic rocks such as syenite, diorite, and gabbro. _At the same time it is true that there are abnormalities incom- patible (so far as we know) with the idea of dry fusion, and that water is actually present in numerous minute cavities ; but the same is true in some of the rocks above named. Further, I do not suppose that any geologist at the present day would assert that perfectly dry fusion is a common thing in nature, if, indeed, it ever exists. Clouds of steam are discharged from the craters of volcanoes and the surfaces of lava streams as they flow. The latter by parting thus with their water will cool in a manner more analogous to that of a furnace-product ; had the same material solidified deep in the earth, a large portion of the water at any rate would not have been * With regard to the alleged transitions from igneous to sedimentary rocks, Dr. Wadsworth, in his recent ‘ Lithological Studies’ (a copy of which through the author’s kindness reached me after the greater part of this address was written), uses language which, though severe, is not unjustifiable (p. 12). After dwelling on the numerous cases where the asserted evidence of transition has proved to be either negative or exactly opposed to the hypothesis, he con- tinues :—‘ Practically, when the existence of these junctions has been shown, the observers who had previously denied their evidence have always said, ‘ That is not a typical locality ; we were not quite sure about that place, but if you will go to such and such a locality,’ indicating some new one, ‘ you will find an un- doubted passage of sedimentary rock into eruptive forms.’ When the new locality is also examined and the statements are found to be erroneous, another one is mentioned, and so on; until one must demand hereafter of these observers _ that they shall select some locality on which they shall be willing to fully and finally stake their pet hypothesis, and abide by the evidence.” 64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. disengaged, and thus crystallization, and previous fusion (if the rock has not always been molten) have taken place in the presence of water. Thus the controversy is either illogical, if restricted to granite, or merely a verbal one, if extended to other plutonic rocks. But some will assert that granite may justifiably be considered alone, because many cases exist in which a perfect passage can be traced from normal granite into normal gneiss. As regards this assertion, I repeat the remark already made, that these cases are less numerous than is supposed. I have examined a good many asserted cases of transitions from igneous to sedimentary rocks, and found that, as a rule, the distinction between the two rocks was well marked, and that the generalization was the result either of precon- ceived theory or of too hasty observation; further, that precisely similar difficulties exist with syenite and diorite, though the cases are less numerous, as the rocks seem not quite so common ; lastly, that those cases which appear to favour the theory occur only in the case of rocks which there is good reason to believe are among the most ancient yet discovered. ‘These, as I have said, I lay aside for the present. But in the case of the Paleozoic and later rocks it is only rarely, and under circumstances suggesting subsequent obliteration of the characteristic structure, that I see a difficulty in distinguishing between rocks of igneous and of non-igneous origin. IT shall not then dwell further on the question of the origin of an igneous rock, but I shall use the term to signify one that has solidi- fied from a state of fusion, due to the existence of an elevated temperature, whether we might call this dry fusion or not. Further, in my classification, I shall draw no line of demarcation between igneous rocks of Tertiary and Post-Tertiary age and those of earlier date ; the reasons for this I defer, and think myself justified in so doing, because it is one which logically would not arise in any independent study of petrology, but would be imported into it as the result of conclusions arrived at from other considerations not entering into my classification. Theoretically, and probably also in practice, there are at least two well-marked physical conditions in which any rock of a definite chemical composition may occur, the hyaline and the holocrystalline. Is there an intermediate condition wherein the rock, though no longer vitreous, though exhibiting some differentiation of consti- tuents, has not attained such complete individualization as to justify the use of the term holocrystalline? I do not allude to the interpo- sition in the glass of a great number of microliths of individualized minerals, although this may offer obvious practical difficulties, nor do I refer to the size of the crystals making up the holocrystalline rock. I should deem the latter epithet properly applied, whether the cha- racter was readily observed with the unaided eye, or could only be seen under the microscope; but I speak of cases in which the material appears to have lost the usual property of a colloid, to have acquired, around innumerable centres, polarities in one or more directions, without its being possible to distinguish with precision what are the minerals into which it has segregated ; where, in fact, ANNIVERSARY ADDRESS OF THE PRESIDENT. 65 phenomena akin to those of tension or compression appear to have been permanently impressed upon the mass, only in a vast number of directions. This question also can best be considered in a separate excursus. Suffice it to say that, in the present state of our know- ledge, it appears to me convenient to admit the existence of an inter- mediate division, to contain the rocks often called “‘ cryptocrystalline” with some of the “‘ microcrystalline,’ whatever may be the ultimate fate of the division. We will therefore assume that we may expect to find an igneous rock in either a holocrystalline, a hemicrystalline, or a hyaline condition, admitting that the middle term is perhaps rather incorrect as a symbol of facts and temporary in its existence. The relative size of the constituents in rocks, and their arrange- ments—such structures in short as are designated by terms such as porphyritic, spherulitic, fluidal—I shall at present regard as only varietal. There is, however, one question of principle in nomenclature to which I must briefly advert. It is whether we should indicate distinctions of minor weight by conferring separate names, or by the use of qualifying adjectives—that it is to say, whether in our nomenclature we should direct the mind chiefly to specific or generic differences. The former is the habit in mineralogy, and it is in favour with some petrologists. While fully sensible of its advantage in conciseness, I believe it open to grave objection. Some questions of nomenclature, those, for instance, of priority, are of little value. It is comparatively unimportant, subject only to considerations of euphony and orthoepy, what we call a rock, so long as the name expresses as definitive an idea as the circumstances of the case permit; butitis a matter of great moment whether our nomenclature suggests or obscures relationships which exist innature. Distinction is, indeed, necessary for clearness of thought, and is requisite as a first step in scientific comparison ; but itis by comparison and recognition of relationships that all great advances in morphology and in philo- sophic reasoning are likely to be made; and it is, methinks, a matter of no small importance to keep clearly in view, in any system of nomenclature, the underlying affinities rather than the superficial dissimilarities. Our nomenclature in petrology suffers in some parts, as I shall presently indicate, from a plethora, in others from a defect of names. A further: difficulty exists in that there are not a few names which have been so vaguely and variously used, that it seems hopeless ever to render their meaning fixed or precise; these it would be better, in my opinion, to leave as admittedly vague terms, indica- tive of imperfect knowledge. So applied, they become valuable. Petrology needs what I may call “ travellers’ terms,” to be employed as a naturalist would use trivial or generic names, when he either had failed in getting a good view of a creature or had not yet worked out the characteristics of a specimen. In this sense such terms as felstone, greenstone, even trap, are valuable. Aphanite, however, is not so good as compact greenstone, unless we can agree upon a perfectly definite meaning for it; and the same objection applies to 66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. melaphyre, which, however, would be useful if admittedly left vague. Porphyry is admissible as a vague term, but objectionable in any system of classification, because ‘of its diversity of applications 1 in the past. Elvanite isa term wholly bad, because it suggests inaccurate ideas, by affixing a Cornish miner’s trivial name, used even in that county in a very inclusive sense, to a rock which is world-wide in its distribution. Plutonic and voleanic also, though useful for rough divisional purposes and as general expressions, cannot for obvious reasons be used for exact classification. I mention these as examples, the list not being intended to be exhaustive. As already intimated, I should not regard the conepiedons presence in a rock, whether crystalline or vitreous, of one or more minerals in orystals larger than others as justifying the use of anything more than an adj ective ; hence in dropping the term porphyry from our classification, I should continue to use the epithet porphyritic (notwithstanding obvious etymological objections); neither should I signalize the presence of macroscopic cavities, whether large or small, except by an epithet, or by the employment of a trivial name for general purposes of description. If the above premises be admitted, it is evident that our system of classification must, so far as regards the igneous rocks (previously limited by definition), rest upon chemistry*. To a very large extent it will be also mineralogical ; but we must not say wholly minera- logical, because that science will not enable us to determine the exact position of a hyaline rock, and, if alone regarded, may induce us to pay too much regard to minerals which can be shown to be the result of secondary actions after the first consolidation of the rock. Igneous rocks, we must remember, like any others, are: liable to metamorphism; and we should try, as far as possible, to separate in our classification the latter from those which are comparatively unchanged. Now it is well known that, ceteris paribus, the more basic a rock the more readily it assumes a holoerystalline condition. Natural glasses are rare and limited in extent among the basic rocks, are comparatively common and well developed among the more acid, and probably are largely represented among ancient rocks, which, strictly speaking, cannot now be called vitreous. Marked chemical and marked mineralogical differences should, then, be recognized primarily in any system of nomenclature. On the whole I am disposed to attach more weight to the former than to the latter, because sometimes a marked mineralogical difference, for example the substitution of hornblende for augite, may be the result of subsequent change, which, however, it may be difficult to substantiate. Of course, when such changes can be proved to have occurred, the rock should be removed from the category of normal igneous, to that of metamorphic igneous. * Tn reality, of course, our classification deals with the aggregate history of the rock, its ontology as well as its morphology, if the phrases be permitted, because our limitation in using the epithet igneous, presumes an investigation into its relations with cther rocks, an investigation into its petrology as well as into its lithology. — ANNIVERSARY ADDRESS OF THE PRESIDENT. 67 Our nomenclature, then, after the recognition of these essential distinctions, must further acknowledge the more accidental, viz., the physical condition of the rock, whether hyaline or not, the re- lation of its constituents, and the like. Many of these secondary distinctions I should prefer to indicate by adjectival affixes, reserving differences of names for marked differences in chemical constitution, and, after that, of crystalline condition. The latter, I grant, refers rather to a difference of environment than to a difference in essence ; a holocrystalline, a hemicrystalline, and a hyaline rock of the same chemical composition have quite as near a relation one to another as the larva, pupa, and imago of an insect; but the marked difference in aspect and structure justify us, I think, in a nominal separation. ‘The presence of an adventitious mineral not materially affecting the chemical composition, peculiarities of structure or the like, should, I think, be indicated by epithets. The number of minerals, as is well known, which enter into the composition of igneous rocks frequently enough to entitle them to be called “rock-forming,”’ is but small; for convenience they may be grouped as follows*. I. Oxides of Iron, Se. Magnetite, hematite, ilmenite, chromite (with spinel). II. Magnesia-iron Silicates. Olivine, enstatite (with hypersthene), augite and hornblende, biotite. Jil. Alumina-alkaline Silicates. Felspars (with nepheline and leucite), muscovite. IV. Free Silica. Quartz. From this list such minerals as apatite, zircon, titanite, sodalite, nosean, are omitted, though occasionally some of them may be re- garded as rock-constituents, because they do not appear to have any very important classificatory significance, and some are generally associated with certain of the above named. Garnet also is ex- cluded, though occasionally an important rock-constituent, because, as it seems to me, we are not yet in a position to deal with it. If an original constituent, and not an accidental one, due in some way or other to contact-effects, I am disposed to regard it as a member of No. III. The igneous rocks, then, as it appears to me, fall naturally into the following grouping, commencing with the most basic and using the existing nomenclature as far as possible. The Peridotite group consists of olivine with some members of I. and commonly some representatives of II. Its simplest holocrys- talline representative is dunite, essentially olivine and chromite. (I should apply the name to the rock whatever representative of Group I. were present.) The next marked variety is given by the * T follow very nearly the classification proposed by Rosenbusch. 68 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. addition of an enstatitic mineral*. For this Dr. Wadsworth proposes the name savonitey. Another marked variety adds augite or horn- blende; to this we may apply the term Jherzolite t, though hitherto it has been limited to one containing an augitic mineral, because I think that here the substitution of hornblende has no important significance. This group, then, consists of rocks containing little or no alkaline constituent, little lime or alumina, the last named often occurring in very small quantities, a considerable proportion of iron- oxide, and magnesia and silica in nearly equal proportions, the former generally slightly exceeding the latter, and each not far from 40 per cent. Hemicrystalline and vitreous representatives of these rocks are extremely rare. J have never met with one of either in my own experience, though I should expect them to occur. Thus no names have been proposed for them. They are largely repre- sented in past time by the true serpentines §, their metamorphic representatives, into which they pass by insensible gradations ; among these, I have suspected, though I cannot prove it, the presence of glassy representatives, which, however, are rare and local. The Picrite group may be regarded as a transitional one, formed by the introduction of a small and variable amount of felspar, such as apvorthite or labradorite; the amount of olivine is diminished: enstatite and a pyroxenic mineral, with biotite, become important constituents. The chemical composition, as might be expected, is variable, but the percentage of silica is slightly greater than in the last group, though generally not more than 45. Magnesia, though still one of the two dominant constituents, 1s present in an amount distinctly less than the silica, commonly from about 17 to 27 per cent. Alumina is always present, sometimes in considerable - quantities, with alkaline constituents ; but chrome and nickel, which are generally detected in the normal peridotites, are now often absent. These rocks, so far as we at present know, are generally ancient, and often more or less altered ||; but I think the name * J will use this term for brevity to include either enstatite. bronzite, or hypersthene, minerals very closely related, if not varieties of one species. t Lithological Studies, pp. 84, 193. t Dr. Wadsworth proposes (Joc. ci¢. p. 195) to limit the term lherzolite to the variety with diallage, and call that with augite buchnerite, applying to a variety with diallage and without enstatite the name eulysite. I doubt, how- ever, the possibility of separating the first and second. ulysite also has hitherto been applied to a garnet-bearing peridotic rock. § Iam, of course, well aware that this statement has been disputed, but have more than once given my reasons for it, so need not repeat them. On the principles of reasoning which I have endeavoured to establish above, I am unable to understand how the derivation of a true serpentine, 7. ¢. that of which the Lizard serpentine is a type, from a peridotite, or the igneous nature of the latter rock can be doubted. || The serpentinous rock of Duporth (Cornwall), for which the name Dupor- thite has been needlessly proposed, appears to be a member of the picrite group. Many of the picrites certainly hang on very closely to the dolerite group (described hereafter), and can be seen to graduate into representatives of it. ANNIVERSARY ADDRESS OF THE PRESIDENT, 69 piertte preferable to that of palcwopicrite, which has been given by many authors. To this group probably the eulysites of some authors (garnet-bearing peridotites) should be referred, and lim- burgite would represent the hyaline form. I am not aware that a hemicrystalline form has been recognized, certainly it has not been named. As subgroups or intermediaries between this last group and the next great one, we may regard the norites or hyperites, composed chiefly of a plagioclase felspar (anorthite or labradorite), with an eustatitic mineral and perhaps a pyroxenic; the corsites, anorthite hornblende rocks (perhaps we might use eucrite for the anorthite augite); and the troktolites, containing the same felspar with olivine and but little of a pyroxenic mineral. Itis perhaps well to retain these names, but it must be remembered that they have hardly a generic value. It may here be worth while to call attention to the fact that many of the so-called hypersthene rocks, ¢. g. the gabbros of Skye, and of Carrock Fell (Cumberland), either do not contain hyper- sthene, or have it only as a very rare accessory, while in others it is not more conspicuous than a pyroxenic constituent, so that there is no valid reason for calling them more than hypersthene (or enstatite) dolerites or gabbros. We come then next in order to a most important group, that which contains, as constituents, a plagioclase felspar, commonly labradorite, a pyroxenic constituent, usually augite (or occasionally diallage), and often olivine*. To this group many names have been given, and various subdivisions of it have been proposed. Some authors extend it so far as to include rocks in which either nepheline or leucite replace the felspar, calling them respectively nepheline- dolerites, &c., or leucite-dolerites, &c.; some distinguish those in which olivine is present from those from which it is absent. For myself, while fully admitting the relationship of each of the former pair to the normal dolerites, and the frequent existence of interme- diate forms, I think that the marked chemical differences (in the large percentage of alkalies) justify us in separating them from the felspar-dolerite and in retaining the old names, nephelimte and leucitite. Some, again, using geological age as a distinction, apply the name diabase to a rock if it is Pre-Tertiary, and dolerite, if of later age; this, of course I could not accept, but should propose to give the former name to dolerite in which marked alteration, sub- sequent to the original consolidation, has taken place. Others, again, apply the name gabbro to coarse-grained varieties in which the pyroxenic mineral is wholly or chiefly diallage. There is much convenience in the use of this term for a variety often so well marked in the field; but there is at present doubt as to the classificatory value of diallage, some authors of great weight regarding it as really an altered condition of augite. Provisionally, however, we may retain it, remembering that it may be logically indefensible. As, * TI shall, for brevity, not again refer to the presence of a member of Division I., because some oxide of iron, magnetite, hematite, or ilmenite is to be found in every rock, though usually more abundantly in the more basic. VOL. XLI. h 7° PROCEEDINGS OF THE GEOLOGICAL SOCIETY. however, many gabbros have undergone much alteration, the felspar being changed into a saussuritic mineral, the diallage into some form of hornblende, it would be well to restrict the term euphotide to these. Again some authors use the terms dolerite, anamesite, and basalt for rocks which, chemically identical, and all holocrystalline, differ in the coarseness or fineness of their grains, so that the last term is applied to a rock which either may be holocrystalline or may retain a glassy base. It would be convenient, then, to restrict the term dolerite to the holocrystalline variety, using the epithet coarse-grained or fine-grained as the case may be; to apply the name anamesite to the hemicrystalline varieties (very few and local, I suspect); and to include in the term basalt all that retain a glassy base, 7. ¢ the magma-basalts and glass-basalts of some authors. It may be found convenient to use the name magma-basalt (as does Borick¢) for those in the base of which the felspar remains unindi- vidualized. The name tachylyte has been applied (as is well known) to varieties where almost the whole material remains in the form of glass, and the term may be conveniently retained, if we remember that it is only a marked variety of the glass-basalt division. Two rather limited groups of uncertain position come next in order, the phonolites and the tephrites. The former group is essen- tially characterized by the presence of nepheline and of felspar, which is commonly, in part at least, orthoclase, the latter by leucite and felspar (more commonly plagioclase); but there are several accessories and many varieties, as may be seen from an examination of Boricky’s divisions of the former group alone. It also is one whose nomenclature is in great confusion. Among the older mem- bers we have zirkon-syenite, eleolite-syenite, nepheline-syenite, foyaite, ditroite, miascite, while the one term phonolite covers all varieties, whether holocrystalline or not, among the more modern. The group being, to a large extent, a transitional one, differing from that last in order by a higher percentage of silica and of alkalies, and a lower percentage of lime and magnesia, we can hardly hope to secure very marked type-forms ; but perhaps the name foyaite might suffice as a specific term for the holocrystalline varieties ; while in the case where the characteristic mineral is very distinctly the variety eleolite rather than nepheline (which does not appear to be the case with all foyaites), we might prefix the term eleolite. We should thus have as varieties elzeolite-foyaite, nosean- foyaite, &c. It will, however, be a subject for consideration whether it may not be desirable, after the analogy of the groups which follow, to divide those in which a plagioclase felspar pre- dominates, from those in which the felspar is chiefly orthoclase ; but as my opportunities of studying this group have been rather limited, I will not venture an opinion on this poimt. Of the tephrite group 1 must speak yet more guardedly; for although I possess specimens, I have not had the opportunity of paying much attention to the rock. The name, however, is convenient to denote plagioclase-leucite rocks, and should be applied to rocks in which the former mineral predominates, and the percentage of silica is higher —-_- -— —w — * ANNIVERSARY ADDRESS OF THE PRESIDENT. 71 than in the leucitite group and the forms intermediate between it and the dolerite group. An examination of a table of the chemical composition of minerals shows that with a high percentage of alumina compared with the silica, we shall obtain anorthite in rocks rich in lime and poor in alkalies; labradorite with a lower percentage of lime, and a moderate proportion of alkalies (chiefly soda); nepheline with a higher percentage of alkalies, soda still predominating ; and leucite with an exceptionally high percentage of potash. The next two groups contain a higher proportion of silica, rarely less and often more than 60 per cent. Normally they may be defined as felspar with hornblende, though in certain divisions augite more commonly replaces the latter; biotite is not unfrequent, sometimes dominant over the pyroxenic mineral; at times hyper- sthene is an important accessory, taking the place of the unisilicate olivine among the (more basic) dolerites. Although transitional forms may be found between these groups, it is convenient to designate the more typical representatives by different names; thus the ortho- clase-hornblende group may be called, after the holocrystalline form, the syenites, the plagioclase-hornblende group, the diorttes. Hemicrystalline and glassy forms of both are common, but it is by no means easy, especially in the case of the latter, to separate them without chemical analysis, though the character of any individua- lized felspar crystals is often a great help. I may remark, however, that not a few of the so-called hemicrystalline forms are in reality holocrystalline, though very fine-grained, and others can almost be proved to have assumed a hemicrystalline structure by secondary processes, so that in reality they should be placed in the meta- morphic division ; but leaving that distinction to await the results of further study, we may recognize the following divisions of the syenite group :—holocrystalline; orthoclase + hornblende = syenite; if mica replaces the hornblende wholly or to a marked extent, mica-syenite; if augite=augite-syenite. ‘To the last rock, by no means a typical member of the group, as it contains much plagio- clase felspar, the name monzonite has been given. The hemi- crystalline division contains a considerable number of the rocks macroscopically grouped as felstones. By many authors they are called orthoclase-porphyries ; but the name porphyry, as I have stated, being objectionable, and a binary term for a group being awkward, I should prefer tv call them felsites. Then those in which orthoclase or any other mineral was conspicuously present might be called orthoclase-felsites, hornblende-felsites, mica-felsites, or the like. Hyaline forms are now becoming abundant, though commonly the glassy base contains a large number of individualized minerals. These are generally named sanidine-trachytes ; but as the term trachyte is used like felstone for grouping in the field, its use in this more limited and strictly definite sense is objectionable, and, as before, the compound term isawkward. It is no part of my present purpose to attempt to coin new names, so I content myself with expressing a hope in this and like cases that a geological congress will some day invent and authorize one; till then I must » h 2 42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. continue to use that which exists, though under protest. Wholly glassy forms doubtless exist, though probably not very abundantly ; but it is sometimes difficult to distinguish these among the pitch- stones and obsidians, of which the majority belong to rocks with a higher percentage of silica. In the diortte group a considerable portion of the plagioclase felspar belongs to one of those which contain a higher proportion of silica than labradorite, though that felspar is often present, and some distinguish a subgroup the labrador-diorites. In this case, however, much care will be needed to see that we are aot really dealing with a member of the dolerite group, where the augite, by paramorphic or other change, has been altered into hornblende. As in the case of the syenites, we have, then, in the holocrystalline division, diorite, mica-diorite, and augite-diorite, the last being of rare occurrence. For the hemicrystalline division there seems to be a general concurrence in favour of adopting the term porphyrite, which we can subdivide as in the case of felsite ; and for the hyaline we have the term andesite, which division is separable into the hornblende-andesites and the augite-andesites, the latter mineral occurring more frequently is these than in the porphyrites. In these, and especially in the latter, hypersthene has recently been frequently detected in con- siderable quantities, so that its presence requires to be noted by a prefix. Mica is not unfrequent. It is evident that the augite- andesites form a link with the basalts, and the hyperstheniferous augite-andesites approach the norites; to one or the other many of the rocks called melaphyres really belong. Wholly glassy forms no doubt exist, as in the last group. As a small outlying group from the syenites we have the minettes, which may be regarded as extreme forms of the mica-syenites, being composed chiefly of orthoclase and mica (commonly biotite), and the kersantites, extreme forms of the mica-diorites. Of both groups hemicrystalline forms, as well as those with a glassy base, exist; but distinctive names have not generally been assigned to them. Asa rule, they contain a slightly lower percentage of silica than the normal syenites and diorites. They occur also, so far as I know, in masses of very limited extent, mostly dykes and veins, and are commonly, though not universally, of Pre-Mesozoic age. We arrive now at the concluding pair of groups, which differ from the last described in these respects :—quartz is present as an essential constituent, and not as an accessory; in the orthoclase group mica is much more common than hornblende; and mus- covite, or a light-coloured mica of some kind, which has hitherto been rare even as an accessory, becomes sometimes an important constituent. As before, transitional forms between the two groups exist, and probably a plagioclase felspar is never wholly absent from the orthoclase group. That, however, may be defined, when holocrystalline, as essentially consisting of quartz -+ orthoclase+ mica, and is the familiar granite. Some have proposed to restrict this name to those varieties where the mica is muscovite, and to call those with biotite by the name granitite; the name pegmatite is ANNIVERSARY ADDRESS OF THE PRESIDENT. 73 useful for varieties exceedingly poor in muscovite. At present we are obliged to designate the hemicrystalline members quartz- porphyry or quartz-felsite (I would call these elvanite, were not the name so radically bad, or eurite, had not that term, in sym- pathy with its etymology, been used vaguely); here also we wait for a name*. Hyaline forms, as might be expected, are more common than ever; those in which individualized constituents (commonly microlithic felspars) abound are called indifferently quartz-trachytes, liparites, and rhyolites, though the last term is generally applied to more compact and so less rough (or less trachytic) varieties. The first term is open to the objection already stated; the second to this, that the rock abounds at many places besides the Lipari Islands; while the third perhaps indicates too distinctly the appearance of haying once flowed. If, however, it were agreed to use trachytic as an adjective, and call trachytic rhyolites the rocks usually named quartz-trachytes, the difficulty would to some extent be avoided. At present the most glassy members of this and the next group receive the names of pztch- stone and obsidian, the former name being applied to rocks with a resinous lustre, due probably to individualization of ex- tremely minute microliths, and the latter to the most perfect glasses, which also have a more distinct conchoidal fracture, that of the pitchstoues often being splintery. In the second group the name quartz-diorite is commonly applied to the holocrystalline members, which may be defined as quartz+ plagioclase+ hornblende (biotite being here decidedly less common than in the other); but I think the name tonalite greatly preferable, for as this rock appears to be far less common than granite, it may be allowable to use the name of a locality where it occurs in a huge and very typical mass. For marked varieties we should have the names mica-tonalite and augite-tonalite, the latter probably being very rare. For the hemicrystalline division we have at present no other name than quartz-porphyrite; but for the hyaline division, corresponding with the quartz-trachytes, we have fortunately the name dacite. Of the most glassy varieties I have already spoken. It may be remarked that free quartz appears to be less common with the plagioclase felspars than with orthoclase, perhaps because albite contains a higher percentage of silica than orthoclase. Extremely glassy forms also may prove to be rarer in this case, because, as I am informed, a soda-glass is more lable to set up crystallization than a potash-glass. From the above remarks it will appear, not only that our nomen- clature is at present in much confusion, due in part to the want of any definite principles, but also that the inherent difficulties are considerable, owing to the existence of transitional forms. At the same time I believe that there is sufficient predominance of what I * Granophyre has been proposed by some distinguished German authors ; but this term has been used in more than one sense. In fact, as will appear from the latter part of this address, I believe the subgroup will have to be rearranged, because its structure is often of secondary origin. 14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. may call type-forms to justify us in the assumption of the existence of species for purposes of classification, and I trust that I have indicated a natural and logical principle on which to proceed. The relations, then, of the groups may be expressed graphically in the annexed diagram. rs ; (3) — eS, = e oS 3 A 2 3) 5 bes eB =. @ SS =>, S -4- ~— — < e I 2 - me S =i Ce — ~ — ~~ S Sra : 3S “= 2 : / = oS = se : E man es 2 ‘ = = ‘ = Se] i . x \| Phonolite, Nephelinite. / / nities of the Pr groups is muc lagram. | ite the A the d [Nors.—The alliance of the Phonolite and 'lephi in Leucitite. Dolerite. Diagrammatic Representation of S = ~_— i) s = a ~ In the above sketch of what appears to me a natural system of classification, I take no notice, as above stated, of the geological age of the rock, which is regarded as of primary importance by many continental investigators, who consider Pre-Tertiary igneous rocks always separable from those of later date. For this distinction I ANNIVERSARY ADDRESS OF THE PRESIDENT. 75 have never been able to find any solid ground, and will briefly indi- cate the reasons why I venture to dissent from several eminent authorities. At the outset, we naturally feel some surprise that the commencement of the Tertiary period should coincide with so marked an epoch of change in the history of petrology, so that the igneous rocks, like the mammalia, should be en pleine évolution after the close of the Secondary period. But we may further ask, Was there any long pause, any universally definable limit, between the two periods? Did the curtain fall for an interval between two acts of the drama of life played on the world’s stage? Granted that Tertiary can be sharply defined from Secondary in Britain, or even in parts of Enrope, can that line be drawn everywhere? Palaontolo- gists, geologists in general, will, I think, accord in returning us a “negative answer. Still, admitting the impossibility of adopting any very hard and fast line, there is yet a possibility that a certain “ evolution” may exist among the inorganic products of the earth, and that the older may be distinguishable from the newer rocks. Let us then inquire how far this idea is in accordance with facts. The older rocks, of course, are more likely to have undergone mineral changes during the vicissitudes of their longer history. The less stable minerals will have disappeared, and their constituents will - berepresented in more stable forms. Olivine will have been changed into serpentine and iron peroxide: augite and diallage into some form of hornblende, or all these will have been replaced by viridite or chloritic minerals: felspars will have been replaced by zeolites or other alteration-products ; their materials may have been employed in the composition of tourmaline and epidote, and the like. If the rock has had a glassy matrix, this may have been devitrified. In short, an ancient rock, like a living creature, can hardly fail to exhibit signs ot old age. Thus we naturally expect to find such rocks as serpentine and diabase among the older formations, and should hardly expect that a Pre-Cambrian or an Ordovician lava would be absolutely identical with one emitted during the latest geological epoch. Further, as we hold that the more coarsely crystalline rocks, especially when members of the more acid division, have solidified beneath the pressure of superincumbent rock-masses, we should expect such rocks as granite to be usually of ancient date, not be- cause a modern granite may not exist underground, but because it has not yet been exposed to view by denudation. It must, however, be remembered that there seems no reason to doubt the Tertiary age of some of the granite of the Inner Hebrides; cértain Alpine granites also seem to me to be most probably Post-Secondary; at any rate I have seen in the West-central Alps perfectly typical granite cutting Lower Cretaceous strata, and I know of no indications of disturbances in that region until the Tertiary period had begun. Tertiary granite is also said to exist in the island of Jamaica. Some of the Carbo- niferous basalts of Scotland are admitted to be undistinguishable from those of Miocene age; most of them only differ by reason of subsequent mineral change. Restore the rock (and that it can be restored admits, I think, of no reasonable doubt) to its original con- dition, and your diabase resumes its place in the ranks of the normal 76 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. dolerites. Notwithstanding what has been written of late, I can- not admit that some of the altered peridotites and the serpentines of the Apennines are other than intrusive, if not in Eocene, at any rate. in the latest Cretaceous strata, and thus, as deep-seated intrusicns, cannot be in any case older than the earliest part of the Tertiary. Yet these are undistinguishable in all essential characters from olivine rocks and serpentine, which would generally be regarded as Paleozoic or, in some cases, Mesozoic. At our last meeting Professor Judd told us of Tertiary peridotites, picrites, and gabbros in the He- brides not to be distinguished from similar rocks of far earlier dates. Indeed some authors have been so impressed with their ancient aspect as to insist on classing these gabbros with the norites of the Upper Laurentian. We find yet stronger instances of similarity among the andesites and rhyolites. Mr. Teall*, in his excellent papers on the Cheviot rocks, has shown that, except for alterations which can only be attributed to the effect of time, some of the porphyrites of that region are chemically and mineralogically undistinguishable from the hyper- stheniferous andesites of Tertiary or yet more recent age. Mr. S%. Allport has shown that the devitrified perlitic rock of the Wrekin, which is indubitably older than the Lingula Flags, and in all proba- bility is one of the later Pre-Cambrian lavas, is as nearly as possible . identical, chemically, mineralogically, and structurally (except for devitrification) with the perlitic obsidian of Hlinik, near Schemnitz, and corresponds very closely with another Post-Secondary obsidian from Hungary. The red felsite, which in North Wales is found below the base of the Cambrian series, exhibits in some localities a fluidal structure, and every indication of having once been a true — glass, and is chemically identical with the above rock from Schemnitz; while several of the lavas of the Ordovician series in Wales, as has been pointed out by Mr. Rutley and myself, are, except in this one regard of devitrification, not to be distinguished chemically or microscopically from recent rhyolites, exhibiting fluidal or perlitic or spherulitic structures. JI have never been able to satisfy myself as to the distinction, insisted on for some time, between propylites and andesites, and I find that this is now repudiated by some of the best American petrologists. In lke manner there was no reason for coining the barbarous term felsi-dolerite for the reception of some of the lavas of the Lake-district. Chemically, the majority are typi- cal andesites, a few are basalts rich in glass, very similar to those of Tertiary age, and there are no other differences than such as are pro- duced by lapse of time. In short, after a fairly exhaustive study of “‘ felstones” and “ trachytes ” I may say that I am unable to recognize any distinctions between the more ancient and the more modern, be- sides those due to subsequent change, and that it is no more possible to connect these with any single epoch in geology than grey hair in the human subject with any one year of life. The strongest arguments in favour of the division have been derived from the “ mica-traps,” the nepheline and the leucite rocks, * Geol. Mag, Dec. 2, vol. x. ANNIVERSARY ADDRESS OF THE PRESIDENT. Ta all, it will be noted, rather rare and exceptional rocks. The first, it is true, for long time appeared to be universally of Paleozoic age, and in England it is only lately that (in Devonshire) they have been found to cut rocks so late as Carboniferous; but M. Barrois has described kersantites*, which, in his opinion, are certainly Post-Cretaceous, and most probably Post-Eocene. ‘The majority of the nepheline rocks are Post-Secondary. I am not aware that any nepheline-basalts have as yet been identified prior to the Tertiary period, but although many phonolites also belong to the latter, representatives of this group of earlier date are by no means wanting. I will not press the case of those remarkable masses of nepheline rocks which break through Silurian limestones and so strangely interrupt the level plane of the St. Lawrence Valley in the district near Montreal, although the opinion of Canadian geologists is in favour of their antiquity, be- cause | am not aware that there is any actual proof of their age; but I may remark that the nepheline-syenite, which one would naturally, from its appearance, class with the Pre-Tertiary representa- tives of this group, contains perfectly typical nepheline ; while some of the phonolites clesely resemble European phonolites of Tertiary age. For a like reason I abstain from quoting the Wolf Rock of Cornwall, and even the liebenerite-porphyries of the Fassa Thal, although I think that the latter cannot well be later than some part of the Mesozoic period. But in any case I am unable to recognize more than a varietal difference in the so-called elzeolite-syenites, or any real distinction between the nepheline which occurs in the foyaite of Portugal, considered by Dr. Sheibner to belong to the more ancient eruptive series, and that in sundry rocks of Tertiary age. Little can be made of the restriction to Post-Secondary rocks of such rare minerals as hatiyne and nosean, or of tridymite, which is very possibly not an original constituent, and very easily overlooked. It is of no avail to quote such minerals as tourmaline, topaz, beryl, zoisite, andalusite, staurolite, cyanite, &c., as restricted only to Pre-Tertiary rocks, because there is no evidence that any are proper to igneous rocks, and most are distinctly minerals of metamorphic origin. Muscovite also will not, I think, avail much, as its identity and history are yet far from clear. The strongest point in favour of the classification by geologic age can undoubtedly be made with the leucite rocks, for there can be little doubt that all which have been described are comparatively modern. Further I am not aware of any good ground for suspecting that in any of the more ancient rocks which have been microscopically examined this mineral has once been present, but has been replaced by pseudomorphs. Still we must bear in mind that in this respect negative evidence is not of great value ; for the mineral is an exceptional one, being peculiarly rich in potash, and typical leucite rocks are very rare—so rare that for some time no instance was known beyond the limit of Europe. The experience also of Messrs. Fouqué and Lévy appears to me to be significant. They melted together microcline and black mica, the composition of the mixture being 810,=40, Al,O,=17, Fe,O,=8, * Recherches sur les terrains anciens des Asturies, &ec. p. 160. 78 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. MgO=21, K,O=10 (Total = 96*): the composition of a leucitite poor in silica and rather exceptionally rich in magnesia, the result being that they obtained “aprés recuit, un culot crystallin composé de leucite, de peridot, de melilite, et de fer oxydulé, c’est-A-dire, une variété de leucitite a péridot.” This interesting result appears to suggest that microcline may, under certain circumstances, be the representative of leucite, notwithstanding their different percentage of silica; or, to put it otherwise, that the magma which, under certain circumstances, mav crystallize as leucite and olivine, with melilite (or with slight differences probably augite), may, under others, form microcline and biotite (potash-iron mica). It is alsa to be noted that these observers found that the leucite crystallized only at a high temperature; thus in making artificially a leucotephrite from a mixture representing one part of augite, four of labradorite, and eight of leucite, the leucite crystallized at a ‘‘ rouge-blane,”’ the felspar at “‘rouge-cerise” 7. Thus it seems to me unsafe, in the present state of our knowledge, to rely too much on negative evidence afforded us by this one exceptional mineral. It appears, then, to me that this attempted classification of igneous rocks into an older and younger series, notwithstanding the autho- rity and a few facts which can be quoted in its favour, not only is in itself improbable, but also is opposed to the general results of investigation, so that its retention will impede far more than it will facilitate progress. The order of solidification of the more important rock-constituents presents us with some peculiarities worthy of notice. The separa- tion of iron-oxide takes place at a very early period—probably in * This may be modified so as to come nearer to 100, thus :-— SiO, =41:0, Al,O, = 17-42, Fe,0,=8'2, MgO=21°52, K,O=10°25, Total=101°39. + The experiments, indeed, of MM Fouqué and Lévy (described in their ‘Synthése des Minéraux et des Roches,’ a work of the highest value to geologists) appear to me to be so suggestive as to the history and relationship of igneous rocks, that L present the results in a tabular form (it will be remembered that the experiments were made by “dry fusion”). (i) Negative results. They have failed in obtaining artificially rocks containing free quartz, or- thoclase, albite, white mica, black mica, and hornblende. (ii) Positive results. They have succeeded in obtaining artificially andesites and andesitie por- phyrites, labradorites and labradoritie porphyrites, basalts and Jabrado- ritic melaphyres, nephelinites, leucitites, leacotephrite, and lherzolite. (iii) Results indicating relationship. (a) 10 parts of oligoclase with 1 of hornblende produced an augitic andesite : 4 parts of microcline with 4°8 of biotite produced the leucitite mentioned above. (4) Microcline with oligoclase, nepheline, and augite produced in each case a glass in which were oligociase, nepheline, and augite, with- out any trace of a monoclinic felspar. (¢) A rock composed of wernerite and hornblende produced a characteristic augitic labradorite with a little melilite. Minerals, however, which they have failed to obtain as constituents in artifi- cially produced rocks, have been separately formed by MM. Fouqué and Lévy, and other experimenters,—e.g orthoclase, albite, and a brown mica, generally after long exposure to a high temperature. Free quartz also has often been pro- duced by the intervention of water. It will be observed from the above that, except, perhaps, in the case of lherzolite, they have chiefly succeeded, as might be expected, in producing examples of the less deep-seated igneous rocks. ANNIVERSARY ADDRESS OF THE PRESIDENT. 79 all cases this group of minerals is the first to solidify; even in the thin sahlbands of tachylyte we note the cloudy agglomerations of dark dust, globulites or trichites, which indicate incipient differentiation. These often, when well marked, are surrounded by lighter zones, indicating that the segregatory process has continued after motion was arrested in the mass; but we may remark that, in the perido- tite group, the presence of a large amount of magnesia appears to have been unfavourable to the complete separation of the iron- oxide, so that a large quantity has remained as an iron-silicate in such minerals as olivine, enstatite, &c. There is usually as much, sometimes more, iron in a peridotite than in a basalt; yet a slide of the latter exhibits many more granules of iron-oxide than the former. Olivine appears to consolidate at a high temperature; but in the rocks rich in magnesia the bisilicates of the enstatite group, and perhaps those of the pyroxenic, appear commonly to have crystal- lized before it, though the difference cannot have been very great, since these minerals occasionally include (as in the well-known bastite-rock of the Harz) granules of olivine. If, however, the con- stituents of felspar are present in any appreciable quantity, then the olivine is anterior in solidification to the above magnesian bisilicates ; for in the picrite group they frequently include grains of it, as does a brownish mica which occurs occasionally. Asarule, the felspars, including nepheline and leucite, when their constituents are present in large quantities, appear to separate out at an early period; they are then generally anterior to the pyroxenic mineral, and, what is remarkable, the more basic (and in the case of the true felspars the more fusible varieties) separate out before the more acid, so that the remaining magma contains a higher percentage of silica than the separated minerals. In accordance with the same principle and as an extreme case, quartz usually solidifies last in order. We find, however, even in rocks of tolerably uniform structure, whether coarse or fine, not unfrequent anomalies, so that it is almost impos- sible to draw up a table of minerals in the order of their solidifi- cation ; and when we study those which occur porphyritically, the difficulties become greater. The following table exhibits some of these anomalies :— Minerals occurring Composition of Ground-mass*. porphyritically *. Peridanise eo @UVERE L282 T sie eee toe deca { a are aunt see Sasa Dolerite ...... Labradorite t--augite ............ { mre ei So Syentie ...... Orthoclase+-pyroxenic mineral ! ee ae ee (also. biobite) ..3..0:.5.a.ak- J Drorite~5..-.: Plagioclase+pyroxenic mineral { Soa eee plagioclase is a more basic (algo biotite)”. acs OSES. eek kind, with hypersthene. Same minerals, but quartz Granite ...... Minerals of syenite+quartz...... only in hemicrystalline or glassy varieties. Tonalite...... Minerals of diorite+ quartz ...... Td. * Oxides of iror and spinel group omitted. t+ Name used generically ; may include anorthite. 80 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. An explanation of these anomalies does not at first sight appear hopeful; we may, however, notice :— 1. That the temperature of consolidation for a mineral out of a magma is not necessarily identical with that of the isolated mineral, as one substance acts as a flux upon another. 2. That the more anomalous results are presented by the rocks which appear to have cooled rather rapidly. 3. That the presence or absence of water greatly modifies the circumstances both of fusion and consolidation. 4, That Prof. Daubrée’s experiments indicate that pressure and the presence of water are favourable to crystal-building. For instance, in a granite or a tonalite it is obvious that the quartz has been the last mineral to consolidate, while in quartzi- ferous felsites and porphyrites, in rhyolites and dacites (even in the most glassy varieties), it is not rare to find good-sized grains, even bipyramidal crystals of quartz, among the porphyritic minerals. In regard to this, it seems worthy of remark that, among minerals so occurring in the non-holocrystalline rocks, a distinction is obser- vable, some being so perfectly developed that they seem as if they had consolidated out of the enclosing magma shortly before it solidi- fied, while others appear to have been subsequently modified ; the latter being more or less cracked, fragmentary, corroded at the exterior, and sometimes bordered by ferruginous and other minerals. These distinctions probably indicate difference of history. In the former case I should regard it possible that the molten matter, during its upward passage, had been arrested for a considerable time in a position where any further fall of temperature was practi- cally prevented, and the contained water was unable to escape: then crystal-building would go on; possibly the development of quartz might be favoured by an increase of the pressure * from the masses welling up behind. When the resistance in front is over- come, the fiuid mass passes upwards and outwards, its temperature falling and its water escaping, so that further crystallization is impeded, and the mass assumes a hyaline or, at any rate, hemicrys- talline condition. The fracture of included minerals may be explained by strains set up during the motion of the enclosing magma as it approaches the condition of a solid body, while the exterior corrosion probably indi- cates that some local rise of temperature, or increase either in pres- sure or in the quantity of water, has affected the stability of the molecules in the crystal. It must be remembered that, during the intermittent upward progress of a lava-stream, its outer parts, by contact with cooler rock, may at times lose enough heat to allow of the formation of crystals during a pause (for I think that the constant shearing of the molecules in a moving mass would be unfavourable to the development of crystals of any size); but that when the mass again moves onward, the more solid crystalliferous crust may be efaed into the interior of the mass, where the tem- perature has remained higher and its environment is different. It * Prof. Daubrée’s experiments show that pressure and water are very favourable to the development of quartz-crystals. ANNIVERSARY ADDRESS OF THE PRESIDENT. 81 is not impossible that some of the peculiar cases of zonal structure in crystals may be due to changes of position, sometimes slight, during the process of formation. For instance, I think it extremely probable that the zones of albite enclosing the large orthoclase crystals in the “‘porphyroid” of Mairus in the Ardennes (I have no doubt this rock is of igneous origin) are the records of two phases in its history. In this way also very possibly the enclosure of hornblende by augite crystals, or, vice versd, of nepheline by sodalite, &c., may be ex- plained. Definite pressure also during the process of crystal-building cannot fail to produce a marked effect. It may, I think, be taken as an axiom that, ceteris paribus, a molten mass under pressure will crystallize more readily than one not so affected. It is very possible that the devitrification of many of the ancient volcanic glasses has been largely due to the pressure which they have undergone from being buried deep below superincumbent strata. Molecular move- ment within limits can take place in many substances long before they cease to be solid, as is indicated, among other things, both by the ordinary devitrification of glass and by Prof. Daubrée’s special expe- riments ; and the mere fact that, in most cases, the specific gravity of a substance is higher in a crystalline than when in a colloid state, indicates the probable result of the application of pressure. But on the present occasion I shall as far as possible avoid what may be called subsequent metamorphosis, and confine myself mainly to structures which are due to the application of a force definite in direction during the process of crystallization. 1. Crystals, already formed, will be arranged with their longer axes in the direction of a tension, or at right angles to a pressure. This, as every one knows, is the explanation of flow-structure in microliths, and it is sometimes exemplified in the case of larger crystals. 2. Crystals, when forming, if exposed to a tension or pressure, will develope with their longer diameters in the direction of the tension, or at right angles to the pressure. This is especially well exhibited by platy minerals, such as mica and diallage. The foliated aspect of granites and gabbros near to their junction with a level surface of stratified rock has often been noticed; but as I observe that in the newly awakened enthusiasm for subsequent pressure as an agent in modifying rock-structures there is some danger of these being overlooked, I shall venture to recall a few from my own experience. J have often noticed that a mass of granite intrusive into a bedded rock has, for a depth of several inches, its mica-plates parallel with the surface of junction, and without the slightest sign of crushing. The most remarkable instance which I have ever seen was in the neighbourhood of Bergen ; there a vein of granite, rather more than a foot thick, threw off a band some three inches wide into a transverse fracture in the schist. It was obvious that the angles of the latter rock, one being about 60°, the other about 120°, would offer resistances definite in direction to the viscid mass of the granite. Accordingly the plates of mica in the latter (as usual, not numerous) were arranged perpendicularly to the normals to the | 82 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. surface of the schist ; so that they resembled little fish which were turning aside from the main stream to swimupthe branch. I have » / aicealy described to this Society* eases of foliation developed in masses of gabbro in the neighbourhood of a junction with bedded rock, and one yet more remarkable where a vein which cut a mass of serpen- tine and had forced its way between two layers of a large included fragment of bedded rock, preserved its ordinary structure so long as it remained in the former, but became foliated when it was nipped, | as between two boards, by the latter. I have also seen in a trapezium-shaped intrusive tongue of gabbro, the diallage parallel with each of the three sides exposed to view. There is, however, | a marked difference between the foliation in these cases and that | presented by rocks ordinarily called metamorphic. In the former } the structure is generally less conspicuous under the microscope, | and the crystalline constituents present the same characteristies of h external form as in the ordinary igneous rock; but in the latter (whatever may have been the cause of the foliation—crushing of a2 rock already consolidated, or mineral change in a rock originally of fragmental structure) there is a marked difference. The process of crystallization is the disturbance of equilibrium i among the constituent molecules; that which was homogeneous is so no longer. The formation of large erystals appears to be analogous to that of smal], and to be only a question of time. _ When we find a rock full of minute crystals, we may conclude that by a too rapid fall of temperature, freedom of motion was impeded and the separate crystallites were prevented from uniting. In this consideration we have to bear in mind the following facts, as stated above :— (a) That a hyaline condition is rare and local among the more basic rocks. (5) That in the majority of cases the more basie mimerals separate first, so that the residue is rendered more acid, and thus, under changed circumstances, may more readily assume a hyaline condition (and so impede movement) than the original homogeneous magma would have done. (c) That the minerals first formed will be the most perfectly de- veloped; when two minerals are both il developed, or sometimes one, sometimes the other, developed at its fellow’s expense, the erystallization-point for the two is probably, ceieris paribus, nearly identical. (d) That the fusion of an igneous rock is not ‘‘ dry fusion,” but fusion in the presence of water; and the sameis true of crystallization, though the free discharge of water from voleanoes may bring the cases of certain lavas nearer to that of ‘dry solidification.” This may be the cause of the unusual abundance of tachylyte in some of the Hawaiian volcanoes, as these discharge little steam from their molten but ebullient surface. (ec) That pressure modifies the circumstances of crystallization. * Quart. Journ. Geol. Soc. vol. xxxiii. p. 893. ANNIVERSARY ADDRESS OF THE PRESIDENT. 83 It may also be important as preventing dissociation, especially of water. Let us now examine the mode of crystal-building in a volcanic glass, putting aside for the present the consideration of the crystals which occur porphyritically ; because, as will be shown, there is no reason to associate their formation with this last stage of consoli- dation. A volcanic glass, when molten, may be either homogeneous throughout or not homogeneous. The former might produce a homogeneous solid, of which a piece of window-glass would be a perfect type; the latter a glass streaky from the occurrence of different substances, like various slags and very many glassy lavas. This is obviously due to the imperfect mixture of two materials (how mixed, matters not for our present purpose) of slightly different chemical composition, the masses of which during motion are drawn or “‘ teazed ” out into shreds. Considering for a while the former case only, we see that the molten mass may solidify without marked separation of any of its chemical constituents, though this is rare. Commonly, numerous microliths are formed, and the history of these, if traced, throws much light on the process of crystal-building. For this purpose no better examples can be found than some of the well-known pitchstones of Arran. On examining a slide from one of these with an objective of low power, we see that the clear glass of the rock appears full of a minute spicular dust ; on applying a higher power (say 3” objective) the particles of this dust are seen to be very small pale-green belonites, disseminated pretty uniformly and without orientation. ‘Taking another slide, we perceive a number of larger belonites, and in parts of the same or in a third slide we find curiously tufted groups of the belonites, or aggregations of the smaller on the larger, like miniature spruce-fir trees. Now each one of these—larger belonites, tufted groups of all kinds —will be surrounded by a lacuna of perfectly clear glass, while be- yond that, there will be interspaces crowded, as above, with the spicules. Moreover a closer examination of the larger belonites will often show that they are compound in structure, built up by the laying side by side of the spicules; and further that in the fir- tree-like groups the branches, where they inosculate with the stem (to use a simile), sometimes make with it at first a comparatively small angle, and then stretch out more nearly at right angles, exactly as we see the young branches start at an acute angle with the upper part of a fir-stem, but afterwards drawn down by the increasing weight of the bough (a botanical fact of which I may remark, by the way, many artists take no note). It appears, then, pretty clear that either the increasing viscosity of the surrounding material, or the resistance of the tufts to which they were already attached, prevented these spicules from being incorporated into the main stem. Why in parts of the rock we have a uniform distribution of the spicules, and why in others they are able to aggregate as above, we cannot say ; but probably it is due to some very slight irregularity—an almost infinitesimal difference might suffice—in the 84 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. composition of the rock. Some slides, however, illustrate another form of disturbance of equilibrium: crystals of quartz or felspar are imbedded in the rock, and on these the larger belonites have, as it were, grown, in accordance with a well-known law of crystal- building, that a mechanical disturbance of equilibrium is favourable to it, and every crystallite seeks its zov aro. Let us now proceed to the igneous rocks which are comprehended in the general term ‘ trachytes ;” rocks which still retain a glassy base, but have it crowded with microliths ; in which also there is commonly a slightly lower percentage of silica than in such glassy forms as pitchstone and obsidian. Here we find crystallites of felspar largely developed, together with granules of augite, horn- blende, and magnetite; these occasionally are so far associated as to afford instances of twinning, and they vary notably in size. In these rocks we are presented with a stage of crystal-building somewhat analogous to that just described, though taking place in a rock of slightly different composition. This microlithic structure appears to me to indicate that temperature (as in the former case) was changing rather rapidly, and crystal-building was arrested before it had progressed beyond one or two of its earlier stages. Hence I fully expect that it will be restricted to rocks which have either been emitted as lavas or, if intrusive, have solidified not far from the surface of the ground, that is, under circumstances which have allowed of comparatively rapid cooling and perhaps the free evapora- tion of water. Let us now for a moment turn our attention to the larger crystals of quartz, felspar (and, in some more basic examples, nepheline and leucite), biotite, augite, and hornblende, which we find in porphyritic varieties of these rocks. These are not seldom found to have incor- porated into themselves portions of the ground-mass or microliths of other minerals such as occur in the rock, which have been forced to obey the law of crystallization of their captor, and to arrange themselves conformably to it. Instances are too common to require enumeration. I interpret this to mean that the magma was main- tained for a considerable time at the temperature requisite for the separation of some particular mineral, and only slightly below that at which some other mineral, present in a very much smaller quantity, had solidified. For instance, in the ease of magnetite and leucite, the latter mineral begins to form in a magma in which scattered granules of the former have appeared. First, probably, there is a gene- ral development of microlithic leucites; next, owing to a slight non- uniformity of conditions, certain of these act as centres of attraction. The first tendency will be for the leucite microliths to aggregate and, in so doing, to exclude the magnetite, if it be only sparingly present ; but after a while the nucleus becomes larger, the magma possibly slightly more viscous. Motion is not quite so free, and the converging microliths of leucite bring with them granules of magne- tite, and, it may be, the enlargement of the nucleus (as mentioned above) facilitates crystal-formation ; hence the granular magnetite is included in the crystal. (It must be remembered that when one ANNIVERSARY ADDRESS OF THE PRESIDENT. 85 mineral is in the act of crystallizing and the other has crystallized, the latter is inert while the former is active.) It may also happen that in this crystal-building the attached microliths are now diverted in this way, now in that; thus twin-building of various kinds will result, and I should expect that this twinning might be more perfectly developed by molecular rearrangement after the crystal had formed, but while it was still plastic. If this process of aggregation of one or more minerals be carried on to a considerable extent, the residual magma will obviously differ much from the original. At last this also may begin to crystallize. Then, if the fall of temperature, or the change of conditions be very slow, we shall have a coarsely crystalline mass enclosing the earlier developed crystals; but if the change is more rapid, one more finely erystalline will be produced. If the magma contain the constituents of minerals, of which any one (under the circumstances) crystallizes at a markedly higher temperature than the rest, we may expect perfect crystals of that to occur; if not we shall find that the minerals, though thoroughly crystalline in structure, are very imperfect in their external form. In the case of slow consolidation it is obvious that if we suppose at different points in the mass the existence of centres of attraction of any kind, acting uniformly in eyery direction, the microliths as they form will be aggregated around them with a radial structure and thus will form spherulites. On this structure I have some further remarks to make, in relation to vitreous rocks, in which it is far more common; but I may point out here that the curious orbicular diorite may be thus explained. In these globular masses we can generally see a more or less indistinct nucleus, then follows a series of subspherical bands of anorthite and hornblende, the former. predo- minating. ‘The process, then, appears to be as follows :—The two minerals have crystallized almost simultaneously, the felspar having had very slightly the advantage. The nucleus, possibly only in consequence of the accidental presence of a slight excess of anorthite, acts as a centre of attraction, and anorthite from the parts of the magma in immediate continuity. separates out and collects radially upon the existing nucleus. But after this segregation of the felspathic constituents from the magma has gone on for a certain time, there is a zone of it in which is a residual excess of the horn- blendic constituents, so that circumstances now admit of the forma- tion of the latter mineral; and thus a zone of it is built up, until again the inequality is more than redressed, and the formation of anorthite recommences. But this will not go on indefinitely ; for general crystallization of a non-radial character will have been set up in the mass, so that at last molecular motion becomes impossible. The construction of spheroids ceases, and they are enclosed in an ordinary diorite. I notice that where the boundary of the spheroid is the most sharply defined, the outer ring is a thin one and ig hornblende, as it should be with the mineral second in order of - formation. Leaving, then, for a moment, certain structural peculiarities, such VOL. XLI. a \ | | : 86 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. as spherulites, let us see how far we can connect those which we commonly meet with in igneous rocks. Commencing with the hyaline stage (omitting minerals of an- terior consolidation, and restricting our remarks to the rocks con- taining a fair proportion of felspar), we seem able to trace the following order of phenomena in rocks which do not remain in a condition so vitreous as the tachylytes, pitchstones, and obsidians :— A. (1) Formation of a large number of felspar microliths, so that these become the most conspicuous objects in the ground-mass, in which, however, more or less glass usually remains. This gives the trachytoidal structure of many authors, and indicates a compara- tively rapid fall of temperature, so that crystal-building is arrested at a rather early stage. (2) Further development of the felspars, until their chemical constituents are wholly, or almost wholly, removed from the magma, followed by crystallization of the residue. This is the ophitic structure of authors, most perfectly developed when the residue has the composition of a pyroxenic mineral and itself crystallizes rather coarsely—a structure, I think, indicative of more gradual cooling, but still under no great amount of constraint. Not usual in the more acid rocks. B. (1) Structure minute ; but a glassy base is not distinguishable. Want of definiteness of external crystalline form, as though some- times the separation of adjacent minerals had not been absolutely perfect, or an irregularity of boundary, as though crystallization had been simultaneous. Occasionally there is some approach to a coordination of structure, a more or less imperfect micrographic or spherulitic arrangement being visible. This is the petrosiliccous structure of authors, indicative, I believe, of constrained consoli- dation. (2) Generally a coarser structure than the last. The separation of the minerals is more complete, and the felspars tend to have rectilinear boundaries. The microgranulitic structure of authors, which perhaps ultimately may be in great part classed with the next one, the remainder belonging to the first, and both belonging chiefly to the less basic rocks. (3) Fairly coarse felspars, usually well-defined externally, espe- cially in the more acid varieties, the granitoid structure of authors, - especially characteristic of granites, tonalites, most syenites and diorites, and gabbros. This last method of crystallization seems to belong to very deep- seated rocks, where consolidation has taken place under great pressure and in the presence of confined water-vapour ; certain eases of (2), and perhaps some of (1), indicate the same process carried on more rapidly, and so occur frequently in vein-granites and intrusive felstones. The first, or petrosiliceous type, however, requires much discussion, and with some remarks on questions relating to this, I must conclude this already too lengthy address. For many years the subject of the minuter crystal-building has been present to my thoughts, although the pressure of what I may ANNIVERSARY ADDRESS OF THE PRESIDENT. 87 call larger questions has prevented me from devoting to it much of the time which I can secure from daily duties. It was a question to which my work in Charnwood and North Wales obliged me to pay attention, and [ may mention that it is now seven years since I published a paper in the ‘ Geological Magazine’ which dealt with the possible mode of formation of some spherulitic rocks in Arran. This will, I hope, be my excuse for putting before you some of the results of my own work, without direct reference to what others may have written on the subject. The question propounded to us by the study of ‘this class of rocks in the field is practically this: Has the petrosiliceous, the spherulitic, the micrographic structure been produced during the original cooling of the rock, or has it been subsequently brought about? and if it has been produced at either time, is there any hope of distinguishing what I may call original from secondary devitrification? Besides studying a large number of natural rocks, I have examined some artificial glasses in the hope of obtaining some help from them. I have to acknowledge with gratitude the assistance which I have received, both in information and by the gift of specimens, from Professor Judd, Mr. J. A. Phillips, Messrs. Osler, Mr. F. Claudet, and Mr. Frederick Siemens, of Dresden. To the last two I can hardly adequately expressmy thanks. Lach, from the funds of his practical experience, gave me much information; each made me a liberal gift of specimens, Mr. Siemens even having some specially prepared for me. J may add that in the time at my dis- posal since these reached me, it has been impossible to do full justice to the many interesting questions to which they give rise; but I hope to make them the subject of further study. Specimens of artificial glasses vary considerably in composition. The following are analyses (furnished me by M. Claudet) of fint- glass (I. and II.) and a (French) bottle-glass III. * * M. Pelouze also, in his article Sur le Verre, Compt. Rend. Ixiv. p. 53, gives the following analyses :-— Ordinary Glass. Sine Mes 77-04 73:05 77-80 COWEN 285.2%. 741 1516 12:50 Wa.O cerctsec S51 «179... 9:70 99°96 100°00 100-00 Alumina glass. Maenesia glass. S. G. 2-380. (Easily devitrified.) SUS er ereere 75:00 St 0 aye eee 68°9 65:7 i219 Seite 7°60 RNC), « coussrees 14-9 12:0 INGOs Bu. .-anat 17°40 AO). «e552. a 73 — L5G ES 16:2 15°0 100-00 88 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. i. 0 III. SiO, .... 6470 69°65 Si0;° ft 68e5 ALO; 2/4 po 50U eet ee Al,0, . 6-01 CaO: “ye ul3-00 oF Sail Fe,0,. 5-74 Na,O....:19°80 15-22 C800 6.52992 — K,O 5-48 100:00 100-00 100-00 In flint-glass the percentage of silica is often higher, that of alumina lower, and those of lime and soda more nearly equal than in (L.). In fact, we might take as an approximate composition of a typical flint-glass about 70 per cent. of silica and about 27 per cent. of lime and soda, in nearly equal proportions, the residue consisting of alumina, iron, manganese, &c. The presence of alumina, as is well known, renders the glass less fusible. Hence, in order to obtain devitrified specimens, Mr. Claudet was in the habit ef sprinkling a | little clay on the residual glass in a pot. (This, I think, acted mechanically as well as chemically, as probably it was not ‘wholly melted.) Compound silicates also, he informs me, were more fusible than simple. In the comparative study of artificial glasses and of igneous rocks there are, however, two obvious difficulties—one, that the former, as indicated above, contain a much larger percentage of lime and of an alkali than we find in obsidians, pitchstones, or rhyolites, and that in regard to them we are dealing with dry fusion and dry solidification (Mr. Siemens informs me that it is an important matter to allow the ‘‘ metal” to boil for a considerable time, 7. ¢. to eliminate from it vapours and gases). As I had been informed that Messrs. Siemens were making bottle-glass from “‘ granulite” or granite, I had great hopes of obtaining from them an artificially produced obsidian, and thus being enabled to study the devitrification of a_ substance chemically identical with a natural rock. This, I regret to say, is not quite the case. Their staple material is a granite or granulite, of which analyses are given below*, but a certain quantity of calcium fluoride and sodium chloride or sulphate are added. I was not informed of the exact amount; Mr. Siemens says it is done rather roughly, but “‘so as to make a good alkaline glass.” Hence, even in this glass, we have more lime and alkali, as well as less magnesia, than we should find in such a rock as an andesite, on iB Light-coloured Dark-coloured variety. variety. Sn 0 eevee 69°30 60°90 AO oe on 17-70 19°10 iO eee 1-10 310 C208 cee 1-60 2°90 MeO. 2s: 0:13 0-80 KO) Be 3°45 4-10 NaOn ce 5°20 5°53 Wile erence 1-25 3:27 Difference contains H F, MnO, &e. ANNIVERSARY ADDRESS OF THE PRESIDENT. 89 with which probably the silica and alumina percentages would more nearly correspond. Nevertheless, though this fact obliges me to hesitate at present as to the identification of the minerals formed during devitrification, these specimens have proved of great assis- tance*. | It will be convenient to describe very briefly the results of my examination of the various glass specimens referred to above, before indicating their bearing on the deyitritication-structures of natural rocks. q In ordinary window-glass two types of crystals appear to be developedt. One consists of long acicular prisms of a clear mineral with a satiny lustre, like that of pectolite. These form spherulites (sometimes more than an inch in diameter in the body of the glass), but they also, as we might expect, form a more or less mamillated layer, starting from the exterior portion of the mass, especially where in contact with the sides of the pot. Both are composed of thickly crowded tufts of acicular or hair-like microliths, exactly like the growth of microcrystalline quartz which we can study in the chalcedonic linings of cavities in rocks. Sometimes they form radiate hemispheres, the plane face being the surface of the glass, the centre not seldom a little speck, which appears to have been one of the clay granules mentioned above. ‘The second type is a mineral of a less satiny lustre and apparently not quite without colour, the larger aggregates having a faint ochreous-grey tint. Its habit of crystallization appears to be entirely different. Commencing with an elongated flattish prism, smaller prisms attach themselves to the sides at angles of about 60°, and to these in lke way others are added. Occasionally the rachis, as I may term it, of the leaf becomes curved. These, again, combine into stellate six-rayed forms, reminding us of the well-known snow crystals, and develope into flattish hexagons like those figured by Vogelsang in the eighth and ninth plates of his work ‘ Die Crystalliten,’ except that the outer boundary appears sharper than in those on the latter plate. A remarkable twinning now takes place, two composite crystals placing themselves at angles of 60° with the plane of the first plate, so that a vertical section would give us a six-rayed star. This process continues, but with a certain dominance of crystals lying in the original direction, so that its result is an aggregated mass of somewhat flattened forms, the longer diameter of which sometimes measures nearly an inch. At the ends it is rather concave, and its sides still retain a somewhat hexagonal shape. I may give a general idea of the appearance by comparing one of these to a ball of cotton * Tam, of course, aware of the glass formed from melting basalt; but on account of the rarity of glasses and structures suggestive of ‘“ devitrification ” among the more basic rocks, I have not thought it worth while to spend much time over them. + Mr. Claudet informs me that these spherulites were produced by stopping all the orifices of a furnace, and allowing it to become cool yery slowly, the time occupied before the cooling was completed and the pots were withdrawn being from 8 to 10 days. go PROCEEDINGS OF THE GEOLOGICAL SOCIETY. as ordinarily sold, if its sides were compressed by its being placed in a hexagonal box. Both of the above crystalline aggregates appear to be sharply separated from the enclosing glass, which, I may remark, is often cracked for some little distance round them, as though by strain in subsequent cooling. Although the latter microliths appear to form tufted and sometimes spherulitic masses, like the former, by the crowding of the branch-like forms, so that they are compressed together like the twigs in a broom, yet I am disposed to regard the two as distinct varieties, if not distinct minerals. Probably, how- ever, the difference in chemical composition is but slight. Their occurrence, often in the middle of a mass of perfectly homogeneous glass, leads one to suspect that they differ but little from it in com- position, and are crystals of some lime-soda silicate, chemically as nearly as possible identical with the glass*. So far as I can at present ascértain, each is a monoclinic mineral. Mr. F. Siemens sent me a specimen of “ granulite glass ” containing spherulites, taken ‘‘out of an old tank-furnace cooled down slowly with about 1000 ewt. of glass in it.” The fragment is of irregular form, about 5” x3" x2", of a rich resin-brown glass, containing several spherulites beautifully developed, most of them about 1” diameter, sometimes a little more; they exhibit a radial structure, with one distinctly zonal in the exterior part, forming a kind of “rind” about *2” thick. The inner part is of a pale yellowish-grey colour and has a slightly unctuous lustre; the outer has a pinker tinge and deader lustre: but the outermost zone, perhaps =-th inch thick, more nearly resembles the interior. When examined under the microscope these spherulites are not very translucent, of a dusty grey colour and rather earthy aspect; the radial structure is rather irregular, the spherulite being apparently composed of a matted mass of rather curved acicular microliths; the zones are indicated by darker bands and there are some interesting minor peculiarities on which I must not dwell, except to say that beyond the spherulite is a very thin fringe of minute colourless crystallites. This mineral is probably an aluminous silicate, and resembles that in some spherulites which I have seen in obsidians and pitchstones ; perhaps it is an impure microlithic oligoclase. In all these specimens, described above, the various crystallites have formed during the cooling of the mass from a molten condition, * Mr. Claudet tells me that some years since, he analyzed a glass and one of the enclosures, and found no substantial difference between them. I may add that Vom Rath’s analyses of a pitchstone and a spherulite from Antisana (Andes) give but little difference. Dumas’s analyses of a glass and its crystal- lized inclusion, however, show a decided difference :— Vitreous part. Crystallized part. SiO, < sebocsees 64°70 68:20 AIO! in tootag 3°00 490 Ca ge cnanace 12:00 12-00 Na,0) etree 19°80 14-90 ANNIVERSARY ADDRESS OF THE PRESIDENT. gi and thus illustrate what we may term primary devitrification. It represents a segregation of certain crystalline minerals from the body of the glass, which, however, undergoes no change whatever that is visible to the eye in the other part, the free ends of the microliths being bounded by a true glass, apparently identical with that in other parts of the mass. I now turn to some examples illustrative of changes produced by the action of heat upon specimens which have once been perfect glasses. The first, given me by Mr. F. Claudet, is one of great interest. It consists of a number of sheets of window-glass, which, when lying one on another, were exposed to great heat in the noted conflagration at Hamburg, and partially fused, so that they now form an almost solid mass about #? inch in thickness, with thin alternating bands of opaque-white and of clear glass, not unlike a banded rhyolite. A closer examination shows that, except at top and bottom, each white band is more or less double, half belonging to the underpart of one sheet, and half to the upper part of that in contact with it. Each is composed of a tufted growth of very minute acicular crystals of a pale brownish-grey colour. Usually their close approximation - compels them to exhibit a brush-like structure; but occasionally where there are slight interruptions, we have more or Jess perfect half-spherulites, and in a few cases where the fusion of the surface appears to have been complete, we have a perfect spherulite, whose equatorial plane represents the former junction-faces. As the glass has not been completely melted, it seems probable that the spheru- lites are due to a crystallization of, not from, its material, and they clearly originated at the surface of the sheets. A specimen, prepared for me by Mr. F. Siemens, further illustrates this. A group of four pint bottles of different-tinted granulite glass was exposed for twenty-four hours to a temperature of about 600°C. The heat has not sufficed to fuse the bottles, but they have been completely softened, have fallen together and become welded into an irregular flat cake, though the necks, lips, even the letters stamped on the bottles, can be readily distinguished. We have thus had about the same approach to fusion as in the former case. Here, too, a fracture ee one of the bottles shows at either surface a white skin about 3 th inch thick, duplicated as before, where two surfaces have been welded together; but between these, in the clear glass, are numerous small spherulites ‘from 1 sth to 51th of an inch in diameter. Here, again, one would imagine the chemical differences between the crystalline bodies and the glass must be extremely slight. The mineral has a similar aspect with, and is probably the same as, that in the larger spherulites described in the slowly cooled mass of eranulite glass. I am indebted to Mr. F. W. Rudler for a specimen of great in- terest. This is a fragment of a plate of glass, about 11 inch thick, devitrified by exposure in a crucible to a bright red heat for three weeks. A slide cut from it exhibits many points of interest on which I have not time to dwell; but the following have a special bearing on the question before us. So far as I can ascertain, there 92 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. is no residual glass; a fair quantity of an earthy dust, and sundry globulites have formed, also a number of minute belonites ; but the dominant structure consists of crowded “ brushes” of an acicular mineral with a general resemblance to that of the first type described above. The most interesting point, however,is that the fragment has three external faces, parts of the front, back, and an end of the plate ; the acicular microlithic aggregates grow out from each of them until they meet, where a sharp divisional line is formed, visible even to the unaided eye, clearly indicating that the crystallites started simultaneously from each exterior face, and grew inwards till they met. The structure is roughly represented in the annexed diagram. Here, as the whole glass is devitrified, the dominant crystallites must be nearly identical in composition with it. Section of a fragment of devitrified glass. Tn concluding this subject, I must recall to your memory the most important experiments of M. Daubrée on common glass. These, however, were performed in closed tubes in the presence of water (about one third of the weight of the glass)*. Here the composition of the glass was considerably altered, quartz crystals were developed, with many belonites of a silicate, with spherulites and a tufted growth, probably of chalcedony, and with afew grains of pyroxene. The irregular crowding of the spherulites is very noteworthy, and the effect of the surfaces of the glass on the grouping of the structures produced by the alteration. A study of M. Daubrée’s remarks and plates appears clearly to indicate that there is a great difference between the results of mere “heat” devitrification as described above. and those of “‘ heat-water-pressure ” devitrification. The experimental evidence above cited indicates that consider- able structural change and possibly some amount of molecular segregation involving actual change of relative position (which is certainly considerable when water is present) can take place when a solid body is rendered moderately plastic, but without fusion. This is further illustrated by such facts as the kernel-roasting of copper- * «Etudes Synthétiques de Géologie Expérimentale, vol. i. pp. 159-171. C sition :— "ea SiOiaiee re Rete ee 68-4 VME ¢ Seo aap eneecesn ee eee 49 Op 5s ee ees re 12-0 MgO) oe 22-22. -nree-- 2 a) | Fk ) eee Reno = Aes 147 ANNIVERSARY ADDRESS OF THE PRESIDENT. 93 ore. That similar processes can go on in nature is suggested by the numerous instances which we witness in studying the conversion of olivine-rock into serpentine, of pyroxene into varieties of horn- blende, the formation of tourmaline in granite, and the like. I believe also that many of the oolitic grains in limestones are struc- turally true “spherulites ” developed after the rock was more or less consolidated ; and that such is the nature of the radiate balls in the magnesian limestones of Durham can hardly be doubted. Many other instances of “ concretion” might readily be mentioned, notably those singular forms in the flinty slates of Eskdale; but theabove may suffice. I formerly pointed out that the spherulitic structure of certain felsites in Arran could only be explained on the supposition that they had been produced by a metamorphic action due to a subsequent intrusion of an igneous rock. The structures of the devitrified glasses also show us very clearly how great an influence the slightest disturbance of equilibrium has on the initiation and direction of crystal-growth. The discontinuity, and consequent difference, due to the mere existence of a surface—what we may term the surface tension—has sufficed to originate crystallization in each one of these cases of artificial secondary devitrification. Thus my examination of a large number of igneous rocks in the light obtained from the experimental evidence described above leads me to the following conclusions :— (1) That spherulitic and other microlithic structures can be produced in a glassy rock during cooling. (2) That they may sometimes originate from a nidus (as it were) of slightly different mineral composition, which thus starts crystal- lization. (3) That they very often originate by the mechanical aid of some included crystal or particle. (4) That perhaps still more often they are the result of some kind of strain analogous to that of the artificial cases described above. This might occur especially in banded rocks, as the difference in composition in the layers might cause them to contract unequally. (5) That these microlithic structures, unless too crowded, are sharply separated from the surrounding glass. (6) That they can also be produced by subsequent heating short of fusion, and that, except perhaps that the results are more obviously connected with local disturbance of equilibrium, there are no means of distinguishing between “ dry heat ” devitrification and “ slow cool- ing” devitrification. But the experiments of Prof. Daubrée have produced results not wholly identical with those of the dry-heat action ; and to this ex- periment the process which has taken place in nature must have been more nearly analogous ; that is to say when “ devitrification,” in the strict sense of the word, has been produced in a rock once glassy, the agents of change have been pressure, water, heat, the elevation of temperature being probably in most cases very moderate. How far, then, is it possible to distinguish the results of this from those of ** cooling devitrification,” the only other kind likely to occur, except very locally, in nature ? VoL, XLI. k 94 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. An examination of Prof. Daubrée’s results suggests that the devi- trifying action has been more universal and simultaneous throughout the mass than in the above-described cases of “dry heat” or “cooling” devitrification. It is true that the surfaces of the mass have, in this case also, produced modifications ; but spherulites appear to have started almost simultaneously from many independent centres, so as to form a crowded mass, interlocking with irregular outlines, instead of a number of large spherulites, which, if they come into contact, are parted by more uniform surfaces. The formation also of innumerable microliths throughout the whole mass of the glass is not well paralleled in the instances of ‘“ dry-heat ” devitrification. Now on examining cases where we may reasonably conclude that a devi- trification (in the strict sense of the word) has occurred in nature, we are struck with certain structural peculiarities. We may, I think, assume that the existence of a perlitic structure in a rock is an indi- cation that it has once been atrue glass. Isolated spherulites and a well-marked banded structure are, I believe, also presumptions in favour of the same; though in the latter case portions may have assumed a crystalline condition in cooling. If, then, we examine slides of such rocks as the devitrified perlitic lavas of the Wrekin district, we observe that the secondary structure presents certain peculiarities. Not seldom it bears a definite relation to the cracks by which the perlitic mass is traversed, a thing not surprising, because these cracks, as pointed out some years since by myself, and as indicated to you during the present year from another point of view by Mr. Rutley, may have from the very first been connected with pressures or strains of some kind, and this disturbance of equi- librium could scarcely fail to tell when crystallization commenced. There are, indeed, instances to be found where the depolarization- phenomena ordinarily seen in a colloid body subject to strain seem to have been rendered permanent. The devitrification-structures in these perlitic rocks differ much from those which [have observed in any case where there was a reasonable probability of their being the result of the original cooling. It is difficult to express it in words, without entering into lengthy and minute details unfitted for the present occasion; but I may epitomize them thus :—the slide throughout exhibits a peculiar confusedly crystalline structure, the individualized minerals sometimes being of extreme minuteness. The ground-mass appears to be composed of a mixture of quartz and felspar ; but itis exceedingly difficult to say which has been first to consolidate, some- timesthe one, sometimes the other, appearing to have had the mastery. Now and then a felspar crystal exhibits a rectilinear boundary, but very commonly it appears to granulate into the quartz, and sometimes the felspathic mineral (I am doubtful whether it is a true felspar) resembles a kind of residuum or “ sediment,” left unused when the quartz grain had formed. The latter mineral frequently occurs in little groups of moderately distinct, though crowded crystals, as may be observed in some cases of chalcedonic formation in veins and cavities. Close intercrystallizations of the quartz and felspars, leading to all kinds of imperfect spherulitic, micrographic, and den- ANNIVERSARY ADDRESS OF THE PRESIDENT. 95 dritic structure *, are common ; and not seldom tiny spherulites occur, whether singly or in crowded groups, of that indefinite external character already mentioned. In short we have a number of struc- tures similar, so far as I can judge, to those figured by MM. Fouqué and Lévy in their magnificent work ‘ Minéralogie micrographique,’ plates xi., xii.(2), xiv., xv., and xvi. (1): in the last, I believe, at any rate the larger spherulites are of anterior consolidation. Ihave found characters more or less similar prevail in the “ felstones ” beneath the base of the Cambrian of North and South Wales, in the compact lavas from Charnwood, in the more compact of the Ordovician lavas from Wales, and in many other similar rocks. It is, in fact, generally found in those ‘“ felstones” which have a compact, smooth, and sometimes subconchoidal fracture, but hardly so much as a glimmering lustre. Hence it appears to me that the petrosiliceous structure of the above-described character is probably always the result of secondary devitrification, in which pressure and water (acting for a long time) have been more important than heat. It has nearer relations to the microgranulitic structures found in certain vein-granites and intru- sive felstones than to the trachytoidal structure of lava-flows ; which is not surprising, seeing that the former structures have probably been set up under considerable pressure and in the presence of water. Thus we appear to have two groups of structure : one, the trachytoidal and ophitic, which are more generally the results of drier and less constrained cooling; the other, the petrosiliceous, microgranulitic, and eranitoidal, indicative of the presence of some water and the existence of much constraint, the first of these three being probably almost entirely a structure of secondary origin; for I expect that we shall find on further study that we shall be able to distinguish even the more minutely microgranulitie rocks from the truly petrosiliceous; but on this point I will not venture to speak at all positively, as I have not been able to study so many specimens of these vein-granites as I should wish to have done. Still I think we may safely affirm that the majority of the petrosiliceous rocks owe their structure to a peculiar form of subsequent devitrification, and so, as atered rhyolites, obsidians, and pitchstones, belong more properly to the metamorphic rocks (of igneous origin). I have throughout spoken, as I stated I should do, with little reference to the work of others, because I thought that there might be a certain interest and advantage in presenting what I had to Say from a personal point of view, since on nearly every point I have striven to form an independent conclusion, and often the result of many hours’ work has been condensed into a few words. I¢ has been work, I fear you will say, leading to little result; but perhaps its very incompleteness may suggest lines of research to other workers, Another reason why I have referred little to the investigations of others is, that in each case one ought in justice to be sure of naming the original observer. Now to do this would have involved much * T use the last term for want of a better name to express cases where the minerals resemble crowded branches or rootlets. 96 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. additional labour, of a kind unprofitable to one’s self. The great demands made upon my time for the last four years by duties only indirectly connected with science have compelled me to be a little selfish, and have precluded me from the careful study of a good deal of contemporary literature, now becoming fearfully voluminous. But I cannot conclude without stating how much I owe to many fellow- workers—to Daubrée, Fouqué and Lévy, in France, to Renard in Belgium, to Vogelsang, Rosenbusch, and Zirkel, in Germany, to many Americans, above all Wadsworth and Dutton, and, in our own country, to Sorby, Phillips, Teall, Judd, and Allport; all of these last named have aided me in every possible way, freely furnishing me with specimens and frankly imparting to me their own ideas. To the last, Mr. 8. Allport, I feel myself under a special obligation. Fourteen years ago, when I began to study the microscopic structure of rocks, there were few books and, in England, very few petrologists. Mr. Allport had already more than mastered the preliminary diffi- culties, and had got together a fine collection of rock-slides, his own handiwork. This collection and all that he knew were at my service whenever I could visit Birmingham. To him I used to carry my perplexities, and from him I got that help which, in my new stage of work, was invaluable. I can say with truth that had it not been for his assistance, as well as your indulgence, I might never have attained to the honour of addressing you from this chair. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 97 February 25, 1885. Prof. T. G. Bonney, D.Se., LL.D., F.R.S., President, in the Chair. Bennett Hooper Brough, Esq., Assoc. R.S.M., 5 Robert Street, Adelphi, W.C.; Parvati Nath Datta, Esq., 10 Blackwood Crescent, Edinburgh ; Robert Stansfield Herries, Esq., B.A. Cambr., 53 War- wick Square, London, 8.W.; William Herbert Herries, Esq., B.A. Cambr., Shaftesbury, Te Aroka, Auckland, New Zealand; Rev. Edward Jordon, Ravenscroft Park, High Barnet, N.; Lees Knowles, Ksq., M.A., LL.M., Westwood, Pendlebury, near Manchester; and William Hobbs Shrubsole, Esq., Sheerness, were elected Fellows of the Society. The List of Donations to the Library was read. The following communications were read :— 1. “On a Dredged Skull of Ovibos moschatus.” By Prof. W. Boyd Dawkins, M.A., F.R.S., F.G.S. 2. “On Fulgurite from Mont Blanc.” By Frank Rutley, Esq., F.G.S. 3. “On Brecciated Porfido-rosso-antico.” By Frank Rutley, Esq., F.G.S. 4, “Fossil Cyclostomatous Bryozoa from Aldinga and the River- Murray Cliffs, South Australia.” By Arthur Wm. Waters, Esq., F.G.S. The following objects were exhibited :— Specimens, exhibited by Frank Rutley, Esq., F.G.S., in illustra- tion of his papers. A collection of stone implements and two cut bones from the neighbourhood of Reading, Berks, exhibited by O. A. Shrubsole, Ksq., F.G.S. Two old oil-paintings of Vesuvius in eruption, exhibited by George Ellis, Esq. March 11, 1885. Prof. T. G. Bonney, D.Se., UL.D., F.R.S., President, in the Chair. William Lester, Esq., J.P., Bron Offa, near Wrexham, and VOL. XLI. ° 98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Thomas Stewart, Esq., Assoc. M. Inst. C.E., Cape Town, were elected Fellows of the Society. The List of Donations to the Library was read. The following communications were read :— 1. “The Granitic and Schistose Rocks of Northern Donegal.” By C. Callaway, D.Sc., F.G.S. 2. “On Hollow Spherulites and their occurrence in ancient British Lavas.” By Grenville A. J. Cole, Esq., F.G.S. Rock specimens aud microscopic sections were exhibited by Dr. Callaway and Mr. Grenville Cole in illustration of their papers. March 25, 1885. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. Charles De Laune Faunce de Laune, Esq., F.L.S., Sharsted Court, Sittingbourne, Kent; and William Hill, Esq., Jun., The Maples, Hitchin, Herts, were elected Fellows of the Society. The List of Donations to the Library was read. The following communications were read :— 1. “On the Relationship of Ulodendron, Lindley and Hutton, to Lepidodendron, Sternberg, Bothrodendron, Lindley and Hutton, Sigillaria, Brongniart, and Rhytidodendron, Boulay.” By Robert Kidston, Esq., F.G.S. [ Abstract *.] The Author commenced by expressing an opinion that the so-called genus Ulodendron of Lindley and Hutton comprised specimens belonging to several species which were referred to different genera. Unless the outer surface of the bark is well preserved, stems of Clathrarian Siqillarie and Lepidodendra are undistinguishable ; but species of Ulodendron have been in several cases founded on decorticated examples, and distinguished by such characters as the size of the Ulodendroid scar. The three species which have furnished most of the specimens described as Uloden- dron, and to the description of which the present paper was chiefly devoted, are Lepidodendron Velthewmianum, Sternb., Sigillaria dis- cophora, Konig, sp. (=U. majus and U. minus, Lindl. & Hutt.), and S. Taylori, Carruthers, sp. * This paper has been withdrawn by permission of the Council. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 99 The subject of the paper was divided into four heads. In the first an epitome of the views of previous writers on Ulodendron was given. The writers noticed were Steinhauer, Rhode, Allan, Konig, Sternberg, Brongniart, Lindley and Hutton, Buckland, Hooker, Sauveur, Unger, Goppert, Tate, Geinitz, Goldenberg, Miller, Eich- wald, Macalister, Dawson, Carruthers, Rohl, Schimper, Weiss, Williamson, Feistmantel, Stur, Thomson, Zeiller, Lesquereux, and Renault. In the second part the Author described the specimens belonging to the species named that he had been able to examine. The third part contained the general conclusions as to the nature of Ulodendron at which he had arrived. He commenced by defi- ning the four genera Lepidodendron, Lepidophloios, Sigillaria, and Rhytidodendron, as distinguished by the characters of their leaf- scars, and showed that Lepzdodendron, Sigillaria, and Rhytidodendron occasionally exhibit large scars, arranged in two opposite vertical rows. These are the Ulodendroid scars. They marked, in the Author’s opinion, the point of attachment of a caducous appendicular organ, which had in a very few cases been found in position. These appendicular organs were probably sessile cones. Details were given, showing the progressive development of the scars, the obliteration of the normal leaf-scars by the appendicular organs, and the branching of Ulodendroid stems. The concluding portion of the paper contained the synonymy at length and full descriptions of the three fossil plants, Lepidodendron Veltheimianum, Sigillaria discophora, and S. Taylori, together with the horizons and localities in which they have been found in Britain. Bothrodendron was shown to be a decorticated form of Ulodendroid stem, and Knorria a cast of the core of Lepidodendron. DIscussIon. Mr. Carrutuers, after expressing his sense of the value of the paper, remarked upon the difficulty of finding characters of real importance for grouping fossil plants ; hence fossil species and genera are based on very different data from those of recent plants. All the essential characters of the Carboniferous Lycopodiacesr, for example, may be found in the recent genus Selaginella. When he himself wrote on the subject he merely accepted the cha- racters of Ulodendron, and his only important difference from the Author was as to the organs borne by the Ulodendroid scars. There was a difficulty in the way of accepting them as cones in the fact that the scar is surrounded by a ring or distinct cicatrix where there was a connexion of tissue ; if so, impressions of leaves within the scar could not be left. All the markings on the lower portion of the scar are circular, indicating the places where vascular bundles passed through. In the upper part they are drawn out. Hence he had considered the organs borne by these scars as aerial roots, such as occur in the Selaginelle of the present day, allied to the Lycopods of the Coal-measures. The important point is, whether the 12 100 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. marks on the scar are marks of leaves or marks of bundles. Pro- bably these scars are found in different genera, but the scars may be of as great importance as the leaf-scars themselves for grouping the plants in genera. He thought the cushions and permanent leaf-bases, as in some living Cycads and Lycopods, were parts of the leaf, not parts of the stem. Prof. Boyp Dawxtns said that he had a large collection of Coal- plants under his charge in the Manchester Museum, including forms similar to those exhibited by the Author. This collection throws much light upon Lepidodendroid plants, and he agreed with the Author as to the propriety of classing together the various forms of Lepidodendra and Sigillarie. Prof. Williamson regarded all the species named as merely forms of Lepidodendroid plants. He was inclined to regard the Ulodendroid scars as impressions of seed- cones, and not of aerial roots, because on the best specimens of these scars there are impressions of whorls of leaves or modified leaves. In these plants the bark consists of several layers ; hence arise the various patterns exhibited, which have led to the estab- lishment of different genera. Prof. SeELEY said that in former years he had worked through some collections of Coal-plants. If Ulodendron were a good genus, then the internal difference of structure between Siqillaria and Le- pidodendron could not be general. The character of Ulodendron is apparently of not less value morphologically than the form of the leaf-scar. And, whatever the Ulodendron structure implied, Ulo- dendroid scars had been described by M‘Coy in a slightly modified Sigillarian trunk, running round the stem instead of vertically. M‘Coy thought that they were the places of attachment of rootlets. The phenomena seemed to be in favour of the development of fruit- organs, and not of roots from the Ulodendroid scars. The AvrHor, in reply, remarked on the generic distinctions be- tween the leaf-scars of Lepidodendron and Sigillaria. The constancy of leaf-scars throughout the plants shows that there are real generic distinctions between them. Some of the specimens exhibited showed the mode of attachment of the appendicular organ, and these could not be scars of appendicular roots, because they contain markings due apparently to leaves. The particular specimen on which Mr. Carruthers mainly founded his notion of aerial roots was not, in the Author’s opinion, Ulodendroid at all. The genus Arthro- pilus?, ?, described by M‘Coy, was founded on a badly preserved com- pressed stem. 2. “On an almost perfect Skeleton of Rhytina gigas = Rhytina Stelleri (‘ Steller’s Sea-cow’) obtained by Mr. Robert Damon, F.G.S., from the Pleistocene Peat-deposits on Behring’s Island. ¢ By Henry Woodward, LL.D., F.R.S., F.G.S. The following specimens were exhibited — Recent skulls of male and female Dugong (Halicore australis) and PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Io.t skull of Manatus senegalensis, also casts of bones of the éxtinct Rhytina trom Behring’s Island, exhibited by Dr. Henry Woodward, F.R.S., F.G.S., in illustration of his paper. A collection of plant-remains, exhibited by R. Kidston, Esgq., F.G.S., in illustration of his paper. Photographs of Hlasmothertwm from Post-Tertiary deposits at Novousenk, Gov. Samara, Russia, exhibited by Dr. Henry Wood- ward, F.R.S., F.G.S. April 15, 1885. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. John Rudd Leeson, M.D., C.M. (Edin.), M.R..C.8. Eng., 6 Copthall, Twickenham, Middlesex, was elected a Fellow of the Society. The List of Donations to the Library was read. The Secretary announced that a Kit-cat portrait of the late Sir Henry De la Beche, painted in oil-colours by H. W. Pickersgill, R.A., had been presented to the Society by the President; and that Messrs. Maull and Fox had presented 146 copies of photographs of Fellows of the Society. The following communications were read :— 1. “A General Section of the Bagshot Strata from Aldershot to Wokingham.” By the Rev. A. Irving, B.Sc., B.A., F.G.S. 2. “Notes on the Polyzoa and Foraminifera of the Cambridge Greensand.” By G.R. Vine, Esq. (Communicated by Thomas Jes- son, Esq., F.G.8.) [ Abstract. ] After commenting on the want of published information con- cerning the Polyzoa of the Cambridge Greensand, as shown by the fact that none are mentioned in Mr. Jukes-Browne’s list of the fossils (Quart. Journ. Geol. Soc. xxxi. p. 305), the author proceeded to explain the circumstances under which he had been entrusted with the whole of Mr. T. Jesson’s collection from the coprolite-bed for description. The collection is large and important, and the Polyzoa contained in it exhibit a facies distinct from that of the Jurassic beds on the one hand and of the Upper Chalk on the other. There is but little similarity between the collection now described and the forms known from Warminster and Farringdon. The majority of the Cambridge-Greensand Polyzoa occurred unattached to any matrix; i 102 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. but several examples of attachment have been observed, chiefly to Ostrea, Radiolites, and species of Cidaris. A list showing the range of the species described preceded the actual descriptions of the following kinds of Polyzoa and Forami- nifera, with notes on their relations &c. It included :-— PoLyzoa. Stomatopora gracilis, Milne-Edw. Lichenopora, sp. Idmonea dorsata, Hagenow. ? paucipora, Vine. Entalophora raripora, D’ Orb. Dromopora stellata, Goldfuss. Jessonii, sp. nov. polytaxis, Hagenow. striatopora, sp. nov. Osculipora plebeia, Novall. gigantopora, sp. Nov. Truncatula, sp. Diastopora cretacea, Vine. Membranipora cantabrigiensis, sp. , var. lineata, var. nov. nov. fecunda, sp, Dov. ; Microporella, sp. (? antiquata). —— megalopora, sp. nov. Lunularia cretacea, Defr. § D’ Orb. FoRAMINIFERA. Webbina levis, Solas. Trochammina irregularis?, D’ Orb. tuberculata, So/las. Textularia, sp. The following specimens were exhibited :— Specimens exhibited by the Rev. A. Irving, F.G.S., and G. R. Vine, Esq., in illustration of their papers. Sand-worn stones from Hokitika, New Zealand, exhibited by W. D. Campbell, Esq., F.G.S. Specimens illustrating the paper lately read by J. H. Collins, | Esq., F.G.S., on the Rio Tinto district. April 29, 1885. Prof. T. G. Bonney, D.Se., LL.D., F.R.S., President, in the Chair. James Backhouse, Esq., West Bank, York; Percy Bosworth Smith, Esq., Assoc. R.S.M., Government Mineralogist to the Madras Presidency, Madras; and James Shipman, Esq., 8 Manning Grove, The Chase, Nottingham, were elected Fellows of the Society. The List of Donations to the Library was read. The following communications were read :— 1. “On the Structure of the Ambulacra of some Fossil Genera and Species of Regular Echinoidea.” By Prof. P. Martin Duncan, M.B. (Lond.), F.R.S., V.P. Linn. Soc., F.G.S. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 103 2. “The Glacial Period in Australia.” By R. von Lendenfeld, Ph.D. (Communicated by W. T. Blanford, LL.D., F.R.S., Sec. G.S.) [ Abstract. | Although several previous writers have suggested that boulders and gravels found in different parts of Australia are of glacial origin, the evidence is yague, and no clear proof of glaciation has been brought forward. During a recent ascent of the highest ranges in Australia, parts of the Australian Alps, the author succeeded in discovering a peak which he named Mount Clarke, 7256 feet high, and in finding traces of glaciation in the form of roches moutonnées throughout an area of about 100 square miles. The best-preserved of the ice-worn surfaces were found in a valley named by the author the Wilkinson Valley, running from N.E. to$.W., immediately south of Miiller’s Peak and the Abbot Range. No traces of ice-action were found at less than 5800 feet above the sea. The rocks showing ice-action are all granitic, and the fact that the surfaces have been polished by glaciers is said to be proved by the great size of such surfaces, by their occurrence on spurs and projecting points, by many of them being worn down to the same general level, and by their not coinciding in direction with the joints that traverse the rock. In conclusion the author briefly compared the evidence of glacial action in Australia with that in New Zealand. Discussion. The PrustpEnt said that he considered that more evidence was necessary in order to establish the point contended for by the author. All his proofs were founded on granite, which had a con- stant tendency to form rounded bosses. The fact that the supposed roches moutonnées occurred on spurs réndered the matter still more doubtful, seeing: that in small glaciated tracts such surfaces were chiefly found in valleys. It was a remarkable and, to him, a very suspicious fact that no moraines or perched blocks were noticed. In fact the only point of importance adduced in favour of the author’s view seemed to be the difference in the direction of the joint-planes and of the rounded surfaces, and this he thought insufficient. Mr. BuanForp agreed with the President, and mentioned examples of the occurrence, in the plains of India, where glaciation was out of the question, of granite surfaces simulating roches moutonnées, and of larger dimensions than those cited by the author. It seemed to him not impossible that Dr. von Lendenfeld was right; but the evidence brought forward was certainly not sufficient. The circum- stance most in favour of a glacial origin for the supposed roches moutonnées was their restriction to a particular elevation. 3. “The Physical Conditions involved in the Injection, Extrusion, and Cooling of Igneous Matter.” By H. J. Johnston-Lavis, M.D., EGS ee [ Abstract *. ] The great disproportion between the displays of volcanic activity * This paper has been withdrawn by permission of the Council. Io4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. in the same volcano at different times, and between the eruptions of different volcanoes, is a subject deserving the most attentive con- sideration. The violence of a volcanic outburst does not bear any relation to the quantity of material ejected. The union of water with lavas may be compared with the solution of a gas in water; but there is reason to believe that in their deep-seated sources lavas contain little or no water. If igneous matter be extruded through dry strata, the eruption might take place without explosive manifes- tations. But if igneous matter be extruded through water-bearing beds, a kind of dialysis would take place between the igneous and aqueous masses. The amount of water dissolved in the magma will be proportienal to the length of time it is in contact with the aqui- ferous strata, the pressure, and the temperature of the fluid rock ; the violence of the eruption will depend upon the amount of igneous matter, the quantity of water dissolved in it, and its temperature when it reaches the surface. The intrusion of igneous matter into dry or nearly dry strata, the temperature and bulk of the magma will determine whether a sahlband is formed, or formed and re-fused, whether the rock cools quickly, forming a fine-grained structure, or very slowly, in which the result would be a coarse granite or syenite, according to the composition of the magma. The author showed how the cleavage- and stratification-planes ef rocks are suitable to the retention of subterranean heat. Intrusion of igneous matter into water-bearing strata was then studied, and it was shown that a process of dialysis goes on between the colloidal magma and the water in the porous strata, resulting in many inter- esting phenomena. The loss of heat in the magma from the ab- sorption of water will be little, and only that necessary to raise the water to its own temperature. It was shown how this absorption of water will result in the rupturing of the fissure towards the surface ; and the mechanism of a certain group of earthquakes was investi- gated. The occurrence of vesicular structure in dykes was discussed ; the mode of formation and probable process of re-obliteration is dependent upon the variation in pressure, temperature, &c. resulting from the enlargement of the fissure. It was then shown that the cooling of a dyke-mass will depend on the following conditions :— (a) Loss of heat from conduction away by the surrounding rocks. (6) Raising the acquired water to the mean temperature of the fluid of the fused silicates in which it is dissolved. (c) Heat-loss in consequence of expansion during extension of fissure. (d) Gradual escape of water in the form of steam or vapour through fissures, so supplying fumaroles. (e) Convection-currents of water forming geysers or thermo- mineral springs. The author combatted the theory that the simple contact of the molten rock with water-bearing strata is the cause of an eruption. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 105 The extrusion or eruption of igneous matter into the atmosphere was then studied, and it was shown that one of the irregularities in eruptive activity is due to the varying conditions which different parts of the magma have undergone before reaching the surface. The main varieties of volcanic outbursts were discussed: the violence is dependent upon the amount of magma and its contained water, which on relief of pressure expands with enormous rapidity, tending to reduce the whole mass to 100°. This process in explosive erup- tions accounts for the pumice and the vitreous structure of this type of eruption. The remarkable fact that the pumice-beds resulting from any basic explosive eruption are vitreous towards the bottom and become more crystalline as we approach the surface, was shown to be due to the slower cooling in consequence of less absorption of heat in converting water into steam as the eruption progresses. The various conditions which bring about the extinction of a vol- cano were then pointed out. The higher the volcano the more violent will be its eruptions ; but the intervals will be greater. The mecha- nism of a lateral outburst was then demonstrated. The amount of lava escaping from a given point laterally is far more than that contained in the chimney above, which is due to the welling-up of the portion below when relieved from the pressure of the column that occupied the upper part of the chimney. The discussion of the effect of the presence of volatile matter in modifying the composition and structure of igneous rocks is so long and intricate that it is impossible to render it in abstract; the eruptive phases of Monte Somma, Roccamonfina, Monte Vulture, Ventotene, and Monte Nuovo are givenas examples. The difference of the rocks produced will depend on— (a) Composition of the original magma. (6) Pre-eruptive temperature of the same. (c) Amount of enclosed volatile matter. (d) Amount of pre-eruptive crystallization. (¢) Rapidity of ejection. (f) Height of projection. (g) Temperature of the atmosphere. In the first appearance of a volcano, or the reawakening of one, vitreous pumiceous fragmentary products first appear, and pass by way of more microcrystalline pumice, pumiceous scoria, to actual lava outflows. Scoria differs from pumice in that the vesicular structure is derived from other portions of the magma, whereas in pumice it is formed, where found, by the intermolecular expansion and union of the resulting steam into bubbles. Vesicularity of lavas depends upon the amount of dissolved water and the viscosity of the mass. Volcanic ashes are the result either of the complete reduction of the magma to a powder by the enormous and rapid expansion of the magma in explosive eruptions, or of the grinding-up of the accessory ejectamenta derived from the crater-sides or from accidental ejecta- menta that may lie beneath the volcano, and into which the apex OOOO oa a te EE | i 106 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. of the crater may reach. In no case can an analysis of ash give ~ an accurate idea of the composition of the magma. The structure and composition of igneous rocks were next dis- cussed. It was shown that such minerals as amphibole, orthoclase, and some micas are pre-eruptive as to crystallization, whereas leu- cite and its allies, with pyroxene, are either formed in dykes under low pressure or by prolonged recuzt in the voleanic chimney, or after expulsion. The order of formation of these minerals is quite diffe- rent from their fusibilities, because they may be regarded as dissolved in the magma, and separate according to their degree of solubility in the glassy magma and according to the different elements, their proportions, and their affinities. The part played by the chlorides and sulphates as solvents of silicates was discussed, and it was shown how by their decomposition the hydrochloric and sulphuric acids escape in the volcanic vapour, and how the bases may aid in render- ing the magma more basic. These facts are borne out in the arti- ficial production of rocks and minerals. The author maintained that throughout the whole paper his arguments were based on known facts and physical laws. Discussion. Prof. Prestwich was inclined to agree with the author in his view that the contact of heated lava with water-bearing strata was an efficient cause of volcanic activity, but on some other points he could not agree with him. The following specimens were exhibited :— Specimens of Echinoderms showing the structure of the ambulacra, exhibited by Prof. P. Martin Duncan in illustration of his paper. May 13, 1885. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. William Horton Ellis, Esq., J.P., Hartwell House, Pennsylvania, Exeter, and Prof. J. Hoyes Panton, M.A., Agricultural College, Guelph, Ontario, were elected Fellows; and Prof. J. Gosselet, of Lille, a Foreign Member of the Society. The List of Donations to the Library was read. The Secretary announced that Dr. John Evans, F.R.S., F.G.S., had presented a copy of his photographic portrait. The following communications were read :— 1. “On the Ostracoda of the Purbeck Formation; with Notes on the Wealden Species.” By Prof. T. Rupert Jones, F.RS., F.G.S. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. . 107 2. “ Evidence of the Action of Land-ice at Great Crosby, Lanca- shire.” By T. Mellard Reade, Esq., F.R.S. 3. “The North-Wales and Shrewsbury Coal-fields.” By D. C. Davies, Esq., F.G.S. [Abstract *. | After discussing the origin of Coal-beds, and the causes of their variation in structure and quality, the author proceeded to describe the North Wales and Shrewsbury Coal-field, which consists of three parts :—(1) The Shrewsbury field south of the Severn, exclusively composed of Upper Coal-measures; (2) the tracts north of the Severn, extending from near Oswestry to north of Wrexham; and (3) the Flintshire Coal-field. The first and second are separated from each other by the alluvial plain of the Severn and Vyrnwy, and the second and third by the Great Bala and Yule faults. Some remarks on the scenery of the Welsh border-land followed, and then a general section of the Carboniferous system,as developed in the country described, was given, the Permian beds being in- cluded, as the Author considered them the upper portion of one great division of Paleozoic time. The section was as follows, with the maximum thickness of each subdivision :—- ; Thickness in yards. bla Te oanUSLOHGs. \.\.> 2 2h: ee %assce onus 210 } 1 2. Ifton or St. Martin’s Coal-measures ......... 75 : . 3. Red marls with calcareous matter ............ 180 co 4. Green rocks and Conglomerates ............ 125 SU pper Coal-meastires 25 ca. wen terce nanrcas ones 80} Go, Cet rock 60: Cetin) coal’. trate. ets c.ncvns--es OOTY Gloaleieaaiires 7. Cefn coal to Lower yard-coal................ DO ate 665 : valet 8. Lower yard-coal to Chwarcle coal ............ 80 | ge Pe, 9. Chwarcle coal to Millstone Grit ............ 135 ) 1255 yards. A detailed description of the strata was next given, beginning with the lowest, together with details of each coal-seam as worked in various parts of the field. After describing the beds from the Millstone Grit to the Cefn rock in the North-Wales coal-field, the Author proceeded to notice the Upper Coal-measures and Permian strata in the Shrewsbury area, andshowed that no break exists between the two, the former passing gradually into the latter. He then discussed the probability of Lower Coal-measures existing beneath the upper beds near Shrewsbury, and showed from sections that the existence of the lower measures might be anticipated. A similar inquiry as to the presence of the Coal-measures beneath the New Red Sandstone of the Vale of Clwyd should also, in the Author’s opinion, be answered in the affirmative. The organic remains found in the different beds were briefly noticed, and then the faults of the district were discussed at some * This paper has been withdrawn by permission of the Council. 108 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. length. The principal faults run north and south, with an upthrow to the east, but are crossed by lines of fracture running east and west. In conclusion, the correlation of the strata in the North Wales and Shrewsbury coal-fields, and especially of the coal-seams, with the beds found in other parts of Great Britain, was discussed, and a section was given to show the representation of the different measures in various coal-basins. The Author was disposed to adopt four subdivisions rather than three only, as usually accepted, and pointed out some of the characteristics of each subdivision. Discussion. Mr. Baverman remarked that but little attention had hitherto been paid to the interesting Coal-fields described by the Author, to whom thanks were due for the careful sections which he had made of them. Although the yield of these basins was not large when compared with those of the north of England and South Wales, they formed part of one of the largest deep-lying Carboniferous areas in the country, being the western limit of the great basin under- lying the plain of Cheshire. He thought, however, that the Author’s correlation of the seams throughout the whole of the English Coal-field (apart from that of Northumberland and Durham) was somewhat fanciful. That particular seams, say in the Wigan district, could be proved to be the exact equivalents of others in South Wales, and that both were exactly represented in interme- diate basins, such as the Forest of Wyre, appeared to be exceedingly improbable. The following specimens were exhibited :-— Specimens of Purbeck Ostracoda, exhibited by Prof. T. Rupert Jones, F.R.S., F.G.S., in illustration of his paper. Zinc-spinel and willemite, formed in a zinc-retort, exhibited by H. Bauerman, Esq., F.G.S. May 27, 1885. Prof. T. G. Borner, D.Sc., LL.D, F.R.S., President, in the Chair. George Ormond Kekewich, Esq., 62 Lansdowne Road, Notting Hill, W., was elected a Fellow of the Society. The List of Donations to the Library was read. The Secretary announced that six slides of Fossil Cyclostomatous Bryozoa from Muddy Creek, South Australia, illustrating the paper in Q. J. G. S. vol. xl. p. 674, by A. W. Waters, Esq., F.G.S., had been presented to the Museum by J. Bracebridge Wilson, Esq., of Geelong, South Australia. _—e : PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 109 The following communications were read :— 1. “On the so-called Diorite of Little Knott (Cumberland), with further Remarks on the Occurrence of Picrites in Wales.” By Prof. T. G. Bonney, D.Sc., LL.D. F.R.S., Pres.G.S. 2. “ Sketches of South-African Geology.—No. 2. A Sketch of the Gold-Fields of the Transvaal, South Africa.” By W. H. Penning, Esq., F.G.8. 3. “ On some Erratics in the Boulder-clay of Cheshire &c., and the Conditions of Climate they denote.” By Charles Ricketts, M.D., F.G.8. : The following specimens were exhibited :— Microscopic rock-sections and rock specimens, exhibited by the President, in illustration of his paper. Boulders, &c., exhibited by Dr. Ricketts, in illustration of his paper. June 10, 1885. Prof. T. G. Bonney, D.Sc., LL.D., F.R.S., President, in the Chair. The List of Donations to the Library was read. The following names of Fellows of the Society were read out for the first time, in conformity with the Bye-laws Sec. vi. B. Art. 6, in consequence of the non-payment of the arrears of their contribu- tions: —G. Bock, Esq., Rev. 8. Gasking, and W. Low, Esq. The following communications were read :— 1. “Note on the Sternal Apparatus in [guanodon.” By J. W. Hulke, Esq., F.R.S., V.P.G.S. 2. “The Lower Palzozoic Rocks of the Neighbourhood of Haver- fordwest.” By J. HE. Marr, HEsq., M.A., F.G.S., and T. Roberts, Hsq.,)B-A.30-GS. 3. *% On certain Fossiliferous Nodules and Fragments of Hematite (sometimes Magnetite) from the (so-called) Permian Breccias of Leicestershire and South Derbyshire.” By W.S. Gresley, Esq., F.G.8. [ Abstract. ] In this paper the author described certain pebbles of hematite and magnetite which occur in the so-called Permian breccias on IIo PROCEEDINGS OF THE GEOLOGICAL SOCIETY. the western margin of the Ashby-de-la-Zouch Coalfield. These pebbles, which are collected for sale and used as “ burnishers ” (for which their extreme hardness qualifies them) vary from a diameter of ;}; inch to the size of a man’s fist. They present many varieties of form, usually rounded and often very smooth, angular, and subangular ; a few contain cayites, which are often lined with fibrous botryoidal ore, or contain a group of crystals of calcite, or a kernel of soft pea-ore ; have sometimes an agate-like, and rarely a columnar structure, and occasionally exhibit well-marked magnetic polarity, others being simply magnetic. Sometimes they show dimpling, also grooving and striation resembling those produced by ice-action, whilst at other times they seem to have been crushed and recemented ; many of these markings are doubtless due to oscil- latory movement of the rocks en masse. Many of these pebbles contain fossils of various kinds, chiefly plant- and insect-remains, but with a few of Annelids, Mollusca, and Fish(?). All the fossils are of Carboniferous age (Coal-measures, for the most part). Amongst the associated rock-fragments in the breccias many bits exhibiting cone-in-cone structure occur, composed chiefly of a close-grained quartzose material; and a specimen showing the cones whose axes lie in radiating lines (the cones facing upwards, downwards, and ‘sideways or fan-shaped) has been noticed for the first time. From the consideration of all the facts detailed in the paper, the Author concluded that the nodules were originally composed of clay-ironstone, aud that they were derived from the Coal-measures, whilst other fragments were possibly of older date. He considered that the pseudomorphic action by which they have acquired their present composition must have taken place zn situ since their inclusion in the breccia. ; Discussion. The PresipEnt believed, from a study of the specimens in the Jermyn-Street Museum, that there was no evidence of the action of ice in the Permian breccias to which allusion had been made by the Author, but that the striation of the fragments, like the dimpling and crushing in the pebbles of more than one conglomerate, were due to movements of the rocks. Prof. Hueners regretted the absence of specimens. He could not understand the identity in mineralogical character of the pebbles with fossils, and of those with cone-in-cone structure. The following specimens were exhibited :— A specimen showing the clayicles and inter-clavicle of Iqguanodon, im situ, exhibited by J. W. Hulke, Esq., F.R.S., V.P.G.S., in illustra- tion of his paper. Paleozoic fossils, exhibited by J. E. Marr, Esq., F.G.S., and T. Roberts, Esq., F.G.S., in illustration of their paper. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. LE June 24, 1885. Prof. T. G. Bonnry, D.Sc., LL.D., F.R.S., President, in the Chair. John Macdonald Cameron, Esq., 36 Weltje Road, Hammersmith, W.; Matthew Heckels, Esq., Walker-on-Tyne, near Newcastle-on- Tyne; and Robert H. Williams, Esq., Assoc. M. Inst. C.E., Cuddra, near St. Austell, Cornwall, were elected Fellows of the Society. ‘The List of Donations to the Library was read. The following names of Fellows of the Society were read out fox the second time, in conformity with the Byelaws, Sec. vi. B. Art. 6, in consequence of the non-payment of the arrears of their contribu- tions :—C. Bock, Esq., Rev. 8S. Gasking, and W. Low, Esq. The following communications were read :— 1. “Supplementary Notes on the Deep Boring at Richmond, Surrey.” By Prof. John W. Judd, F.R.S., Sec. G.S., and Collett Homersham, Esq., F.G.S. 2. “On the Igneous and Associated Rocks of the Breidden Hills in East Montgomeryshire and West Shropshire.” By W. W. Watts, Esq., F.G.S. 3. “Note on the Zoological Position of the genus Microcherus, Wood, and its apparent Identity with Hyopsodus, Leidy.” By R. Lydekker, Esq., B.A., F.G.S. 4, “*Observations on some imperfectly known Madreporaria from the Cretaceous Formation of England.” By R. F. Tomes, Esq., F.G.S. [ Abstract. | This communication contained notes on several species of Cre- taceous corals. The author considered that Smilotrochus insignis of Duncan must be referred to the genus Ceratotrochus; that S. granu- latus, Duncan, was founded on immature specimens of T’rochocyathus Wiltshire, Duncan; that Micrabacia Fittoni, Duncan, is a variety of Cyclocyathus Fitton; that the genus Fodoseris, Duncan, and pro- bably Syzygophyllum, Reuss, are the same as Rhizangia, M.-Kdw. and Haime, and consequently P. mamuilliformis, Duncan, and P. elongata, Duncan, are species of Rhizangia. He further stated that Turbinoseris, Duncan, is identical with Leptophyllia, Reuss, and as the specific name de Fromenteli is preoccupied in the latter genus, he proposed to substitute the name Leptophyllia anglica, Tomes, for Turbinoseris de Fromenteli, Duncan. A new species, probably of Smilotrochus, from the Gault of Folkestone, and a new Jsastrea from Atherfield were described, -and notes added on the occurrence in British localities of Barysmilia tuberosa, Reuss, B. Cordieri, M.-Edw. VoL. XLI. m i12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, and Haime, Pleurosmilia neocomiensis, E. de From., of a small form of Astrocenia, and of Isastrea Reussiana, M.-Edw. and Haime © (=Ulophyllia crispa, Reuss). The occurrence of Beaumontia Egertoni, derived from the Carboniferous Limestone, in the Upper Greensand of Cambridge, was also recorded. Discussion. Dr. Duncan said that the specimens called Ceratotrochus by Mr. Tomes were not before the Society, and that with one or two ex- ceptions the other forms remarked upon were represented by very indifferent specimens. The so-called Rhizangia had no stoloni- ferous part and had synapticule, therefore it did not belong to the genus, but to that to which he (Dr. Duncan) had assigned the Hunstanton coral in the Palzontographical Society’s Memoir. He was satisfied that the types of Smzlotrochus he had examined, and which were well drawn by De Wilde, had no columelle. He ob- jected to the use of the term “ imperfectly known” in the title of the paper, as it reflected even upon the work of Mr. Tomes. He would have preferred M. Cotteau’s term “ little known.” 5. “Correlations of the Curiosity-Shop Beds, Canterbury, New Zealand.” By Capt. F. W. Hutton, F.G.S. 6. “On the Fossil Flora of Sagor in Carniola.” By Constantin Baron von Ettingshausen, F.C.G.S. The following specimens were exhibited :— Specimens, exhibited by Prof. J. W. Judd and C. Homersham, Esq., in illustration of their paper. Rock specimens and fossils, exhibited by W. W. Watts, Esq., in illustration of his paper. Specimens of Labyrinthodont fossils belonging to Mastodonsaurus and a form allied to Capitosaurus, from Central India, and of Hyperodapedon, from India and Warwickshire, exhibited by R. Lydekker, Esq. Specimens from the well-borings at Chatham Dockyard, Crossness, and Harwich, exhibited by the Director-General of the Geological Survey. A series of fossiliferous nodules and fragments of hematite from the Permian breccias of Leicestershire and South Derbyshire, ex- hibited by W. 8S. Gresley, Esq., in illustration of his paper, read on the 10th inst. Cretaceous Corals, exhibited by R. F. Tomes, Esq., in illustration of his paper. . ADDITIONS TO THE LIBRARY AND MUSEUM OF THE GEOLOGICAL SOCIETY. Session 1884-85. I. ADDITIONS TO THE LIBRARY. 1. PERIODICALS AND PuBLIcATIONS oF LEARNED Socrertes. Presented by the respective Societies and Editors, if not otherwise stated. Academy. Nos. 634-660. 1884. ——. Nos. 661-685. 1885. Analyst. Vol. ix. Nos. 100-105. 1884. ——. Vol.x. Nos. 106-111. 1885. Annals and Magazine of Natural History. Ser. 5. Vol. xiv. Nos. 79-84. 1884. Purchased. H. J. Carter. On the Spongia coriacea of Montagu, = Leucosolenia coriacea, Bk., together with a new Variety of Lewcosolenia lacunosa, Bk., elucidating the Spicular Structure of some of the Fossil Calcispongie ; followed by illustrations of the Pin-like Spicules on Verticillites helvetica, De Loriol, 17.—G. R. Vine. Notes on Species of Ascodictyon and Rho- palonaria from the Wenlock Shales, 77,—R. Kidston. On a new Species of Lycopodites, Goldenberg (L. Stockii), from the Calciferous-Sandstone Series of Scotland, 111.—A. de Quatrefages. Moas and Moa-hunters, 124, 159.—R. Etheridge, jun., and Arthur H. Foord. On two Species of Alveolites and one of Amplexopora from the Devonian Rocks of Northern Queensland, 175.—P. M. Duncan and W. P. Sladen. The Classificatory Position of Hemiaster elongatus, Duncan and Sladen: a Reply to a Criti- cism by Prof. Sven Lovén, 225.—S. H. Scudder. Triassic Insects from the Rocky Mountains, 254.—K. A. Zittel. On Astylospongide and Anomocladina, 271.—R. Etheridge, jun., and A. H. Foord. Descriptions of Paleozoic Corals in the Collections of the British Museum (Nat. Hist.), No. IL, 314.—T. Rupert Jones. Notes on the Palzozoic Bivalved Ento- mostraca, No. XVII. Some North-American Leperditiz and allied Forms, 339.—T. Rupert Jones. Notes on the Paleozoic Bivalved Entomostraca, No. XVIII. Some Species of the Entomidide, 391. ; . Vol. xv. Nos. 85-90. 1885. Purchased. P.M. Duncan. On the Classificatory Position of Hemiaster elongatus, 72. m 2 Ti4 ADDITIONS TO THE LIBRARY. —G. Lindstrém. A Scorpion from the Silurian Formation of Sweden, 76. —F. W. Hutton. The Origin of the Fauna and Flora of New Zealand, — 77.—G. J. Hinde. Description of a new Species of Crinoids with Articu- lating Spines, 157.—T. Rupert Jones. Notes on the Paleozoic Bivalved Entomostraca,No. XIX. On some Carboniferous Species of the Ostracodous Genus Kirkbya, Jones, 174.—C. Brongniart. On the Discovery of an Impression of an Insect in the Silurian Sandstone of Jurques (Calvados), 355.—R. Kidston. On some new or little-known Fossil Lycopods from the Carboniferous Formation, 357.—S. H. Scudder. New Genera and Species of Fossil Cockroaches from the Older American Rocks, 408.— R. Kidston. Notes on some Fossil Plants collected by Mr. R. Dunlop, Airdrie, from the Lanarkshire Coal-field, 473. Art Union of London. Report of the Council for the year 1884. 1884. Atheneum (Journal). Nos. 2957-2983. 1884. ——. Nos. 2984-3007. 1885. ——. Parts 678-684. 1884. ——. Parts 685-689. 1885. Barnsley. Midland Institute of Mining, Civil, and Mechanical Engineers. Transactions. Vol. ix. Parts 72-74. 1884. A. Lupton. Notes on a Visit to some Continental Mines, 287. SS ee Viele batroe aloes: Basel. Société Paleontologique Suisse. Mémoires. Vol.xi. 1884. Purchased. F. Korby. Monographie des polypiers jurassiques de la Suisse, 4° partie. —G. Millard. Monographie des invertébrés du Purbeck du Jura.— H. Haas. Etude monographique et critique des Brachiopodes Rhétiens et Jurassiques des Alpes Vaudoises et des contrées environnantes, 1° partie. Bath. Natural-History and Antiquarian Field Club. Proceedings. Vol.v. No. 4. 1885. Belfast. Natural-History and Philosophical Society. Report and Proceedings for 1883-84. 1884. M. F. Heddle. On Agates, 14. _._, Naturalists’ Field Club. Annual Report and Proceedings, 1883-84. Ser.2. Vol.u. Part 4. 1884. J.S. Gardner. The Age of the Basalts of the North-eastAtlantic, 254. Berlin. Deutsche Geologische Gesellschaft. Zeitschrift. Band xxxvi. Hefte 1-4. 1884. Fr. Pfaff. Zur-Frage der Verinderungen des Meeresspiegels durch den Einfluss des Landes, 1.—A. Grabbe. Beitrage zur Kenntniss der Schild- kyvéten des deutschen Wealden, 17.—G. R. Lepsius. Ueber ein neues Quecksilber-Seismometer und die Erdbeben im J. 1883 bei Darmstadt, 29._S. Nikitin. Diluvium, Alluvium, Eluvium, 37.—E. von Duni- kowski. Geologische Untersuchungen in Russisch-Podolien, 41.—K. =o eee eee —_ ey ee, a : c ADDITIONS TO THE LIBRARY. 115 Tietze. Die Versuche einer Gliederung des unteren Neogen in den dsterreichischen Lindern, 68.—F. Sandberger. Ueber den Bimsstein und Trachyttuff von Schoneberg auf dem Westerwalde, 122.—G. Giirich. Ueber einige Saurier des oberschlesischen Muschelkalkes, 125.—H. Keil- hack. Ueber postglaciale Meeresablagerungen in Island, 145.—H. Eck. Zur Gliederung des Buntsandstein im Odenwald, 161.—A. Jentzsch. Ueber Diatomeen-ftihrende Schichten des westpreussischen Diluviums, 169.—A. G. Nathorst. Ueber cambrische Medusen, 177.E. Beyrich. Erlauterungen zu den Goniatiten L. v. Buch’s, 203.—G. Rammelsberg. Ueber die Gruppen des Skapoliths, Chabasits und Phillipsits, 220.— F. Schmidt. inige Mittheilungen tiber die gevenwirtige anne der elacialen und postglacialen Bildungen im silurischen Gebiet von Ehstland, Oesel und Ingermanland, 248.—V. Uhlig. Ueber die Diluvialbildungen bei Bukowna am Dnjestr, 274.—G. Stache. Ueber die Silurbildungen der Ostalpen mit Bemerkungen tuber die Devon-, Carbon- und Perm- Schichten dieses Gebietes, 277.—K. Dalmer. Ueber das Vorkommen von Culm und Kohlenkalk bei Wildenfels unweit Zwickau in Sachsen, 379.— C. W. von Giimbel. Ueber die Beschaffenheit der Mollusken-Schalen, 385,—J. Felix. Korallen aus agyptischen Tertiarbildungen, 415.—E. Holzapfel. Ueber einige wichtige Mollusken der Aachener Kreide, 454. —A. Wichmann. Ueber Gesteine von Labrador, 485.—E. Koken. Ueber Fisch-Otolithen, insbesondere tiber diejenigen der norddeutschen Oligocin- Ablagerungen, 500.—F. E. Geinitz. Ueber die Fauna des Dobbertiner Lias, 566.—A. Seeck. Beitrag zur Kenntniss der granitischen Diluvial- geschiebe in den Provinzen Ost- und Westpreussen, 584.—G. Vom Rath. Hinige Wahrnehmungen langs der Nord-Pacific-Bahn zwischen Helena, der Hauptstadt Montanas, und den Dalles (Oregon) am Ostabhange des Kaskaden-Gebirges, 629.—A. von Groddeck. Zur Kenutniss der Zinnerz- lagerstatte des Mount Bischoff in Tasmanien, 642.—F, J. P. van Calker. Beitrage zur Kenntniss des Groninger Diluviums, 713.—G. Bohm. Bei- trage zur Kenntniss der grauen Kalk in Venetien, 737.—H. Vater. Die fossilen Holzer der Phosphoritlager des Herzogthums Braunschweig, 783. —F. EH. Geinitz. Ueber ein Graptolithen-fiihrendes Geschiebe mit Cyathaspis yon Rostock, 854.—C. H. Weiss. Ueber den Porphyr mit sogenannter Fluidal-Structur von Thal im Thiiringer Wald, 858.— J.G. Bornemann, sen. Cyclopelta Winteri, eine Bryozoe aus dem Eifeler Mitteldevon, 864.—G. Berendt. Kreide und Tertiir von Finkenwalde bei Stettin, 866.—C. Gottsche. Auffindung cambrischer Schichten in Korea, 875.—K. Dalmer. Ueber den Kohlenkalk von Wildenfels in Sachsen, 876. Berlin. Deutsche Geologische Gesellschaft. Zeitschrift. Band xxxvii. Heft 1. 1885. Branco. Ueber die Anfangskammer von Bactrites, 1—A. Becker. Schmelzversuche mit Pyroxenen und Amphibolen und Bemerkungen tiber Olivinknollen, 10.—F. Frech.. Die Korallenfauna des Oberdevons in Deutschland, 21.—T. Fuchs. Die Versuche einer Gliederung des unteren Neogen im Gebiete des Mittelmeers, 131—M. Verworn. Ueber Patellites antiguas, Schloth, 173.—G. de Geer. Ueber die zweite Aus- breitung des skandinavischen Landeises, 172.—E. Kayser. Lodanella mira, eine unterdevonische Spongie, 207.—E. Koken. Ueber Ornitho- chetrus hilsensis, Koken, 214. Koniglich-Preussische Akademie der Wissenschaften. Sit- zangsberichte, 1884. Nos. 18-54. 1884-85. H. Bucking. Ueber die Lagerungsverhiltnisse der dlteren Schichten in Attika, 985. 116 ADDITIONS TO THE LIBRARY. Berlin. Palsontologische Abhandlungen. Band ii. Hefte 2 & 3.. 1884. Purchased. H. Graf zu Solms-Laubach. Die Coniferenformen des deutschen Kupferschiefers und Zechsteins (Heft 2)—W. Dames. Ueber Archaeo- pteryx (Heft 3). : : Heft 4. 1885. Purchased. F. Notling. Die Fauna der baltischen Cenoman-Geschiebe. Birmingham. Midland Naturalist. N.S. Vol. vii. Nos. 79 & 80. 1884. Presented by Wm. Whitaker, Esq., F.GS. H. Pearce. Ice Action in the Valley of the Artro, 197. Birmingham Philosophical Society. Proceedings. Vol. iv. Part 1 (1883-84). 1884. ; W. Mathews. Modern Geological Problems, 1.—T. Turner. An Analysis of Water from Salt Wells near Dudley, 38.—H. W. Crosskey. Note on Ice-marked Boulders, illustrating the Grooved Blocks of Rowley Hill, 69.—F. W. Martin. The Geological Section along the West Suburban Railway from Birmingham to King’s Norton, 257. Bordeaux. Société Linnéenne. Actes. Vol. xxxvii. (Série 4, Tome vu.). 1883. H. Arnaud. Etudes pratiques sur la craie du sud-ouest: Profils géo- logiques des chemins de fer de Siorac a Sarlat et de Périgueux 4 Ribérac, 34,—K. Benoist. Les Néritacées fossiles des terrains tertiaires moyens du sud-ouest de la France, 379.—E. Benoist. Observations géologiques résultant du forage d’un puits artésien, chez M. Briol, 4 Lestiac, xii.— E. Benoist. Les huitres fossiles des terrains tertiaires moyens de V’ Aquitaine, xvi—E. Benoist. Note sur une couche lacustre observée au Planta, commune de Saint-Morillon, xxii.—H. Benoist. Note sur quelques coupes relevées aux environs de Bergerac, xxxiii.—E. Benoist. Compte- rendu géologique de l’excursion trimestrielle faite & Citon-Cénac, xxxviii. —H. Benoist. Compte-rendu géologique de l’excursion de Fronsac, XXXIx. Boston. American Academy of Arts and Sciences. Proceedings. N28. Voloxa. 1883-34. S. H. Scudder. The fossil White Ants of Colorado, 133. Boston Society of Natural History. Memoirs. _ Vol. iii. Nos. 8, 9, 10. 1884. ele S. H. Scudder. Two new and diverse Types of Carboniferous Myria- pods, 283.—S. H. Scudder. The Species of Mylacris; a Carboniferous Genus of Cockroaches, 299. ——. Proceedings. Vol. xxii. Part 2 (1882-83). 1883. M. E. Wadsworth. The Argillite and Conglomerate of the Boston Basin, 1380.—A. A. Julien. The Dunyte-beds of North Carolina, 141.— T. N. Dale. A Contribution to the Geology of Rhode Island, 179.— M. EH. Wadsworth. Some Instances of Atmospheric Action on Sand- stone, 201. : : Part 3 (1883). 1884. A. Hyatt. Genera of Fossil Cephalopods, 253. ADDITIONS TO THE LIBRARY. EL} Brisbane. Royal Society of Queensland. Proceedings. Vol. i. Part 1. 1884. HK. Palmer. Hot Springs and Mud Eruptions on the Lower Flinders River, 19.—C. W. De Vis. The Moa (Dimornis) in Australia, 23.— J. Falconer. Water Supply: Springs and their Origin, 28,—H. F. Wall- mann. Pseudomorphism in Minerals, 32.—C. W. De Vis. Ceratodus Forstert Post-Pliocene, 40. British Association for the Advancement of Science. Report of the Fifty-fourth Meeting, 1884. Montreal. 1885. T. Rupert Jones. Second Report of the Committee on the Fossil Phyllopoda of the Paleozoic Rocks, 75.—C. E. De Rance. Tenth Report of the Committee appointed for the purpose of investigating the Circulation of Underground Waters in the Permeable Formations of England and Wales, and the Quantity and Character of the Water sup- plied to various Towns and Districts from those Formations, 96.—G. R. Vine. Fifth and last Report of the Committee appointed for the purpose of reporting on Fossil Polyzoa, 97.—Twelfth Report of the Committee appointed for the purpose of recording the Position, Height above the Sea, Lithological Characters, Size, and Origin of the Erratic Blocks of England, Wales, and Ireland, reporting other matters of interest con- nected with the same, and taking measures for their Preservation, 219.— W. Topley. Report upon National Geological Surveys: Part I., Europe, 221.—C. E. De Rance and W. Topley. Report of the Committee appointed for the purpose of inquiring into the Rate of Erosion of the Sea-coasts of England and Wales, and the Influence of the Artificial Abstraction of Shingle or other Material in that Action, 238.—J. W. Davis. Fourth Report of the Committee appointed to assist in the Ex- ploration of the Raygill Fissure in Lothersdale, Yorkshire, 240.—J. Milne. Fourth Report of the Committee appointed for the purpose of investi- gating the HKarthquake Phenomena of Japan, 241.—T. G. Bonney. On the Archean Rocks of Great Britain, 529.—H. 8. Poole. Note on the Internal Temperature of the Earth at Westville, Nova Scotia, 644.— W. T. Blanford. Presidential Address to Section C, Geology, 691.— E. Gilpin, jun. Results of the past Experience in Gold Mining in Nova Scotia, 711.—E. Gilpin, jun. A Comparison of the Distinctive Features of Nova-Scotian Coal-fields, 712—H. A. Budden. On the Coals of Canada, 718.—D. Honeyman. On the Geology of Halifax Harbour, Nova Scotia, 714.—J. H. Panton. Gleanings from Outcrops of Silurian Strata in Red River Valley, Manitoba, 715.—G.C. Brown. The Apatite Deposits of the Province of Quebec, 716.—F. D. Adams. On the Occur- rence of the Norwegian “ Apatitbringer” in Canada, with a few Notes on the Microscopic Characters of some Laurentian Amphibolites, 717.— L. W. Bailey. On the Acadian Basin in American Geology, 717.—E. W. Claypole. Pennsylvania before and after the Elevation of the Appalachian Mountains, 718.—J.S. Newberry. Phases in the Evolution of the North American Continent, 719.—H. C. Lewis. Marginal Kames, 720.—H, Miller. On Fluxion-Structure in Till, 720.—A. R.C. Selwyn. On the Glacial Origin of Lake Basins, 721.—R. Richardson. On Points of Dis- similarity and Resemblance between Acadian and Scottish Glacial Beds, 722.—_W. F. Stanley. On the Improbability of the Theory that former Glacial Periods in the Northern Hemisphere were due to Eccentricity of the Earth’s Orbit and to its Winter Perihelion in the North, 723.—E. Hill. On Ice-Age Theories, 723.—J. 8. Newberry. On the recent Discovery of new and remarkable Fossil Fishes in the Carboniferous and Devonian Rocks of Ohio and Indiana, 724.—J. Hall. On the Fossil Reticulate 118 ADDITIONS TO THE LIBRARY. Sponges constituting the Family Dictyospongide, 725.—J. Hall. On the | Lamellibranchiate Fauna of the Upper Helderberg, Hamilton, Portage, Chemung, and Catskill Groups (equivalent to the Lower, Middle, and Upper Devonian of Europe); with especial reference to the Arrangement of the Monomyaria and the Development and Distribution of the Species of the Genus Leptodesma, 726.—T. Sterry Hunt. The Eozoic Rocks of North America, 727.—J. F. Blake. First Impressions of some Pre- Cambrian Rocks of Canada, 728.—J. D. Dana. On the Southward Ending of a great Synclinal in the Taconic Range, 729.—H. J. Johnston- Lavis. Notice of a Geolegical Map of Monte Somma and Vesuvius, 730.—W. Whitaker. The Value of detailed Geological Maps in relation to Water-supply and other Practical Questions, 731.—V. Ball. On the Mode of Occurrence of Precious Stones and Metals in India, 731.— C. Le Neve Foster. What is a Mineral Vein or Lode? 732.—G. K. Gilbert. Plan for the Subject-Bibliography of North-American Geology, 732.—E. W. Claypole. On some Remains of Fish from the Upper Silurian Rocks of Pennsylvania, 733.—O. C. Marsh. On American Jurassic Mammals, 734.—T: Rupert Jones. On the Geology of South Africa, 736.—Sir W. Dawson. On the more Ancient Land Floras of the Old and New Worlds, 738.—J.S. Gardner. On the Relative Ages of the American and the English Cretaceous and Eocene Series, 739.— E. Wethered. On the Structure of English and American Carboniferous Coals, 741.—A. H. Mackay. A preliminary Examination of the Siliceous Organic Remains in the Lacustrine Deposits of the Province of Nova Scotia, Canada, 742.—G. F. Matthew. The Geological Age of the Acadian Fauna, 742.—G. F. Matthew. The Primitive Conocoryphean, 743.—P. Hallett. Notes on Niagara, 744—O.C. Marsh. On the Classi- fication and Affinities of Dinosaurian Reptiles, 763. Brussels. Musée Royal d'Histoire Naturelle de Belgique. Bulletin. Tome ii. (1884). Nos. 2-4. 1884. A. Renard. Notice sur la composition minéralogique de Varkose de Haybes, 117.—L. Dollo. Cinquiéme Note sur les Dinosauriens de Ber- nissart, 129.—L. Dollo. Premiére Note sur le Simcedosaurien d’Erque- linnes, 151.—A. Renard. Recherches sur la composition et la structure des phyllades ardennais, 231.—J. Purves. Esquisse géologique de Vile de Antigoa, 273. —. Société Royale des Sciences de Liége. Mémoires. Supplé-- ment au Tome x. 1883. (4to.) Buckhurst Hill, Essex Field Club. Transactions. Vol.ii. Part8. 1884. N. F. Robarts. Notes on the London Clay and Bagshot Beds at “Oakhill” Quarry, Epping Forest, 231. Budapest. Magyar Foldtani Tarsulat [Geological Society]. Fold- tani Kézlony. Kotet 4 (1874). 1874. F. Posepny. Geologisch-montanische Studie der Erzlagerstatten von Rézbanya in 8.0.-Ungarn, 1. - Kotet 9 (1879). 1879. J. Bockh. Szérénymegye déli részére vonatkoz6 geologiai jegyzetek, 1. —L. Maderspach. Uj czinkércz fekhely Gomorben, 31.—J. Matyasovszky. A Glenodictyum egy uj lelhelye Erdélyben, 32.—J. Bockh. Auf den sud- lichen Theil des Comit. Szorény beziigliche geologische Notizen, 65.—L. ADDITIONS TO THD LIBRARY. 119 Roth. A rakos-ruszti hegyvonulat és a Lajtahegyseg déli részének geolo- giai vazlata, 99.—J. Stiirzenbaum. Mosonymegyében eszkézélt geologiai folvétel 1878 ban, 111.—M. Staub. Carya costata (Sternb.) Unger, a magyarhoni fossil floréban, 115.—B. Winkler. Urvélgyit, egy uj rézasvany Urvolgyrél, 121—A. Péch. Az Urvéleyén tortént ujabb feltarasokrol, 125.—S. Schmidt. Kristélyos Tetraédrit Rozsnyérél, 127.—L. v. Roth. Geologische Skizze des Kroisbach-Ruster Bergzuges und des siidlichen Theiles des Leita-Gebirges, 189,—J. Stiirzenbaum. Geologische Aufnahme im Comitate Wieselburg im Jahre 1878, 150.—M. Staub. Carya costata (Stbg.) Unger, in der ungarischen fossilen Flora, 155.—B. v. Winkler. Urvolgyit, em neues Kupfermineral von Herrengrund, 156.—L. Mader- spach. ine neue Zinkerz-Lagerstitte im Gomorer Comitate, 159.—J. v. Matyasovszky. Ein neuer Fundort des Glenodictyum in Siebenbirgen, 160,—A. Péch. Neuere Ausrichtungen in dem Bergbaue von Herren- gerund, 162.—A. Schmidt. Krystallisirter Tetraédrit von Rosenau, 164.— K. Hofmann. Jelentés az 1878 nyaraén Szilagymegye Keleti részében tett foldtani részletes felvételekrol, 167.—J. Stiirzenbaum. Az ard6i ezinkérez-fekhely geologiai viszonyair6l, 213.—J. Stiirzenbaum. A dernoi kdsseni rétegekrol, 217.—K. Hofmann. Bericht iiber die im dstlichen Theil des Szilaeyer Comitates wihrend der Sommercampagne 1878 voll- fiihrten geologischen Specialaufnahmen, 231.—J. Stiirzenbaum. Ueber die geologischen Verhaltnisse der Zinkerz-Lagerstitte bei Pelsécz-Ard6 im Gomo6rer Comitat, 283.—J. Stiirzenbaum. Kossener Schichten bei Derno im Tornaer Comitate, 287.—J. Matyasovszky. Jelentés az 1878 évben Szilagymegyében eszk6zélt féldtani felvételrol, 293.—J. Szabé. A Num- mulitképlet viszonya a Trachythoz Vihnyen Selmecz mellett, 301.—L. Roth. Adatok az Alfold altalajanak ismeretéhez, 312.—T. Posevitz. Szorény megyei eruptiv koézetek, 317.—J. v. Matyasovszky. Bericht iiber geologische Detailaufnahmen im Comitate Szilaigy im Jahre 1878, 332.—L. vy. Roth. Daten zur Kenntniss des Untergrundes im Alfold, 341.—T. Posewitz. Ueber Eruptivgesteine vom Comitate Szérény, 347. —V. Legeza. Granat von Uj-Kemencze, 364.—B. Inkey. A boiczai éreztelérek mellekkézetérol, 364.—H. Stern. Nehdny szérénymegyei k6zet petrographiai meghatarozdsa, 376.—G. Primics. A Hargita éjszaki nyulvanyanak, nevezetesen Beszterczevoleye, Tihavolgye, Henyul és Sztrimba eruptiv kozeteinek petrographiai vizsgalata, 382.—F. Scha- farzik. Diabas Dobojrél Boszniéban, 393.—J. Bernath. Magyarhon dsvanyvizi terképe, 399.—F. Schafarzik. Szilard és folyekony zarvanyok asvanyokban es Koézetekben, 401.—K. Hofmann. Megjegyzések trachy- - tanyagnak a hazai 6-harmadkori lerakédasokban val6 eldfordulasara, 406. —B. v. Inkey. Ueber das Nebengestein der Erzginge von Boicza in Siebenbtirgen, 425.—H. Stern. Petrographische Bestimmung einiger Gesteine aus dem Comitate Szérény, 433.—F. Schafarzik. Diabas von Doboj in Bosnien, 439.—J. Szab6. Das Verhaltniss der Nummulitforma- tion zum Trachyt bei Vichnye (Hisenbach) nichst Schemnitz, 442.— G. Primics. Petrographische Untersuchung der eruptiven Gesteine des nordlichen Hargitazuges, insbesondere des Bistritz und Tihathales, des Henyul und Sztrimba, 455.—J. Bernath. Mineralquellenkarte Ungarns, 467.—F. Schafarzik. Feste und fliissige Einschliisse in Mineralien und Gesteinen, 469.—K. Hofmann. Bemerkungen tiber das Auftreten tra- chytischen Materials in den ungarisch-siebenbiirgischen alttertiaren Abla- gerungen, 474. Budapest. Magyar Foldtani Tarsulat [Geological Society]. Fold- tani Kozlony. Kotet 10 (1880). 1881. J. Matyasovszky. Arvizlecsapolasi kisérlet egyelnyel6 artézi knit altal, 1.—T. Fuchs. A fdldségel szabalyos alakjarol, 7—J. Szabd. Calcit- I20 ADDITIONS TO THE LIBRARY. pseudomorphose Mihalytarnab6l Selmeczen, 12—B.Inkey. Egy feltuné vonas Nagyag vidékének domborzataban, 16.—J. v. Matyasovszky. Ein Entwasserungsversuch mittelst negativer Brunnen, 19.—T. Fuchs. Ueber die regelmassige Gestalt der Continente, 28.—J. Szab6. Ueber Calcit- Pseudomorphosen aus dem Michaeli-Stollen in Schemnitz, 32.—B. v. Inkey. Ueber eine auffallende Bergform in der Umgebung von Nagyag, 37.— M. Hantken. A buda-vidéki 6-harmadkori képzédmények, 41.—F. Scha- farzik. A fodldrengések Del-Magyarorszigon és a szomszédos teruleteken 1879 Oktéber 10-ét6l 1880 marczius lig, 53.—A. Franzenau. Egy uj lelhelyu kél Asvanyrél,76.—M. Hantken. Die alttertiéren Bildungen der Umgegend von Ofen, 78.—F. Schafarzik. Das Erdbeben in Sud-Ungarn und den angrenzenden Landern, 10 October 1879-13 April 1880, 91.— A. Franzenau. Ueber zwei Mineralien eines neuen Fundortes, 119.— L. Roth. Adatok az Alfold altalajanak ismeretéhez, 121.—G. Halavats. Adatok Szorénymegye foldtani viszonyaihoz, 131.—A. Koch. A Czibles és Olahlaposbanya vidéke zoldkoandesitjeinek Uj petrographiai vizsgalata, 138.—L. y. Roth. Daten zur Kenntniss des Untergrundes im Alfold, 147. —J. Halavats. Zur geologischen Kenntniss des Szorényer Comitates, 158. —A. Koch. Petrographische Untersuchung der trachytischen Gesteine des Czibles und von Olahlaposbanya, 165A. Koch. Rodna vidéke trachyt-csaladhoz tartoz6 kozeteinek uj petrographiai vizsgalata, 177.— H. Stern. Szdrénymegyei eruptiv kézetekrol, 187.—J. Bernath. Erdély konyhas6-vizei, 200.—L. Nagy. Adatok a dobsinai Dioritrol, 217.—A. Koch. Neue petrographische Untersuchung der trachytischen Gesteine der Gegend von Rodna, 219.—H. Stern. Eruptivgesteine aus dem Comitate Szérény, 230.—J. Bernath. Die Kochsalzwisser in Sieben- biirgen, 244.—K. Hofmann. Buda vidékének némely 6-harmadkori képzodéserol, 245.—G. Halayats. A golubaczi (Szerbia) mediterran fauna, 293.—F. Schafarzik. A “Cserhat” D Nyi végének eruptiv- kozetei, 295.—K. Hofmann. Ueber einige alttertiire Bildungen der Umgebung yon Ofen, 319.—J. Halavats. Die mediterrane Fauna von Golubatz in Serbien, 374.—F. Schafarzik. Die eruptiven Gesteine der siidwestlichen Auslaufer des Cserhat-Gebietes (N.N.O. von Budapest), 377.—L. Nagy. Daten tiber den Diorit von Dobschau, 403. Budapest. Magyar Foldtani Tarsuiat [Geological Society]. Fold- tani Kozlony. Kotet 11 (1881). 1881. G. Halavats. A magyarhoni mediterran rétegekben eldfordulé conu- sokrol, 1.—M. Staub. Adalék a Szekelyfold fossil florajahoz, 6.—L. Roth. Adalék a szekelyfoldi neogen édesvizi lerakédasok faunajanak ismeretéhez, 13.—B. Inkey. A zagrabi 1880 évi foldrengés forgatasi tiinemenyeirdl, 24,—A. Franzenau. Adatoka rékosi (Budapest) felso mediterran emelet foraminifera faunajahoz, 31.—J. Halavats. Ueber die Verbreitung der in den Mediterran-Schichten von Ungarn vorkommenden Conus-Formen, 56.—M. Staub. Beitrage zur fossilen Flora des Szeklerlandes, 58.— B. vy. Inkey. Ueber Drehungserscheinungen beim Erdbeben von Agram 1880, 76.—A. Franzenau. Beitrage zur Foraminifera~Fauna der Rakoser (Budapest) Ober-Mediterran Stufe, 83—J. Budai. Adatok a Hargita déli reszenek petrographidjahoz, 109—S. Roth. A Jekelfalviés Dobsinai diallag-serpentin leirdsa, 120.—A. Steiner. A karpati homokk6 kulénbéz6 szinének okairél, 124.—G. Halavats. A Lokva hegyseg foldtani viszonyai, 132.—J. Bernath. Egy balatonparti foldsiilyedesrol, 137.—G. Guckler. A Varallyén eléfordulé asvanyvizekrol, 140.—S. Roth. Der Jekelsdorfer und Dobschauer Diallag-Serpentin, 142.—A. Steiner. Ueber die Ursachen der verschiedenen Farbe des Karpathen Sandsteines, 146.—V. Guckler. Daten zu den Varallyaer Mineralquellen, 154.—L. Locezy. Utazasi jegy- zetek Javar6l, 161.—B.Inkey. Uti jegyzetek az erdélyi déli hatarhegy- ADDITIONS TO THE LIBRARY. I21 séobél, 172. —A. L. Cserey. Az Aplit elegyrészeinek vegyelemzése, 176.—G. Primics. Adatok Bosznia Koézettani ismeretéhez, 184.—B. v. Inkey. Reisenotizen aus dem siidlichen Grenzgebirge von Siebenbiirgen, 190.—G. Primics. Zur petrographischen Kenntniss yon Bosnien, 195.— J. Halayats. Die geologischen Verhiiltnisse des Lokva-Gebirges, 200.— I. Bernath. Ueber eine Bodensenkung am Ufer des Plattensees, 205.— J. Szabé. Hefie S10 (1883). 1884. M. Staub. Tertiare Pflanzen von Felek bei Klausenburg, 263.—G. Primics. Die geologischen Verhiltnisse der Fogarascher Alpen und des benachbarten rumanischen Gebirges, 283.—T, Posewitz. Geologische Mittheilungen tber Borneo, 317. ee : : : Band vii. Hefte 1-4. 1884-85. J. Felix. Die Holzopale Ungarns in palaeophytologischer Hinsicht, 1. —A. Koch. Die alttertiaren Echiniden Siebenbiirgens, 45.—M. Groller von Mildensee. Topografisch-geologische Skizze der Inselgruppe Pelagosa im adriatischen Meer, 131.—T. Posewitz. Die Zinninseln im indischen Oceane: I. Geologie von Bangka. Als Anhang: Das Diamant-Vorkom- men in Borneo, 153. : : . Jahresbericht fiir 1883. 1884. J. Bockh. Directions-Bericht, 3—C. Hofmann. Ueber die auf der rechten Seite der Donau zwischen O-Szény und Piszke ausgeftihrten geologischen Specialaufnahmen, 19.—J.von Matyasovszky. Der Kiraly- hagé und das Thal des Sebes-Korés Flusses yon Buesa bis Réy, 38.— L. von Léezy. Bericht tber die geologische Detailaufnahme wahrend des Sommers 1883, im Gebirge zwischen der Maros und der Weissen- K6rés und in der Arad-Hegyalja, 45—A. Koch. Bericht iiber die im Klausenburger Randgebirge ausgefiihrte Specialaufnahme, 64.—L. Roth. Das Gebirge noérdlich von Pattas-Bozovics im Krassé-Szérényer Comitate, 87.—J. Halavats. Bericht ter die geologische Detailaufnahme im Jahr 1883 in der Umgebung von Alibunar, Moravicza, Moriczfold und Kakova, 99.—F. Schafarzik. Geologische Aufnahme des Pilis-Gebirges und der beiden “ Wachtberge” bei Gran, 105.—A. Gesell. Bericht tiber die montangeologische Detailaufnahme von Schemnitz und Umgebung in den Jahren 1882-83, 132. g . Konyy- és Térképtdranak Czimjegyzéke’ [Catalogue of the Library]. (8vo.) 1884. Buenos Aires. Academia Nacional de Ciencias en Cordoba. Boletin. Tomovi. Entregas 2-4. 1884. F. Ameghino. Escursiones Geoldgicas y Paleontologicas en la provincia de Buenos Aires, 161. ; . Tomo vii. Entregas 1-4. 1885. H. Conwentz. Sobre algunos Arboles fésiles del Rio Negro, 435.— F. Ameghino. Oracanthus Burmeistert, nuevo edentado extinguido de la Republica Argentina, 499. ; ; Tomo vii. Entregal. 1885. F,. Ameghino. Nuevos restos de mamiferos fosiles oligocenos recogidos por el profesor Pedro Scalabrini, y pertenecientes al Museo Provincial del Parana, 5. ——. Sociedad Cientifica Argentina. Anales, 1884. Tomo xvii. Entregas 5 & 6. 1884. eS Se er ADDITIONS TO THE LIBRARY. 125 Buenos Aires. Sociedad Cientifica Argentina. Anales, 1884. Tomo xviii. Entregas 1-6. 1884. A. Déring. Informe sobre un sedimento lacustre fosilifero, encontrado en la perforacion del Desaguadero (Ferro-Carril Andino), 1—G. Avé- Lallemant. Datos mineros de la republica oriental, 193. , 1885. Tomo xix. Entregas1 & 2. 1885. ——_—_—_- — . . Caen. Société Linnéenne de Normandie. Bulletin. Série3. Vol. vii. (1882-83). i883. C. Renault. Etude stratigraphique du Cambrien et du Silurien dans les vallées de l’Orne et de la Laige, 16, 88.—A. Bigot. Note sur la base du Silurien moyen dans la Hague, 31.—J. Moriére. Note sur une Ery- onidée nouvelle trouvée a la Caine (Calvados) dans le Lias supérieur, 116. —C. Renault. Note sur le Lias de la prairie de Caen, 130.—L. Lecornu. Sur la composition de certains sables et de certains alluvions, 134.— H.E.Sauvage. Note sur le genre Pachycormus, 144.—J. Moriére. Note sur une empreinte de corps organisé offerte par le grés armoricain de May (Calvados), 150.—C. Renault. Le Cambrien et le Silurien de la vallée de ’Orne (d’Etavaux 4 Feugerolles), 261.—A. Bigot. Compte- rendu de l’excursion géologique 4 May-sur-Orne, 303. Calcutta. Asiatic Society of Bengal. Journal. Vol. lii. Part 2. Title-page, Plates, &c., 1883. 1885. —-. Vol. lii. Partl. No.3. 1884. —_. 1-——. ——. —. Part2. Nos.1 &2. 1884. —. ——. —. —. ——. Special Number. 1884. ; Proceedings, 1884. Nos. 3-11. 1884-85. R.D. Oldham. Rough Notes for the construction of a Chapter on the History of the Earth, 145. Cambridge Philosophical Society. Proceedings. Vol. v. Parts 1-3. 1884-85. T. G. Bonney. On the Micgoscopic Structure of a Boulder from the Cambridge Greensand found at Ashwell, Herts, 65——EH. Hill. On a Continuous Succession in part of the Guernsey Gneiss, 154. —_=, “Pransactions: Vol. xiv. Pariil. . 1885. Cambridge, Mass. Museum of Comparative Zoology at Harvard College. Bulletin. Vol. vu. (Geological Series, Vol. i.). Nos. 2-8. 1881. J.S. Diller. The Felsites and their Associated Rocks North of Boston, 165.—M. E. Wadsworth. On an Occurrence of Gold in Maine, 181.— M. E. Wadsworth. A Microscopical Study of the Iron Ore, or Peridotite, of Iron Mine Hill, Cumberland, Rhode Island, 183.—C. E. Hamlin. Observations upon the Physical Geography and Geology of Mount Ktaadin and the adjacent district, 189.—L. Lesquereux. Report on the Recent Additions of Fossil Plants, 225.—J. E. Wolff. The Great Dike at Hough’s Neck, Quincy, Mass., 231.—L. Lesquereux. On some Spe- cimens of Permian Fossil Plants from Colorado, 248. 126 ADDITIONS TO THE LIBRARY. Cambridge, Mass. Museum of Comparative Zoology at Harvard College. Bulletin. Vol. vii. (Geological Series, vol. i.). No. 11. 18845 2% J. Whitney and M. E. Wadsworth. The Azoic System and its pro- posed Subdivisions, 331. ee Vola “No AOS Biss ey es Memairs sew Ol yi NO aes = Voli Nod. - 1652 M. E. Wadsworth. Lithological Studies. A Description and Classifi- cation of the Rocks of the Cordilleras, iF —. «——. —~. —. No.3. 1884. Volk-x, Ne: 3.41684. C.E. Hamlin. Results of an Examination of Syrian Molluscan Fossils, chiefly from the range of Mount Lebanon, 1 Vols. xii. & xii. 1884. ——, Science. Nos. 73-92, 95-99: 1884. eS oe eo —_ e -_t _-_, Cape Town. South-African Philosophical Society. Transactions. Vol. m1. (1881-83). 1884. A.H. Green. [Notes of a Lecture on South African Geology, | 27. Carlisle (Keswick). Cumberland Association for the Advancement of Literature and Science. Transactions. Part 1 (1875-76). 1876. . J.C. Ward. Sketch of the Geological History of the Lake District, 59. ——_,, ——. Part 2 (1876-77). 1877. R. Russell and T. V. Holmes. The Raised Beach on the Cumberland Coast between Whitehaven and Bowness, 68.—J.C. Ward. Remarkable Boulders of Keswick District, 71. ‘ 3 Part 3 (1877-78). 1878. Sir G. Airy. On the probable Condition of the Interior of the Earth, 43. —J.C. Ward. Quartz, as it occurs in the Lake District, its Structure ‘and its History, 77.—C. Smith. Boulder Clay, 91.—R. Pickering. Submerged Forest at St. Bees, 109. pid! sees Paa asTeL7Oy LBP: —. ‘ Part 5 (1879-80). 1886. JAD. Kendall. The Influence of Geological Structure on Scenery, 97. —J.D. Kendall. Distribution of Boulders in West Cumberland, 151. : Part 6 (1880-81). 1881. T. V. Holmes. On asubmerged Forest off Cardurnock, on the Solway ; and on the Destruction of Skinburness by the Sea about the year 1305, 121.—T. V. Holmes. Notes on the Physical Geographyof North-west Cumberland, 167. ——e e ADDITIONS TO THE LIBRARY. 127 Carlisle. Cumberland and Westmoreland Association. Transac- tions. No. 9 (1883-84), 1885. J.G. Goodchild. The Penrith Sandstone, 31.—T. V. Holmes. Notes on the best Locality for Coal beneath the Permian Rocks of North-west Cumberland, 109.--Miss Donald. Notes on some Carboniferous Gaste- ropoda from Penton and elsewhere, 127.—J. Leitch. Notes on the Geo- logical Formation and Fossils of the Silloth new Dock, 169.—J. G. Good- child. Contributions towards a List of the Minerals occurring in Cumber-- land and Westmoreland (concluding part), 175. Cassel. Paleontographica. Band xxxi. (Folge 8, Band vii.). Lief. 1 & 2. 1884. Purchased. C. Hasse. Einige seltene palaontologische Funde, 1.—M. Kliver. Ueber Arthropleura armata, Jord., 11.—M. Schlosser. Die Nager des europii- schen Tertiirs nebst Betrachtungen uber die Organisation und die ge- schichtliche Entwicklung der Nager tiberhaupt, 19.—A. Schenk. Die wihrend der Reise des Grafen Bela Széchenyi in China gesammelten fossilen Pflanzen, 163. a, : Lief. 3-6. 1885. Purchased. L. von Graff. Ueber einige Deformitaten an fossilen Crinoiden, 183. —A. Bohm und J. Lorié. Die Fauna des Kelheimer Diceras-Kalkes. Dritter Abtheilung: Echinoideen, 193.—Hosius und Von der Marck. Weitere Beitriige zur Kenntniss der fossilen Pflanzen und Fische aus der Kreide Westfalens, 225.—Von der Marck. Fische von der oberen Kreide | Westfalens, 233.—Riust. Beitrage zur Kenntniss der fossilen Radio- larien aus Gesteinen des Jura, 271.—M. Schlosser. Nachtrige und Berichtigungen zu: die Nager des europaischen Tertiars, 323.—A. von Konen. Nekrolog tiber Professor Wilhelm Dunker, 331. ——. ——. Supplement 2. Abth. 5. (Text, 8vo; Atlas, fol.) 1884. Purchased. G. Cotteau. Die Echinideti der Stramberger Schichten, 1. Catania. Accademia Gioenia di Scienze Naturali. Atti. Serie 3. Tomo xvil. 1883. L. Ricciardi. Sulla composizione chimica de’ diversi strati di una stessa corrente di lava eruttata dall’ Etna nel 1669, 17.—L. Ricciardi. Le rocce cristalline dei dintorni di Messina, 37.—L. Ricciardi. Sulla diffusione del Vanadio nel regno minerale e vegetale, 161.—O. Silvestri. Sopra un particulare specie di quarzite semivetrosa, a struttura pomiceo- eranulare contenuta nell’ interno di alcune bombe projettate dall’ Htna nella recente eruzione eccentrica del 22 Marzo 1883, 167.—L. Ricciardi. L’ Etna e I eruzione del mese di Marzo 1883, 195.—L. Ricciardi. Sulla composizione chimica dei basalti di Cattolica e Tremiglia e di una breccia basaltica, 231.—O. Silvestri. Sulla esplosione Etnea del 22 Marzo 1883 in relazione ai fenomeni vulcanici (geodinamici et eruttivi) presentati dall’ Etna durante il quadriennio compreso dal Gennaio 1880 al Dicembre 1883, 235. Chemical News. Nos. 1283-1309. 1884. Nos. 1310-1334. 1885. Chemical Society. Abstracts of the Proceedings. Nos. 1-9 (1884-85). 1885. VOL. XII. n 128 ADDITIONS TO THE LIBRARY. Chemical Society. Journal. Nos. 260-265. 1884. —. ——. Supplementary number, 1884 (Title-pages, Indexes, &e.). —. —. Nos. 266-721. 1885. Colliery Guardian. Nos. 1226-1252. 1884. —. Nos. 1253-1277. 1885. Copenhagen. Kongelige Danske Videnskabernes Selskab. Natur- videnskabelige og Mathematiske Afhandlinger. Rekke 6. Bindi. Nos. 6, 9,10. 1884. Se ES es) CE SE NO nse ay Se ee Bid i) Nom aeeoeas ——. ——. Oversigt, 1883. No.3. 1884. Aol Sage ceil , 1884. Nos. 1-3. 1884-85. ib Si inert bil eae res liNig: 11s URS oR: Cracow. Akademija Umiejetnosci w Krakowie. Sprawozdanie. Komisyi Fizyjograficznéj. Tom xviii. 1884. W. Teisseyre. Obudowie geologicznéj okolicy Tarnopola i Zharaza, Czesé I., 216.—A. Altha. Sprawozdanie z podrézy w r. 1883 odbyté} po *wechodnigj Galicyi, 239. Crystallological Society. Proceedings. Part 1 (1877). 1877. A. Des Cloizeaux. Memoir on the three Types of Humite, 6.—W. C. Broeger and G. Vom Rath. On certain large Crystals of Enstatite found by W. C. Brogger and H. H. Reusch, 14—F. Field. On Ludlamite, a new Cornish Mineral, 23.—W. J. Lewis. Notice of Crystallographical Forms of Glaucodote, 31.—E. Bertrand. Note on the Law of Twinning and Hemihedrism of Leucophane, 35.—W. J. Lewis. Crystallographic Notes, 37. —. ——. Part 2 (1882). 1882. W. J. Lewis. Crystallographic Notes, 49.—N. S. Maskelyne. On an Artificial Diopside Rock formed in a Bessemer Converter, 59.—N. S. Maskelyne. Enstatite Rock from South Africa, 60.—W. Flight. Exa- mination of two new Amalgams and a Specimen of Native Gold, 84.— L. Fletcher. Crystallographic Notes, 85.—W. G. Lettsom. On ‘Rhab- dophane, a new Mineral, 105.—W. G. Lettsom. On the Dichroism of two European Andalusites, 108.—W. J. Lewis. Crystallographic Notes, 108.—L. Fletcher. Crystallographic Notes, 114. - -Dorpat. Naturforscher-Gesellschaft. Archiv fir die Naturkunde Liv-, Ehst- und Kurlands. Serie2. Biologische Naturkunde. Band x. Lief. 1. 1884. ——. ——. Schriften I. 1884. (8vo.) Dorpat, 1834. ADDITIONS TO THE LIBRARY. 129 5 Dorpat. Naturforscher-Gesellschaft. Sitzungsberichte. Band vii. Heft 1 (1884). 1885. J. Siemiradzki. Geologische Verhialtnisse von Martinique, 54.—C. Gre- wingk, Ueber einige neue Funde subfossiler Wirbelthierreste unserer Provinzen, 143.—J. Siemiradzki. Beitrag zur Kenntniss unserer Torf- moore, 174. Dresden. Naturwissenschaftliche Gesellschaft Isis. Sitzungs- berichte und Abhandlungen. Jahrgang 1884, Jan.—Juni. 1884. Sitzungsberichte. C. Kénig. Ueber Moor und Torf, 21.—A. Purgold, Zirkon-Zwilling von Renfrew, Canada, und Pyrit aus Cornwall, 25. ee on necomber. L885. Sitzungsberichte. A. Purgold. Ueber die mineralogischen und geologischen Ergebnisse einer Reise in Italien, 58. Abhandlungen. E. Danzig. Ueber das archaische Gebiet nordlich vom Zittauer und Jeschken—Gebirge, 141. Dublin. Royal Irish Academy. Proceedings. Ser. 2. Vol. ii. No. 5. Polite Literature and Antiquities. 1884. —. ——. —. ——. Vol. iv. Nos. 1 & 2. Science. 1884. J. P. O’Reilly. On the Directions of Main-lines of Jointing observable in the Rocks about Dublin, and ‘tir Relations with existing Coast-lines and with lines of Faulting and Contact of Geological Formations, Part IL., 116. ——, ——. Transactions. Vol. xxviii. Science. Parts 14-16. 1883-84. Dudley and Midland Geological and Scientific Society and Field Club. Proceedings. Vol. iii. No. 3. 1877. Presented by W. Whitaker, Esq., F.GS. J. W. Oliver. Railway Cutting at Daw End, near Walsall, 111.— E. Terry. Section of Wenlock Shale from the Wren’s Nest, Dudley, 113. —W. J. Harrison. On the Rhetic Section at Dunhampstead Cutting, near Droitwich, and its correlation with the same strata elsewhere, 115.— J.H. Thomson. On Salt, 127.—C. Cochrane. Ink Photograph of the Fossil tosaurus ferratus, Fraas, 180.—W. Molyneux. The Bunter Conglomerates of Cannock Chase, 139. Dulwich College Science Society. Sixth Annual Report, 1883-84. 1884. R. G. Reid. Volcanoes, 16.—C. O. Blagden. Amber, 20.—T. Rose. Crystallography, 24.—A. Tribe. The Salt-mines of Stassfurt, 26.— A. R. Saunders. Geology, 34.—S. W. Carruthers. Australia, 38.— W. Carrithers. Coal, and the Plants which form it, 39.—A. Tribe. The Chemistry of Coal, 41. ; n 130 ADDITIONS TO THE LIBRARY, Dundee. East of Scotland Union of Naturalists’ Societies. Reports, 1884. 1885. J. Durham and W. N. Walker. Report on Geology, 73.—W. W. Peyton. Report on Mineralogy, 78. East-India Association. Journal. Vol.xvi. Nos. 46. 1884. =», Vol. xvii. Nos. 1-4.) 1885: Easton. American Institute of Mining Engineers. Transactions. Index, Vols. i.-x. 1884. Edinburgh. Royal Physical Society. Proceedings. Session 1883-84. 1884. A. Geikie. Opening Address, 1.—R. H. Traquair. Remarks on the Genus Megalichthys (Agassiz), with Description of a new Species, 67.— R. H. Traquair. Notes on the Genus Gyracanthus (Agassiz), 91.—J. T. Richards. On Scottish Fossil Cycadaceous Leaves contained in the Hugh Miller Collection, 116.—R. Kidston. On a specimen of Pecopteris (? polymorpha, Brongn.) in Circinate Vernation, with Remarks on the Genera Spiropteris and Rhizomopterts of Schimper, 123.—R. Kidston. On a new Species of Schutzia from the Calciferous Sandstones of Scot- land, 127.—H. Gunn. On the Silver Districts of Colorado (Leadville and San Juan), 155.—H. Miller. On Boulder-Glaciation, 156.—J. 8. G. ‘Wilson and H. M. Cadell. The Breadalbane Mines, 189.—H. M. Cadell. The Harz Mountains, their Geological Structure and History, 207. Royal Society. Proceedings. Vol. xi. No.110. 1881-82. R. Christison. On the Application of the Rocks of Ben Nevis to Ornamental Art, 365.—Duns. The Surface-Geology of Mid-Lochaber, 483. —M.F. Heddle. Chapters on the Mineralogy of Scotland, Chapter VIL., 549.—A. Geikie. Note on the Carboniferous Rocks of the South of Scotland, 598.—R. Kidston. Report on the Fossil Plants collected by the Geclogical Survey of Scotland in Eskdale and Liddesdale, 603.—J. J. Dobbie and G. G. Henderson. On the Formation of Serpentine from Dolomite, 606.—M. F. Heddle. Geological Notes, 630.—T. H. Tizard and J. Murray. Exploration of the Faroe Channel during the Summer of 1880, in H.M.’s hired ship ‘Knight Errant,’ 638—D. Milne-Holme. Report of the Boulder-Committee, with Remarks, 743. : : . Wokvxat, “Nov i3.-"4883: D. Milne-Holme. Ninth Report of the Boulder-Committee, 193. ——. ——. Transactions. Vol. xxx. Parts 2 & 3. 1881-82 & 1882-83. M. F. Heddle. Chapters on the Mineralogy of Scotland, Chapter VII, 427 —B.N. Peach. Further Researches among the Crustacea and Arach- nida of the Carboniferous Rocks of the Scottish Border, 511.—R. Kidston. Report on Fossil Plants collected by the Geological Survey of Scotland in Eskdale and Liddesdale, 531. —. ——. ——. Vol. xxxii. Partl. 1882-83. Falmouth. Royal Cornwall Polytechnic Society. Fifty-first Annual Report, 1883. 1884. E. A. Wiinsch. On the Genesis of Slate Rocks, and on the Theory of Vulcanicity, 51. ADDITIONS TO THE LIBRARY. 13a Frankfort-on-the-Maine. Senckenbergische Naturforschende Gesell- schaft. Bericht, 1884. 1884. F. Kinkelin. Ueber zwei siidamerikanische diluviale Riesenthiere, 156. —F. Kinkelin. Ueber Fossilien aus Braunkohlen der Umgebung von Frankfurt-a-M., 165.—F. Kinkelin. Sande und Sandsteine im Mainzer Tertiarbecken, 183.—F. Kinkelin. Die Schleusenkammer von Frankfurt- Niederrand und ihre Fauna, 219.—O. Bottger. Fossile Binneuschnecken aus den intermiocainen Corbicula-Thonen von Niederrand bei Frankfurt- a-M., 258.—F. Ritter. Ueber neue Mineralfunde im Taunus, 320. Geneva. Société de Physique et d’Histoire Naturelle. Mémoires. Tome xxviii. Partie 2. 1884. Geological Magazine. Dec. ILI. Vol.i. Nos. 7-12. 1884. J. W. Dawson. Notes on the Geology of the Nile Valley, 289.—W. H. Hudleston. Contributions to the Paleontology of the Yorkshire Oolites, 293.—E. W. Claypole. On the Occurrence of the Genus Dalmanites in the Lower Carboniferous Rocks of Ohio, 803.—S. Spence Bate. Arche- astacus (Eryon) Willemesx, anew Genus and Species of Eryonide, 307. —C.Ochsenius. Metalliferous Deposits, 310.—W. T. Blanford. On the Classification of Sedimentary Strata, 318—A. Irving. The Permian- Trias Question, 321.—H. Woodward. On the Wing of a Neuropterous Insect from the Cretaceous Limestone of Flinders River, North Queens- land, Australia, 337.—W.H. Hudleston. Notes on some Mollusca from South Australia, obtained near Mount Hamilton and the Peak Station, 539.—H. Woodward. Note on the Remains of Trilobites from South Australia, 342.—O, C. Marsh. Principal Characters of American Creta- ceous Pterodactyls: Part I. The Skull of Pteranodon, 345.—T. R. Jones. Gn some Paleozoic Phyllopoda, 348.—T. R. Jones and J. W. Kirkby. On some Carboniferous Entorfestraca from Nova Scotia, 356.—C. Calla- way. On a new Metamorphic Area in Shropshire, 362.—J. F’. Blake. Criticisms on recent Papers about Faults, 366.—J. W. Dawson. Notes on the Geology of Egypt, 385, 459.—T. R. Jones and H. Woodward. Notes on Phyllopodiform Crustaceans, referable to the Genus Echinocaris, from the Paleeozoic Rocks, 393.—O. Fisher. On Cleavage and Distortion, Part V., 396.—T. G. Bonney. Remarks on Serpentine, 406.—R. D. Oldham. Note on a Graphic Table of Dips, 412.—E. Wilson and H. E. Quilter. The Rhetic Section at Wigston, Leicestershire, 415.—W. Davies. Notes on some new Carnivores from the British Eocene Forma- tions, 433.—R. Lydekker. Notes on some Fossil Carnivora and Rodentia, 442.—T. M. Reade. On a Section of Keuper Marls at Great Crosby, 445. —W.Topley. Report upon the National Geological Surveys of Europe, 447.—K. W. Claypole. Pennsylvania before and after the Elevation of the Appalachian Mountains, 466.—E. Gilpin. A Comparison of the Distinctive Features of Nova-Scotian Coalfields, 467.—W.Whitaker. The Value of Detailed Geological Maps in relation to Water-supply and other Practical Questions, 468.—J. W. Dawson. On the more Ancient Land- floras of the Old and New Worlds, 469.—G. F. Mathew. The Geological Age of the Acadian Fauna, 470.—G. F. Mathew. The Primitive Cono- coryphean, 471.—H. Miller. On Fluxion-Structure in Till, 472.—J. D. Dana. On the Southward Ending of a great Synclinal in the Taconic Range, 473.—J.H. Panton. Gleanings from Outcrops of Silurian Strata in Red River Valley, Manitoba, 474.—C. E. De Rance. Tenth Report of the Underground Waters Committee, 475.—T. R. Jones. On the Geology of South Africa, 476.—L. W. Bailey. The Acadian Basin in American Geology, 478. —. 1«-——. —. Purchased. 132 ADDITIONS TO THE LIBRARY. Geological Magazine. Dec. III. Vol. ii. Nos. 1-6. 1885. R. A. C. Godwin-Austen, Life of, 1—H. Woodward. Iguanodon Mantelli, Meyer, 10——A. Harker. The Cause of Slaty Cleavage, 15.— A. Irving. Water-supply from the Bagshot Beds, 17.—T. M. Reade. Gulf-Stream Deposits, 25—W. H. Hudleston. Contributions to the Paleontology of Yorkshire, 49.—F. W. Hutton. Geological Nomen- clature, 59.—R. Lydekker. Note on Three Genera of Fossil Artiodactyla, with Description of a new Species, 63.—G. A. Lebour. Note on the Posidonomya Bechert Beds of Budle (Northumberland), with Remarks on the Distribution of the Species, 73.—T.G. Bonney. On the Occur- rence of a Mineral allied to Enstatite in the Ancient Lavas of Eycott Hill, Cumberland, 76.—C. Lapworth. On the Close of the Highland Controversy, 97.—J. J. H.Teail. On some Quartz-Felsites and Augite- Granites from the Cheviot District, 106—W. H. Hudleston. Contri- butions to the Paleontology of the Yorkshire Oolites, 121, 151, 201, 252. —H. Goss. On the recent Discovery of the Wing of a Cockroach and two Scorpions in Rocks of Silurian Age, 129.—R. Lydekker. Note on an apparently new Species of Hyopotamus (H. FPicteti), 151.— B.S. Lyman. Contour-Lines on Geological Maps, 132.—J. S. Gardner. Oscillations of Level along our South Coast since the Human Period, 145. —T.R. Jones. Intermittent Streams in Berkshire, 148.—G. H. Kinahan. Canadian Archzean or Pre-Cambrian Rocks and the Irish Metamorphic Rocks, 159.—R. Lydekker. A Revision of the Antelopes of the Siwaliks, 169.—E. J. Dunn. On the Mode of Occurrence of Gold in the Transvaal Goldfield, 171.—J. W. Judd. On the Occurrence, as a Common Rock- forming Mineral, of a remarkable Member of the Enstatite Group (amblystegite, Vom Rath), 173.—O. Fisher. The Cause of Slaty Cleavage; Shearing vy. Compression, 174.—T. F. Jamieson. The Inland Seas and Salt-Lakes of the Glacial Period, 193M. E. Wadsworth. On the Presence of Syenite and Gabbro in Essex County, Massachusetts, 207.—C. Davison. On a possible Cause of the Disturbance of Magnetic Compass-Needles during Earthquakes, 210.—J. 8S. Gardner. On the Land-Mollusea of the Hocenes, 241.—C. Callaway. A Plea for Com- parative Lithology, 258.—S. H. Scudder. Two more English Car- boniferous Insects, 265.—A. Harker. On the Successive Stages of Slaty Cleavage, 266, eee Purchase, Geologists’ Association. Proceedings. Vol. vii. No. 7. 1884. D. Honeyman. Glacial Distribution in Canada, 377.—A. Strahan and W.D. Carr. Excursion to Lincoln, 383.—H. H. Godwin-Austen. Ex- cursion to Guildford and the new Railway Works in Progress there, 590. —W. Topley. Excursion to the Crystal Palace, 391.—T. V. Holmes. Excursion to Tilbury Docks, 392.—W.H. Dalton. Excursion to Epsom and Dorking, 396.—T. McK. Hughes. Excursion to Cambridge, 399.— T. V. Holmes. On some Curious Excavations in the Isle of Portland, 404.—J. L. Lobley. Excursion to Caterham and Merstham, 411.—C. E. De Rance. Excursion to the International Health Exhibition, 418. : - 2 MNon Sa ose. J. F. Blake. The North-west Highlands and their Teachings, 419,— C. Lapworth. On the Stratigraphy and Metamorphism of the Rocks of the Durness-Eriboll District, 438.—W. A. E. Ussher. On the Geology of South Devon, with special reference to the Long Excursion, 442.— J. Hopkinson. Report on the Excursion to Radlett, 452.—R. N. Worth and A. Champernowne. Report on the Excursion to South Devon, 458. ADDITIONS TO THE LIBRARY. 133 Geologists’ Association. Proceedings. Vol.ix. No.1. 1885. Hi. Hicks. On some recent Researches in Bone-Caves in Wales, 1.— R. Meldola. On some Geological Aspects of the East-Anglian Earth- quake of April 22nd, 1884, 20. Giessen. Oberhessische Gesellschaft fiir Natur- und Heilkunde. Bericht 23. 1884. Glasgow. Geological Society. Transactions. Vol. vii. Part 2 (1882-84). 1885. R. Craig. Volcanic Disturbance of the Ironstone Measures in the vicinity of Dalry during the Carboniferous Period, 233.—J. R. S. Hunter. Biographical Sketch of the late Robert Slimon, 238.—J. Young. On the Identity of Ceramopora (Berenicea) megastoma, McCoy, with Fistu- lypora minor, McCoy, 244.—D. Forsyth. A Bed of Post-glacial Clay, exposed by Dredging in the Harbour of Girvan, Ayrshire, 251.—J. Horne. The Geology of the Isle of Man, 254.—T. King. Notes on a recent Flood in the Deserts of Atacama, North Chile, 262.—J. Young. Notes on Ure’s “ Mil- lepore” Tabuhipora Uru, J. Young (Cellepora Uri, Flem.), 264.—J. R. 8. Hunter. Three Months’ Tent Life amongst the Silurian Hills of Logan Water, Lesmahagow, 272.—T.Scott and J. Steel. Notes on the occurrence of Leda arctica, Gray, Lyonsia arenosa, Moller, and other Organic Remains in the Post-pliocene Clays of Garvel Park, Greenock, 279.—J. Smith. Cleaves Cove, Dalry, Ayrshire, its Exploration and History, 284.—A. Patton. Geological Observations in the Parish of Kast Kilbride, Lanark- shire, 309.—J. White. Random Notes on the English Lake-District, 534.—D, Bell. On the Geology of Ardrossan and West Kilbride, 342.— D.C. Glen. Notes on the Sphexulite Rock of Corriegills, and the Banded Pitchstone of Invercloy, Arran, 352.—D. Forsyth. The Silurian Rocks of the Girvan District, 358.—J. Young. Note on Favosites (?) (Calamo- pora) dentifera, Phillips, 369.—A. Macconochie. Review of the Southern Silurian Question, 370.—J. R. 8. Hunter. The Silurian Districts of Leadhills and Wanlockhead, their early and recent Mining History, 373. —R. H. Traquair. On a specimen of Psephodus magnus, Agassiz, from the Carboniferous Limestones of Hast Kilbride, Lanarkshire, 392.—T. Scott. Some Notes on a Fossiliferous Shale, a little way below the Cloch Lighthouse, 402. Haarlem. Société Hollandaise des Sciences. Archives Neéerlan- daises. Tome xix. Livr. 2-5. 1884. R. D. M. Verbeek. Rapport sommaire sur l’éruption de Krakatau les 26, 27 et 28 aout 1883, 153.—E. H. von Baumhauer. Sur la météorite de Ngawi, tombée le 3 octobre 1883, dans la partie centrale de Vile de * Java, 177. Halifax, N.S. Nova-Scotian Institute of Natural Science. Pro- ceedings and Transactions. Vol.vi. Part 2 (1883-84). 1885. FE. Gilpin, jun. Notes on the Debert Coal-field, Colchester, N.S., 98. —E. Gilpin, jun. Notes on the Manganese Ores of Loch Lomond, 97.— S. D. McDonald. Sable Island, 110.—D. Honeyman. Glacial Action at Rimouski, Canada, and Loch Eck, Argyleshire, Scotland, 119.—D, Honeyman. Notes of a Polariscopic and Microscopic Examination of Crystalline Rocks of Nova Scotia and Cape, Breton, 121.—M. Murphy. Some Physical Features of Nova Scotia, with notes on Glacial Action, 130.—D. Honeyman. Glacial Distribution in Canada, Appendix, xiii. 134 ADDITIONS TO THE LIBRARY. Halle. Kaiserliche Leopoldinisch-Carolinische Deutsche Akademie der Naturforscher. Verhandlungen (Nova Acta). Band xlv. 1884. | F. E. Geinitz. Die skandinavischen Plagioklasgesteine und Phonolith aus dem mecklenburgischen Diluvium, 33. socks | ee eee Baal ox vale eels ——. Zeitschrift fiir Naturwissenschaften. Band lvii. (Folge 4, Band iti.).. Hefte 2-6. 1884. H. Hofmann. Untersuchungen tuber fossile Holzer, 156.—K. Dalmer. Die geologischen Verhaltnisse der Insel Elba, 258. — H. Hofmann. Ueber Pflanzenreste aus dem Knollenstein von Meerane in Sachsen, 456. __, ——. Band Iviii. (Folge 4, Band iv.). Heft 1. 1885. Havre. Société Géologique de Normandie. Bulletin. Tome ix. (1882). 1884. G. Lionnet. Notes géologiques et minéralogiques sur la Bourboule et les environs, 8—C. Beaugrand. Le Cénomanien de Villers-sur-Mer, 16. —E. Savalle. Note sur un gisement de Cardiwm edule a Benerville, 18. —KE. Savalle. Note sur des Silex taillés, de la Période Néolithique, trouvés & Octeville, hameau du Tot, 20.—E. Savalle. Note sur l’Etat des Falaises, du Havre a Cauyville, pendant les années 1881-82, 24.—E. Savalle. Note sur une Station Néolithique, découverte 4 Cauville dans la plaine de Villequier, 26.—F. Prudhomme. Note sur la position du Cap de la Héve dans les temps historiques, 27.—P. Bizet. Notice a Vappui des profils géologiques des chemins de fer de Mortagne 4 Ménil- Mauger et de Mortagne a Laigle, 37.—G. Lennier. Compte-rendu d’une excursion géologique 4 Saint-Jouin, Antifer et Etretat, 56.—Skrodsky. Note sur la présence a Tilly-sur-Seulles du Leprdotus elvensis, 61.—G. Lionnet. Excursicns 4 Tancarville, Lillebonne, Bolbec, Mirville, Fécamp, 64.—C. A. Lesueur. Notice sur les vues et coupes du Cap de la Héve, 82. Hobart Town. Royal Society of Tasmania. Papers and Proceedings for 1882. 1888. R. Etheridge, jun. .A Description of the Remains of Trilobites from the Lower Silurian Rocks of the Mersey-River District, Tasmania, 150.— R. Etheridge, jun. Brachiopoda from the Conglomerate of Table Cape, 158. —. —. — 1883. 1884. : : 1884. 1885. R. M. Johnston. Notes regarding certain Fossil Shells occurring at Table Cape, supposed to be identical with living species, 199.—F. von Miller. References to Baron Constantin von Httingshausen’s recent ’ Observations on the Tertiary Flora of Australia, 203.—R. Tate. Notes of a critical Examination of the Mollusca of the older Tertiary of Tasmania alleged to have living representatives, 207.—T. Stephens. Notes on Boring Operations in search of Coal in Tasmania, 217.—R. M. Johnston. Description of a new Species of Vitrina from the Travertin Beds, Geilston, ——=——— ADDITIONS TO THE LIBRARY. 135 219.—R. M. Johnston. Additions to the list of Table Cape Fossils, together with further Remarks upon certain Fossil Shells supposed to be identical with living species, 220.—R. M. Johnston. Discovery of Ento- mostraca in the Upper Members of the Travertin Beds, Geilston, and a description of a new species of Cypris, 224.—R. M. Johnston. Discovery of a Cone, probably of a species of Lepidostrobus, in the Sandstones of Campania, 225—R. Tate. Description of new Species of Mollusca of the es Kocene Beds at Table Cape, 226.—R. M. Johnston. Description of a new Fossil Shell from the Eocene Beds, Table Cape, 232.—R. M. Johnston. Description of a new Species of Crepidula from the Eocene Beds, Table Cape, 235.—Short. Summary of Observations on Earthquake Phenomena made in Tasmania during 1883 and 1884, 263. Institution of Civil Engineers. Minutes of Proceedings. Vol. lxxvii. 1884. ee Ol Geayie oo. ee a Nel oma oe: Knowledge. Nos. 138-165. 1884. ——. Nos. 166-190. 1885. Lausanne. Société Vaudoise des Sciences Naturelles. Bulletin. Série 2. Vol. xx. Noa90. 1884. Hans Schardt. Etudes Géologiques sur le Pays-d’Enhaut Vaudois, 1. E. Renevier. Le Musée Géologique de Lausanne en 1883, 230. : : - : No. 91. 1885. A. Jaccard. Essai sur les phénoménes erratiques en Suisse pendant la période quaternaire, 381.—H. Golliez. Rapport de la Commission des blocs erratiques 1885-84, 389. Leeds. Philosophical and Literary Society. Annual Report for 1884. 1884. ——. Yorkshire Geological and Polytechnic Society. Proceedings. Nie. eVele will Parts. 13S W. C. Williamson. Biographical Notices of Eminent Yorkshire Geo- logists: III. John Williamson, 295.—R. Carter. On the Mineral Wells at Harrogate, 3138.—C. Fox-Strangways. The Harrogate Wells, or the Mineral Waters of Harrogate geologically considered, 319.—G. Oliver. The Mineral Springs of the Grand Anticlinal of the West Riding, 336.— R. H. Davis. The Mineral Wealth of Harrogate, 357.—hk. L. Whiteley. Analysis of the Kissingen Saline Chalybeate Water, 1885, as compared with Analyses in 1845, 1867, and 1879, 366.—T. Hick and W. Cash. Contributions to the Fossil Flora of Halifax, 370.—G. R. Vine. Further Notes on new Species, and other Yorkshire Carboniferous Fossil Polyzoa described by Prof. John Phillips, 377—H. B. Stocks. On the Compo- sition of the Coal Balls and Baum Pots in the Lower Coal-Measures, 393.—J. W. Davis. On a new Species of Heterolepidotus from the Lias, 408. I 36 ADDITIONS TO THE LIBRARY. Leicester. Literary and Philosophical Society. Report and Trans- actions, 1883-84. 1884. J. Marriott. The Beds exposed in the Railway-cutting at Slawston Hill, 80.—H. E. Quilter. The Rhetic Beds of the Spinney Hills, 81. —J.D. Paul. The Cores from a Boring made near Evington, 83.— H. E. Quilter. The Cutting near Market Harborough Station, 86. —. . Session 1884-85. Inaugural Address delivered by G. Shaw, October 6th, 1884. (8vo.) 1885. ——. Town Museum. 10th Report of the Museum-Committee to the Town Council, 1882-84. 1884. Leipzig. Zeitschrift fir Krystallographie und Mineralogie. Band vii. Heft 5. 1883. Purchased. : . Bandix. Hefte 3-6. 1884. Purchased. C. Morton. Stephanit von Kongsberg, 238.—J. Lorenzen. Unter- suchung einiger Mineralien aus Kangerdluarsuk, 243.—J. A. Krenner. Ueber den Szaboit, 255.—H.S. Dana. Ueber Herderit von Stoneham, Maine, 278.—C. Dolter. Zur Synthese des Nephelins, 321.—A. Forstner. Ueber kinstliche physikalische Veranderungen der Feldspathe von Pan- telleria, 333.—A. Cathrein. Neue Krystallformen tirolischer Mineralien, 353.—A. Cathrein. Ueber den Orthoklas von Valfloriana, 368.—A. Cethrein. Ueber Umwandlungspseudomorphosen yon Skapolith nach Granat, 378.—E. Palla. Ueber die vicinalen Pyramidenflachen am Natrolith, 386.—T. Liweh. Anglesit, Cerussit und Linarit von der Grube “ Hausbaden ” bei Badenweiler, 499, : . Band x. Hefte 1-3. 1885. Purchased. — E. Kalkowsky. Ueber Olivinzwillinge in Gesteinen, 17.—T. Hiortdahl. Colemanit, ein krystallisirtes Kalkborat aus Californien, 25.—C. Busz. Ueber den Baryt von Mittelagger, 32.—A. Knop. Ueber die Augite des Kaiserstuhlgebirges im Breisgau (Grossherzogthum Baden), 58.—H. Sjogren. Ueber die Manganarseniate von Nordmarken in Wermland, 113. —G. Vom Rath. Mineralogische Mittheilungen, 156.—C. Bodewig und G. Vom Rath. Colemanit aus Californien, 179.—O. Liidecke. Ueber Thiringer Mineralyorkommnisse (Orthit, Datolith, Albit, Anatas), i86.— A. Schmidt. Ueber die Minerale von Palsécz-Ardo, 202.—A. Schmidt. Die Minerale eines Andesits von der Umgegend yon Malnas, 210.—G. E. Moore und V. von Zepharovich. Kallait Pseudomorph nach Apatit aus Californien, 240. Leyden. Geologische Reichs-Museums Sammlungen. No.10. 1884. Purchased. Beitrage zur Geologie Ost-Asiens und Australiens, Band iv. Heft 1: Ueberreste vorweltlicher Proboscider von Java und Banka von K. Martin (pp. 1-24, pl. 1). Liége. Société Géologique de Belgique. Annales. Tome x. (1882-83). 1884. A. de Ceuleneer. Le dolmen de Wéris, lx.—G. Dewalque. Un nou- veau gite fossilifére dans le poudingue de Burnot, lxix.—G. Dewalque. Sur la hatchettite de Seraing, Ixxi—G. Dewalque. Sur Pholadomya Esmarkit, Ryckh. (non Pusch, non Nilss.), Ixxxv.—A. Firket. Sur Vextension, en Angleterre, du bassin houiller franco-belge, xcili—A. Firket. Découverte de la chalcocite & Moét-Fontaine (Rahier), xevii.— —_—— ADDITIONS TO THE LIBRARY. Fe a M. Lohest. Découverte de stringocéphales dans le poudingue de Burnot & Nessonvaux, xcix.—L. L. de Koninck. Infiuence de la pyrite sur le dosage des composés ferreux dans les silicates, ci—G. Cesaro. Sur un silicate double de zinc et d’aluminium hydraté, exi.—G. Cesaro. Sur la probabilité de la Voltzine cristallisée, cxii—E. Delvaux. Note prélimi- naire sur un dépot d’ossements de mammitéres découvert dans la tourbe, aux environs d’Audenarde, cxliii.i—A. Rutot. Note sur les découvertes de vertébrés fossiles dans l’Hocéne inférieur de Belgique, cliv.—G. Dewalque. Compte-rendu de la session extraordinaire de la Société, tenue a Liége les 26, 27 et 28 aout 1888, clviii. Mémoires. E. Delvaux. Note sur le forage d’un puits artésien exécuté 4 la fabrique de MM. Dupont, fréres, 4 Renaix, 2.—C. Malaise. Sur la composition du massif Ardoisier du Brabant, 19.—C. Ubaghs. La machoire de la Chelonia Hoffmanni, Gray, 25.—G. Cesaro et G. Despret. La Richellite, nouvelle espéce minérale des environs de Vise, 36.—J. Fraipont. Re- cherches sur les crinoides du famennien (devonien supérieur) de Belgique, 45. Bibliographie. H. Forir. Mémoire sur la formation dela houille, par C. Grand’Eury, 3. —H. Forir. Sur la maniére d’étre des structures grenue et porphyrique dans les roches éruptives, par A. Rosenbusch, 17. Liége. Société Géologique de Belgique. Annales. Tome xi. (1883-84). 1884. E. Delvaux. Sur l’extension du dépét erratique de la Scandinavie en Belgique, lvii—G. Dewalque. Sur des empreintes végétales trouvées dans l’6tage gedinnien prés de Vielsalm, 1xi1—G. Dewalque. Sur la rhodochrosite de Chevron, Ixiii—A. Cocheteux. Sur la découverte de malachite 4 Chokier, de wad a Flémalle-Haute et (aragonite 4 Angleur, lxix.—J. Libert. Sur le minerai de zinc de Beaufays et sur un gite de limonite a Louveigné, lxx.—H. Forir. Note sur un gisement de bois fossile 4 Beaumont, Ixxiii.—R. Storms. Un nouveau gite diestien fossilifére, lxxxii—M. Lohest. Sur les minéraux et fossiles du calcaire carbonifére inférieur des vallées de YOurthe et de l’Ambléve, lxxxii.— A.de Vaux. Sur lapatite de Marvao, Portugal, xciii—V. Watteyne. Sur une transformation remarquable d’une couche de houille, xcv.—V. Watteyne et G. Dewalque. Sur la présence de la barytine dans l’étage houiller du couchant de Mons, xevii.—A. Firket. Documents pour l’étude de la répartition stratigraphique des végétaux houillers de la Belgique, xeix.—H. Delvaux. Présentation d’un bloc anguleux zirconien, trouvé dans la Flandre, cii—C. De la Vallée Poussin. Sur le landénien supé- rieur, civ.—G. Dewalque. Sur la terminaison N.E. du massif cambrien de Stavelot, cxix.—M. Lohest. Découverte de gisements de phosphate de calcium en certains points de la Hesbaye, exx.—E. Delvaux. Epoque quaternaire. Sur quelques nouveaux fragments de blocs erratiques re- cueillis dans la Flandre et sur les collines francaises, exlii.—O. van Ert- born et P. Cogels. Sur quelques dépéts modernes des environs d’Anvers, exlix. Mémoires. E. Delvaux. Des puits artésiens de la Flandre, 3, 118. — W. Spring. Note sur la véritable origine de la différence des densités d’une couche de calcaire dans les parties concaves et dans les parties convexes du méme pli, 48.—E. Delvaux. De l’extension des dépots glaciaires de 138 ADDITIONS TO THE LIBRARY. la Scandinavie et de la présence de blocs erratiques du Nord dans les plaines de la Belgique, 52.—EK. Prost. Sur la salmite de Dumont, MS., chloritoide manganésifére, 93.—J. Fraipont. Notice sur une caverne 4 ossements d’ Ursus speleus, 98.—J. Fraipont. Recherches sur les cri- noides du famennien (devonien supérieur) de Belgique, Partie IIT., 105.— W. Spring et E. Prost. Etude sur les eaux de la Meuse, 123.—A. Firket. Composition chimique de quelques calcaires et de quelques dolomies des terrains anciens de la Belgique, 221.—G. Cesaro. Mémoire traitant: 1° de la koninckite, 2° de la formule de la richellite, 3° de Voxyfluorure de fer, 247.—E. Delvaux. Découverte de gisements de phosphate de chaux appartenant 4 l’étage ypresien dans le sous-sol de la ville de Renaix et dans celui de la région de Flobecq, 279.—M: Lohest. Recherches sur les poissons des terrains paléozoiques de Belgique: Poissons de lampélite alunifére, des genres Campodus, Petrodus et Xystracanthus, 294. Bibliographe. H. Forir. Sur la déposition stratigraphique et les roches éruptives des Ardennes francaises, principalement du massif de Rocroy, par A. von Lasaulx, Bibl., 3—H. Forir. Recherches sur le développement des roches schisto-cristallies anciennes....par J. Lehmann, 20.—H. Forir. Sur les zones climatériques pendant les périodes jurassique et crétacée, par M. Neumayr, 25.—F. Dewalque. Sur le gisement et l’exploitation de la strontianite en Westphalie, 41. Lille. Société Géologique du Nord. Annales. Tome xi. (1883-84). Livr.3 & 4. 1884. J.Gosselet, Sur la faillede Remagne et sur le métamorphisme qu'elle a produit, 176.—J. Ortlieb et A. Six. Une excursion a Pernes, 190.—J. Ortlieb. Fossiles diluviens trouvés 4 Willems, 199.—A. Six. Les Fou- géres du terrain houiller du Nord, 201.—A. Six. Un oiseau landénien en Belgique, 212.—A. Six. Les Crocodiles de Bernissart, 214.—C. Barrois. Sur les ardoises 4 Nereites de Bourg d’Orieil, Haute-Garonne, 219.—C. Barrois. Sur étage aptien de la Haute-Garonne, 227.—A. Six. Les appendices des Trilobites, 228.—A.Six. Un nouveau Dinosaurien d’aprés le professeur O. C. Marsh, 237.—Boussemaer. Note sur les couches supé- rieures du Mont Aigu, 243, 381.—J. Gosselet. Note sur quelques affleure- ments de poudingues devonien et liassique et sur lexistence de dépdts siluriens dans l’Ardenne, 245.—Hassenpflug. Sur Vozokérite, 253.— J. Gosselet. Note sur les schistes de Saint-Hubert dans le Luxembourg et principalement dans le bassin de Neufchateau, 258.—C. Barrois. Ob- servations sur la constitution géologique de la Bretagne, 278.—A. Six. Compte-rendu de l’excursion annuelle | environs de Bavai], 285.—A. Six. Le Batracien et les Chéloniens de Bernissart [d’aprés M. Dollo |, 297.— A. Six. Les Dinosauriens carnivores du Jurassique américain, d’aprés M. le prof. O. C. Marsh, 306.—C. Barrois. Note préliminaire sur les schistes 4 staurotides du Finistére, 312.—A. Six. Le Challenger et les abimes de la mer [d’aprés MM. Murray et Renard], 313.—A. Six. [Les hydrocarbures naturels de la série du petrole,| 334—J. Gosselet. Re- marques sur la faune de l’assise de Vireux, 336.—J. Gosselet. Note sur deux roches cristallines du terrain devonien du Luxembourg, 338.—C. Queva et H. Fockeu. Compte-rendu de l’excursion dans le massif de Stavelot, 340, 360.—H. Fockeu. Compte-rendu de l’excursion du 5 Juin 1884 dans les environs de Mons, 363.—C. Queva. Compte-rendu d’une excursion géologique dans le terrain jurassique de Maubert-Fontaine a Lonny, 369.—J. Gosselet. Etude sur les tranchées du chemin de fer de VEst entre Saint-Michel et Maubert-Fontaine, 376.—T. Mellard Reade. Domes en miniature a la surface des sables, 379. ADDITIONS TO THE LIBRARY. 139 Lille. Société Géologique du Nord. Annales. Tome xii. (1884— 85). Livr. 1-3. 1885. C. Barrois. Le granit de Rostrenen, ses apophyses et ses contacts, 1.— A. Six. Les Dinosauriens de Bernissart, 120.—Cambessedés. Travaux de sondage en Hainaut, 124.—Jannel. Etude géologique de la ligne de Mézy a Romilly, 127.—S. Calderon. Résumé de quelques recherches orographiques dans le plateau central de l’Espagne, 148.—C. Barrois. Légende de la feuille de Granville, 154.—C. Maurice. Le Lac tertiaire Florissant, Colorado: Analyse d’un travail de M. Samuel Scudder, 158. —G. Lecocq. Excursion de l’Association frangaise pour l’avancement des sciences (sections de géologie et d’anthropologie) faite 4 Thenay, le 8 Sep- tembre 1884, lors du Congrés a Blois, 169.—C. Barrois. Observations sur des sédiments clastiques du bassin de Paris, d’aprés le mémoire du Dr. Hans Thiirach, 172.—J. Gosselet. Note sur les schistes de Bastogne, 173. —J.Gosselet. Sur la structure géologique de l’Ardenne d’aprés M. von Lasaulx, 195.—A. Six. Le granite ardennais, 202.—A. Six. Les Scor- pions fossiles, 229.—J. Gosselet. Note sur divers sondages faits aux en- virons de Lille, 246.—H. Fockeu. Note sur la craie de Lille, 255. Linnean Society. Journal. Botany. Vol. xxi. Nos. 134 & 1385. 1884. Nos. 136 & 137. 1885. a Zoology. Vol. xvii. No.103. 1884. A. W. Waters. Closure of the Cyclostomatous Bryozoa, 400. ‘ ; . Volexyaii. Nos. 104-106. 1884. P. Martin Duncan. A Revision of the Families and Genera of the Sclerodermic Zoantharia, Ed. & H., or Madreporaria (M. rugosa ex~- cepted), 1. ———EE cae Se ° e —— : A : sees: 107 & 108. 1885: J. W. Davis. On Heterolepidotus grandis, a Fossil Fish from the Lias, 293.—P. Martin Duncan. On the Family Arbaciade, Gray: Part L The Morphology of the Test in the Genera Celopleurus and Arbacia, 25. ——. Transactions. Ser. 2. Botany. Vol. u. Part 7. 1884. ——. “Zoology. Vol.i. Part 10. 1884. Lisbon. Secc&o dos Trabalhos Geologicos de Portugal. Communi- cacdes. Tomoi. Fasc. 1 (1885). 1885. [Anciennement: Commission Géologique du Portugal.] (8vo.) J. F. N. Delgado. Consideragdes acerca dos estudos geologicos em Portugal, 1—A. Ben-Saude. Anomalias opticas de crystaes tesseraes, 15.—P. Choffat. De Vimpossibilité de comprendre le Callovien dans le Jurassique supérieur, 69.—D. J. Macpherson. LEstudo petrographico das ophites e teschenites de Portugal, 89.—P. Choffat. Nouvelles données sur les vallées typhoniques et sur les éruptions d’ophite et de teschénite en Portugal, 113.—Rapport des membres portugais des sous-commissions hispano-lusitaniennes en vue du Congrés géologique international devant avoir lieu & Bologne en 1881, 123.—Réponse de la sous-commission portugaise 4 la circulaire de M. Capellini, Président de la Com- mission internationale de nomenclature géologique, 134.—Rapport de la sous-commission portugaise de nomenclature, en vue du Congrés géolo- gique international devant avoir lieu a Berlin en 1884, 141.—P. Choffat. ——_— 140 ; ADDITIONS TO THE LIBRARY. Age du granite de Cintra, 155.—P. Choffat. Sur la place 4 assigner au Callovien, 159. Lisbon. Sociedade de Geographia. Boletin. 42 Serie. Nos. 6-8, 10 &11. 1883. Liverpool Geological Society. Proceedings. Vol.iv. Part 6 (1883 —84). 1884. . D. Mackintosh. The Time which has elapsed since the Close of the Glacial Period, 417.—G. H. Morton. Section across the Trias recently exposed by a Railway Excavation in Liverpool, 427._T. M. Reade. Experiments on the Circulation of Water in Sandstone, 434.—C. Ricketts. On Indented Pebbles in the Bunter Sandstone near Prescot, 447. London, Edinburgh, and Dublin Philosophical Magazine and Journal of Science. Ser. 5. Vol. xvii. Nos. 110-115. 1884. Pre- sented by Dr. W. Francis, F.GS. H. A. Miers. Hemihedrism of Cuprite, 127.—J. Croll. On the Cause of Mild Polar Climates, 268. : . Vol. xix. Nos. 116-121. 1885. Presented by Dr. W. Francis, F.GS. J. Croll. On Arctic Interglacial Periods, 30. London Iron Trades Exchange. Nos. 1307-1333. 1884. —. Nos. 13834-1357. 1885. Manchester. Geological Society. Transactions. Vol. xvii. Parts 16-18 (1883-84). 1884. J. D. Kendall. The Mineral Veins of the Lake District, 292. ‘ : Vol. xviii. Parts 1-9. 1884-85. W. Boyd Dawkins. Onsome Deposits of Apatite near Ottawa, Canada, — 47,—C. KE. De Rance. On the Occurrence of Brine in the Coal Measures, with some remarks on Filtration, 61—W. Boyd Dawkins. The Car- boniferous Flora, 101.—G. H. Kinahan. On a possible Genesis of the Canadian Apatite, 123——G. A. Kinahan. Notes on Professor Boyd Dawkins’s paper, “ Apatite Deposits near Ottawa,” 1382.—M. Stirrup. On Coal and Coal Plants, 189. Melbourne. Royal Society of Victoria. Transactions. Vol. xx. 1834. | J. Stirling. On the Caves perforating Marble Deposits, Limestone Creek, 7.—A. W. Howitt. The Rocks of Noyang, 18. Mineralogical Society. Mineralogical Magazine and Journal. Vol. vi. Nos. 27-29. 1884. K. J. V. Steenstrup. On the existence of Nickel-Iron with Wid- mannstatten’s figures in the Basalt of North Greenland, 1—J. Lorenzen. A chemical examination of Greenland Telluric Iron, 14.—T. G. Bonney. On some specimens of Lava from Old Providence Island, 39.—H. Louis. Note on a new mode of occurrence of Garnet, 46.—T. G. Bonney. Note on a case of replacement of Quartz by Fluor Spar, 48.—W. Simmons. Notes on “ Enargite” from Montana, U.S.A., 49.—C. O. Trechmann. Analysis of an altered Siderite from Helton Beacon Lead Mine, near ADDITIONS TO THE LIBRARY. I4i Appleby, 52.—T. G. Bonney. Notes on a Picrite (Paleopicrite) and other Rocks from Gipps’ Land, and a Serpentine from Tasmania, 54.— H. A. Miers. The Crystallography of Bournonite, 59.—R.H.Solly. On the tetartohedral development of a Crystal of Tourmaline, 80.—T. Car- nelley. Applications of the Periodic Law to Mineralogy, 83.—W. J. Macadam. On Diatomaceous deposits in Scotland, 87.—H. M. Cadell. On the Age and Origin of the Metallic Veins of the Upper Harz, 90.—J. Horne. The Origin of the Andalusite Schists of Aberdeenshire, 98.— W. Morrison. The mineral Albertite, Strathpefter, Ross-shire, 101.—A. Taylor. On the occurrence of Prehnite and other minerals in the Rocks of Samson’s Ribs and Salisbury Crags, 104.—T. Wallach. On Kyanite localities in the North, 106.—T. A. Readwin. Note on Welsh Gold, 108.—W. H. Bell. Note on a new locality for Zoisite, 109.—T. G. Bonney. Address to the Mineralogical Society, 111.—R.H.Solly. Fine crystals of pale lilac Calcite from Tankerville Mine, near Shelve, Shrop- shire, 120.—Guyot de Grandmaison. Description ofa crystal of Parisite, 123.—W. Semmons. Further notes on Enargite, 124—W. W. Peyton. Some occurrences of Actinolite in Scotland, 126.—J. E. Ady. Observa- tions on the preparation of mineral and rock-sections for the Micro- scope, 127. Montreal. Natural History Society. Canadian Record of Science. Vol.i. No. 1. 1884. [Replacing the Canadian N aturalist. | (8vo.) | J. W. Dawson. On Rhizocarps in the Paleozoic Period, 19.—J. W. Dawson. Notes on Eozoon canadense, 58. Moscow. Société Impériale des Naturalistes. Bulletin, 1883. Tome lvii. No. 4. 1884. H. Trautschold. Bemerkungen zur geologischen Karte des Wetluga- Gebiets, 205.—A.de Gregorio. Une nouvelle Pleurotoma du Miocéne de Italie, Pleurotoma Renardi, de Greg., 301.—V. Sokol. [Materials for the Geology of the Crimea, | 309 (in Russian). —. ——. —,1884. Tomelix. Nos.1 &2. 1884. , . Nouveaux Mémoires. Tome xv. Livr.1. 1884. H. Trautschold. Die Reste permischer Reptilien des palaontologischen _ Kabinets der Universitat Kasan, 5. . Munich. Koniglich-Bayerische Akademie der Wissenschaften. Ab- handlungen. Band liti. Abth.1. 1884. LL. von Ammon. Ueber neue Exemplare von jurassischen Medusen, 105. : Sitzungsberichte der Mathematisch-Physikalischen Classe, 1883. Heft 3. 1884. F. Pfaff. Untersuchungen iiber die absolute Harte des Kalkspathes und Gypses und das Wesen der Harte, 372. ee eer’ (6e4- Hetto 1 & 2; - 1884. Nancy. Société des Sciences de Nancy. Bulletin. Série 2. Tome yi. Fase. 16 (1883). 1884. P. Fliche. Description d’un nouveau Cycadeospermum du terrain Jurassique moyen, 55, I42 ADDITIONS TO THE LIBRARY, Nature. Vol. xxx. Nos. 765-783. 1884. The Extinct Lakes of the Great Basin, 197.—Geology at the British As- sociation, 217.—British Association, Section C, Geology, 440, 526, 553. —H. J. Johnston-Lavis. Earthquakes, 608. —. Vol. xxxi. Nos. 784-809. 1884-85. A. Geikie. The Crystalline Rocks of the Scottish Highlands, 29.—B. N. Peach and J. Horne. Report on the Geology of the North-west of Sutherland, 31—W.G.8. Paterson. The new Volcanic Island off Ice- land, 37.—O. C. Marsh. The Classification and Affinities of Dinosaurian Reptiles, 68.—The Earthquake in Spain, 199, 237._S. Lupton. The Coal Question, 242.—B. N. Peach. Ancient Air-Breathers, 295—J. J. H. Teall. The Scope and Method of Petrography, 444.—J. E. Tenison- Woods. The Borneo Coal Fields, 583.—W. H. Hudleston. Further Notes on the Geology of Palestine, with a Consideration of the Jordan Valley Scheme, 614. : ——. Vol. xxxn. Nos. 810-816. 1885. H. J. Johnston-Lavis. The new Outburst of Lava from Vesuvius, 55. Neuchatel. Société des Sciences Naturelles. Bulletin. Tome xiv. 1884. A. Jaccard. Note sur les sources de Combe-Garot, 63.—A. Jaccard. Les couches 4 Mytilus des Alpes Vaudoises et du Simmenthal et leur véritable horizon géologique, 152.—A. Jaccard. Sur les vertébrés fossiles découverts récemment dans l’Amérique du Nord, 191.—L. Charpy et M. de Tribolet. Note sur la présence du terrain crétacé 4 Montmercy-la- Ville, arrondissement de Dole, Jura, 198. Newcastle-under-Lyme. North-Staffordshire Institute of Mining and Mechanical Engineers. Transactions. Vol. i. (1873-75). 1879. (8vo.) : C.J. Homer. The North Staffordshire Coal-field, with the Ironstones contained therein, 102.—R. A. Marshall. Mineral Oil as found at the Deep Main Pits, Riddings, Derbyshire, 126.—Section of Strata sunk through (with shaft 16 feet diameter), at Rose Bridge Collieries, Ince, near Wigan, 159.—Section of Strata sunk through at Astley Deep Pit, Dukinfield, 181—Thermometrical Observations in the Dukinfield Col- liery, 190. —— : : Vol. u. (1875-78). 1881. C. J. Homer. The North Staffordshire Coal-field, with the Ironstones contained therein, 11—G.G. Audré. Lecture on the Geology of Coal, 102.—G. G. André. Cleavage Planes and their Influence or the Econo- mical Working of Coal, 132. ieceeh vi yee ear etintremng '/ Were gts cc ele: de ge Neyo Be) 3 > Vol. iv. (1879-80). 1879-80. W.C. Williamson. On Coals and Coal Plants, 151. a yc pe Vol ge (ISSO Sy a0 oP ii) Te EO ya RBI gen) qage tee : : . Vol. vii. Parts 1-7 (1883-84). 1883-85. J. R. Haines. The Channel Tunnel, 16. ADDITIONS TO THE LIBRARY. 143 Newcastle-upon-Tyne. Natural History Society and Tyneside Naturalists’ Field Club. Natural History Transactions of Northumberland, Durham, and Neweastle-upon Tyne. Vol. vill. .,.Part. 1/1884. G. A. Lebour. A Statement as to recent Publications relating to Anodonta Jukesvi, 30.—T. T. Clarke. The Yorkshire Caves, 50.—A. M. Norman. Presidential Address to the Members of the Tyneside Natura- lists’ Field Cub, 67 (Part II. The Abysses of the Ocean, 91).—S. Oswald. On a Perched Block of Sandstone in Lunedale, 181. —. North of England Institute of Mining and Mechanical Engineers. Transactions. Vol. xxxvi. Parts 1-3. 1885. E. Halse. On the Manganese Deposit of the Islet of San Pietro, Sar- dinia, 145.—F. W. Rudler. Notes on Microscopic Sections of Rocks from San Pietro, Sardinia, 159. ; An Account of the Strata of Northumberland and Durham, as proved by Borings and Sinkings. F-K. (8vo.) 1885. —_——— New Haven, Conn. American Journal of Science. Ser. 3. Vol. xxviii. Nos. 163-168. 1884. F, W. Clarke and T. M. Chatard. Mineralogical Notes from the Laboratory of the United States Geological Survey, 20.—S. L. Penfield. On the Occurrence of Alkalies in Beryl, 25.—G. F. Wright. The Niagara River and the Glacial Period, 32.—S. W. Ford. Note on the Discovery of Primordial Fossils in the Town of Stuyvesant, Columbia County, N.Y., 35.—W. P. Blake.—Crystallized Gold in Prismatic Forms, 57.—A. Gray. Memorials of George Engelmann and of Oswald Heer, 61.—M. E. Wads- worth. Notes on the Rocks and Ore Deposits in the vicinity of Notre Dame Bay, Newfoundland, 94.—S. F. Peckham. The Origin of Bitu- mens, 105.—S. B. Newberry. On some Specimens of Nickel Ore from Nevada, 122.—W. M. Davis. Gorges and Waterfalls, 123.—F. H. Blake. Vanadinite in Pinal County, Arizona, 145.—O.C. Marsh. On the United Metatarsal Bones of Ceratosawrus, 161.—S. H. Scudder. Triassic Insects from the Rocky Mountains, 199.—O. A. Derby. On the Flexibility of Itacolumite, 203.—S. W. Ford. On the Age ofthe Glazed and Contorted Slaty Rocks in the vicinity of Schodack Landing, Rensselaer County, N. Y., 206.—G. F. Becker. The Relations of the Mineral Belts of the Pacific Slope to the Great Upheaval, 209.—J. L. Campbell. Geology of the Blue Ridge near Balcony Falls, Virginia, 221.—J. 8. Diller. Fulgur- . ite from Mount Thielson, Oregon, 252.—G. H. Williams. On the Para- morphosis of Pyroxene to Hornblende in Rocks, 259.—J. D. Dana. On the Southward Ending of a great Synclinal in the Taconic Range, 268.— H. C. Lewis. On supposed Glaciation in Pennsylvania south of the Terminal Moraine, 276.—J. W. Mallet. On a mass of Meteoric Iron from Wichita County, Texas, 285.—W. P. Blake. Columbite in the Black Hills of Dakota, 340.—R. E. Browne. Criticism of Becker’s Theory of Faulting, 348.—J. D. Dana. Note on the Cortlandt and Stoney Point Hornblendic and Augitic Rocks, 384.—W. M. Davis. The Distribution and Origin of Drumlins, 407.—J. P. Kimball. Geological Relations and Genesis of the Specular Iron Ores of Santiago de Cuba, 416.—C. A. Schaeffer. A new Tantalite Locality, 430.—D. Walcott. Note on Palzo- zoic Rocks of Central Texas, 431.—A. C. Baines. On the Sufficiency of Terrestrial Rotation for the Deflection of Streams, 454.--O. A. Derby. Peculiar Modes of Occurrence of Gold in Brazil, 440.—A. W. Jackson. VoL, XLI,. 0 144 ADDITIONS TO THE LIBRARY. On Colemanite, anew Borate of Lime, 447,—_J. D. Dana. On the Decay of Quartzyte, and the Formation of Sand, Kaolin, and Crystallized Quartz, 448, New Haven, Conn. American Journal of Science. Ser. 3. Vol. xxix. Nos. 169-174. 1885. W.H. Brewer. On the Suspension and Sedimentation of Clays, 1— J.D. Dana. On a System of Rock Notation for Geological Diagrams, 7.—A. Geikie. The Crystalline Rocks of the Scottish Highlands, 10.— S. W. Ford. Observations upon the Great Fault in the vicinity of the Schodack Landing, Rensselaer County, N. Y., 16.—J. Croll. On the Cause of Mild Polar Climates, 20, 188.—A. L. Ewing. An Attempt to determine the Amount and Rate of Chemical Erosion taking place in the Limestone (Calciferous to Trenton) Valley of Center County, Pa., and hence applicable to similar regions throughout the Appalachian Regions, 29.—E. G. Smith. On the Chrysotile from Shipton, Canada, 23.—O. A. Derby. The Santa Catharina Meteorite, 33.—F. D. Chester. The Gravels of the Southern Delaware Peninsula, 36.—J. D. Dana. Decay of Quartzyte: Pseudo-breccia, 57.—J. W. Powell. The Organi- zation and Plan of the United States Geological Survey, 93.—C. D. Walcott. Palzeontologic Notes, 114.—J. H. Kinahan.—Use of the term “Esker” or Kim Drift, 135.—J. A. Perry. Note on a Fossil Coal Plant found at the Graphite deposit in Mica-schist at Worcester, Mass., 157.—L. E. Hicks. The Test Well in the Carboniferous For- mation at Brownville, Neb., 159—O. C. Marsh. Monograph of the Dinocerata, 173.—J. D. Dana. On Taconic Rocks and Stratigraphy, with a Geological Map of the Taconic region, 205.—C. A. White. Notes on the Jurassic Strata of North America, 228.—N. T. Lupton. Meteoric Iron from Coahuila, Mexico, 232.—R. D. Irving. Divi- sibility of the Archean in the North-west, 237—W. E. Hidden. Mineralogical Notes, 249.—C. A. White. The Genus Pyrgulifera, Meek, and its Associates and Congeners, 277.—E. W. Wilkinson. On the Oc- currence of Native Mercury in the Alluvium in Louisiana, 280.—C. G. Rockwood. The Earthquakes in Spain, 282.—J. M. Clarke. On Devo- nian Spores, 284.—T. M. Reade. Denudation of the two Americas, 290. —J.Croll. On Arctic Interglacial Periods, 300.—C. D. Walcott. Palee- ozoic Notes: New Genus of Cambrian Trilobites, Mesonacis, 328.— Le Roy W. McCay. Massive Safflorite, 369.—F. W. Clarke and J. S. Diller. Topaz from Stoneham, Maine, 378.—C. Whittlesey. The Pre- glacial Channel of Hagle River, Keweenaw Point, Lake Superior, 392.— —S. W. Ford. Note on the Age of the Slaty and Arenaceous Rocks in the vicinity of Schenectady, Schenectady County, N. Y., 397.—J. D. Dana. Taconic Rocks and Stratigraphy, 487.—J. F. Whiteaves. Notes on the possibleAge of some of the Mesozoic Rocks of the Queen Charlotte Islands and British Columbia, 444.—S. L. Penfield. Crystallized Tie- mannite and Metacinnabarite, 449.—A. G. Dana. Gahnite of Rowe, Mass., 455.—O. Meyer. The Genealogy and the Age of the Species in the Southern Old-tertiary, 457.—C. U. Shepard. Meteoric Iron from Trinity County, California, 469.—H. D. Campbell. The Potsdam Group east of the Blue Ridge at Balcony Falls, Virginia, 470.—A. Lindenkohl. Geology of the Sea-bottom in the Approaches to the New York Bay, 475. —B. F. Koons. Kettle-Holes of the Wood’s Holl Region, Mass., 480,.— G. H. Williams. Cause of the apparently Perfect Cleavage in American Sphene (Titanite), 486. New Haven, Conn. Connecticut Academy of Arts and Sciences. Transactions. Vol. vi. Part 1. 1884. ADDITIONS TO THE LIBRARY. 145 Newport, R.1. Natural History Society. Proceedings, 1883-84. Document 2. 1884. T. N. Dale. The Geology of the tract known as “ Paradise,” near Newport, 3.—T. N. Dale. Remarks on some of the Evidences of Geolo- gical Disturbance in the vicinity of Newport, 5.—E. F. Clark. Studies in the Rhode-Island Coal Measures, 9.—A. D. Wilson. A Trip through North-western Wyoming, 25. New York. Academy of Sciences. Annals. Vol. iii. Nos.1& 2. 1883. —. American Institute of Mining Engineers. Transactions. Vol. xii. 1884. Presented by Wm. Whitaker, Esq., F.GS. A. 8. McCreath. The Iron Ores of the Valley of Virginia, 17.—C. R. Boyd. The Ores of Cripple Creek, Virginia, 27.—C. H. Hitchcock. The Geological Position of the Philadelphia Gneisses, 68.—P. Frazer. An Hypothesis of the Structure of the Copper Belt of the South Mountain, 82. —C.H. Henderson. The Copper Deposits of the South Mountain, 85.— J.C. Smock. Geologico-geographical Distribution of the Iron Ores of the Eastern United States, 130.—E. J. Schmitz. Contributions to the Geology of Alabama, 144.—F. P. Dewey. Some Canadian Iron Ores, 192. —H. M. Howe. A Systematic Nomenclature for Minerals, 238.—P. Frazer. The Northern Serpentine Belt in Chester County, Pa., 349.—P. Frazer. The Peach Bottom Slates of South-eastern York and Southern Lancaster Counties, 355.—T. 8. Hunt. The Apatite Deposits of Canada, 459,—J. P. Kimball. The Quemahoning Coal-field of Somerset County, Pennsylvania, 468.—-W. H. Adams. The Pyrites Deposits of Louisa County, Va., 527.—P. Frazer. Certain Silver and Iron Mines in the States of Nuevo Leon and Coahuila, Mexico, 537.—N. W. Perry. A new Mineral, 628.—W. B. Devereux. Notes on Iron-Ore Deposits in Pitkin County, Colorado, 638. Northampton. Northamptonshire Natural-History Society and Field Club. Journal. Vol. ii. Nos. 19 & 22. 1884-85. C. A. Markham. The great English Earthquake, 107.—B. Thompson and T. J. George. A Catalogue of the Geological Collection in the North- -ampton Museum, 154.—B. Thompson. On Swallow-Holes and Dumb- Wells, 159.—Henry J. Eunson. On a probable Fault in the Lias under Northampton, 169.—B. Thompson. The Upper Lias of Northampton- shire, 182.—B. Thompson and T. J. George. A Catalogue of the Geolo- gical Collection in the Northampton Museum: Part II. The Carbonife- rous System, 240. Paleontographical Society. Monographs. Vol. xxxvili. 1884. (Two copies.) J.S. Gardner. A Monograph of the British Eocene Flora, vol. ii. part 2: Gymnospermia.—T. Rupert Jones, J. W. Kirkby, and G. 8. Brady. A Monograph of the British Fossil Bivalved Entomostraca from the Carboniferous Formations, part 1, no. 2: The Cypridinade and their Allies—H. Woodward. A Monograph of the British Carboniferous Tri- lobites, part 2.—T. Davidson. A Monograph of the British Fossil Bra- chiopoda, vol. v. part 3—T. Wright. Monograph on the Lias Ammo- nites of the British Islands, part 7. 02 146 ADDITIONS TO THE LIBRARY. Paris. Académie des Sciences. Comptes Rendus. Tome xcyiii. Nos. 25 & 26. 1884. R. Zeiller. Sur des cones de fructifications de Sigillaires, 1601. : : . Tome xcix. Nos. 1-26. 1884. B. Renault et R. Zeiller. Sur un nouveau genre de graines du terrain houiller supérieur, 56.—Sace. Sur un dépdt de salpétre dans le voisi- nage de Cochabamba, Bolivie, 84.—A. Carnot. Sur Vorigine et la distri- bution du phosphore dans la houille et le cannel-coal, 154.—B. Renault. Quatriéme note pour servir a l’histoire de la formation de la houille: galets de houille, 200.—P. Marés. Sur la géologie des environs du Keff, Tunisie, 207.—L. Lartet. Sur le terrain carbonifére des Pyrénées cen- trales, 250.—A. Carnot. Sur la composition et les qualités de la houille, eu égard & la nature des plantes qui l’ont formée, 253.—L. Dieulafait. Ori- gine des phosphorites et des argiles ferrugineuses, 259.—L. Crié. Contri- butions 4 la flore pliocéne de Java, 288.—Bréon et Korthals. Sur état actuel du Krakatau, 895.—L. Dieulafait. Nouvelle contribution 4 la ques- tion d’origine des phosphates de chaux du sud-ouest de la France, 440.— C. Mano. Observations géologiques sur le passage des Cordilléres par Visthme de Panama, 573.—A. Favre. Carte du phénoméne erratique et des anciens glaciers du versant nord des Alpes suisses et de la chaine du Mont Blanc, 599.—A. Vivier. Analyse de l’apatite de Logrozan, Espagne, 709.—F. Gonnard. Sur une pegmatite 4 grands cristaux de chlorophyl- lite, des bords du Vizézy, prés de Montbrison, Loire, 711.—A. Gaudry. Nouvelle note sur les reptiles permiens, 737.—L. Dieulafait. Origine et mode de formation des phosphates de chaux en amas dans les terrains sédimentaires ; leur liaison avec les minerais de fer et les argiles des horizons sidérolitiques, 8138.—A. F. Marion. Sur les caractéres d’une Conifére tertiaire, voisine des Dammarées (Dolostrobus Sternbergz), 821. —G. Cotteau. Sur les calcaires a Hchinides de Stramberg, Moravie, 836. —P.de Gasparin. Contribution a l’étude des gites phosphatés dans la région du sud-est de la France, 839.—F. Gonnard. Addition 4 une Note sur une pegmatite a grands cristaux de chlorophyllite des bords du Vizézy, prés de Montbrison (Loire), 881.—Perrotin. Sur un tremblement de terre ressenti 4 Nice le 27 novembre, 960.—G. Lindstrom. Sur un Scorpion du terrain silurien de Suéde, 984.—E. Bureau. Sur la présence de l’étage houiller moyen en Anjou, 1036.—C. Grand’Eury. Fossiles du terrain houiller, trouvés dans le puits de recherche de Lubiére (bassin de Brassac), 1095.—Stan. Meunier. Le kersanton du Croisic, 1135.—F. Gonnard. Sur un phénoméne de cristallogénie, 4 propos de la fluorine de la roche Cornet, prés de Pontgibaud (Puy-de-Dome), 1136.—C. Brone- niart. Sur la découverte d’une empreinte d’insecte dans les grés siluriens de Jurques, Calvados, 1164.—Stan. Meunier. Sur un verre cristallifére des houilléres embrasées de Commentry, 1166. : : Tome c. Nos. 1-24. 1885. E. Hébert. Sur les tremblements de terre du midi de l’Espagne, 24.— B. Renault et R. Zeiller. Sur un Lquisetum du terrain houiller supérieur de Commentry, 71.—J. Macpherson et A. Daubrée. Sur les tremblements de terre de l’ Andalousie du 25 décembre 1884 et semaines suivantes, 136.— A.Germain. Sur quelques-unes des particularités observées dans lesrécents ° tremblements de terre de ’ Espagne, 191.—I. Domeyko. Observations re- cueillies sur les tremblements de terre pendant quarante-six ans de séjour au Chili, 193.—F. de Botella. Observations sur les tremblements de terre de l’Andalousie du 25 décembre 1884 et semaines suivantes, 196.—Da Praia. Secousses de tremblements de terre ressenties aux Acores le 22 décembre 1884, 197.—A. Terreil. Analyse d’une chrysotile (serpentine ——_ ADDITIONS TO THE LIBRARY. 147 fibreuse ayant l’aspect de l’asbeste) ; silice fibreuse résuitant de l’action des acides sur les serpentines, 251.—A. F.Nagués. Phénoménes géologiques produits par les tremblements de terre de l’Andalousie, du 25 décembre 1884 au 16 janvier 1885, 253.—L. Dieulafait. Composition des cendres des Equisetacées: application 4 la formation houillére, 284.—G. Pouchet. Des derniers échouements de Cétacés sur la céte francaise, 286.—F. Laur. Influence des baisses barométriques brusques sur les tremblements de terre et les phénoménes éruptifs, 289.—A. Gaudry. Sur les Hyénes de la grotte de Gargas découvertes par M. Félix Regnault, 325.—H. Gorceix. Sur des sables 4 monazites de Caravellas, province de Bahia, Brésil, 356. —P. Fischer. Sur l’existence de Mollusques pulmonés terrestres dans le terrain permien de Sadne-et-Loire, 593.—J. Macpherson. Tremblements de terre en Espagne, 597.—Delamare. Tremblement de terre ressenti a Landelles, Calvados, le 1 février 1885, 399.—L. Dieulafait. Origine des minerais métalliféres existant autour du plateau central, particuliérement dans les Cévennes, 469.—Vanukoff. Sur les résultats recueillis par M. Sokoloff concernant la formation des dunes 472.—F. Fouqué. Premiéres explorations de la mission chargée de l’étude des récents tremblements de terre de Espagne, 598.—B. Renault et R. Zeiller. Sur des Mousses de Vépoque houillére, 660.—L. Dieulafait. Origine des minerais de fer, de manganése et de zinc, existant autour du plateau central, dans les pre- miers calcaires jurassiques et a la base de ces calcaires, 662.—Stan. Meu- nier. Sur un dépdt de source, provenant de Carmaux, Tarn, 665.—A. Gaudry. La nouvelle galerie de Paléontologie dans le Muséum d’His- toire naturelle, 698.—V. Lemoine. Sur les analogies et les différences du genre Simcedosaure, de Ja faune cernaysienne des environs de Reims, avec le genre Champsosaure d’Erquelinnes, 753.—F. A. Forel. Bruits sous- terrains entendus le 26 aoat 1883 dans Vilot de Caiman-Brac, mer des Caraibes, 755.—L. Dieulafait. Explication de la concentrationdes minerais de zinc carbonaté dans les terrains dolomitiques, 815.—Munier-Chalmas et J. K. Schlumberger. Sur les Miliolidées trématophorées, 818.—B. Renault et R. Zeiller. Sur un nouveau type de Cordaitée, 867.—L. Crié. Con- tribution 4 l’étude des Fougéres éocénes de l’ouest de la France, 870.—J. Martin. Le souléve de la Céte-d’Or est postérieur 4 Vépoque albienne, 872.—L. Vaillant. Remarques complémentaires sur les Tortues gigan- tesques de Madagascar, 874.—Stan. Meunier. Existence du calcaire a Fusulines dans le Morvan, 921.—Faye. Concordance des époques géolo- giques avec les époques cosmogoniques, 926.—L. Dieulafait. Nouvelle contribution a la question de l’acide borique d’origine non volcanique, 1017. —KH. Desté. Forét fossile de Arizona, 1019.—L. Dru. Sur la recherche des sources au voisinage de Gabés, 1020.—F. Fouqué. Explorations de la Mission chargée de l’étude des tremblements de terre de |’Andalousie, 1049.—M. Levy et J. Bergeron. Sur la constitution géologique de la Serrania de Ronda, 1054.—M. Bertrand et W. Kilian. Sur les terrains secondaires et tertiaires de !Andalousie (provinces de Grenade et de Ma- laga), 1057.—C. Barrois et A. Offret. Sur la constitution géologique de la Sierra Nevada, des Alpujarras et de la Sierra de Almjarra, 1060.— C. Grand’Eury.—Sondage de Ricard 4 la Grand’Combe, Gard, 1110.—F. Fouqué. Relations entre les phénoménes présentés par le tremblement de terre de l’Andalousie et la constitution géologique de la région qui ena été le siége, 1113.—R. Zeiller. Détermination, par la flore fossile, de l’age relatif des couches de houille de la Grand’Combe, 1171.—Guillemin- Tarayre. Sur la constitution minéralogique de la Sierra Nevada de Gre- nade, 1251.—B. Renault et C. Eg. Bertrand. Grrilletia spherospermi, Chytridiacée fossile du terrain houiller supérieur, 1306.—De Montessus. Sur les tremblements de terre et les éruptions volcaniques dans l’Amérique centrale, 1315.—Stan. Meunier. Synthése accidentelle de l’anorthite, 148 ADDITIONS TO THE LIBRARY. 1350.—C. Velain. Le pénéen dans la région des Vosges, 1855.—A. Ino- stranzeff. Appareil comparateur pour l'étude des minéraux non trans- parents, 1396.—Stan. Meunier. Sur un silex enhydre du terrain quater- naire de la vallée du Loing (Seine-et-Marne), 1398.—L. Rérolle et C. Depéret. Sur le miocéne supérieur de la Cerdagne, 1399.—F. Fouqué. Propagation de la secousse de tremblement de terre du 25 décembre 1884, 1436.—G. de Saporta. Sur un type végétal nouveau provenant du coral- lien d’Auxey (Cote-d’Or), 1440.—G. Cotteau. Considérations sur les Echinides du terrain jurassique en France, 1515.—A. de Schulten. Re- production artificielle de la strengite, 1522.—J. Macpherson. Symétrie de situation des lambeaux archéens des versants du Guadalquivir: rap- port avec les principales dislocations qui ont donné 4 l’Espagne son relief, 1524. Paris. Annales des Mines. Série 8. Tomeiy. 6° livraison de 1883. 1883. K. Lappierre. Note sur le bassin houiller de Tete, région du Zamhéze, 585.—R. Zeiller. Note sur la flore du bassin houiller de Tete, 594. Tome v. 1° livraison de 1884. 1884. M. Luceyt. " Mémoire sur le bassin houiller du Lancashire, 5. ; —. ; . 2° et 3° livraisons de 1884. 1884. Ternier. Etude sur les éruptions du Hartz, 243.—Kuss. Note sur les filons de quartz aurifére de l’Atajo, province de Catamarca, Ré- publique Argentine, 379.—A. de Bovet. Note sur une exploitation de diamants prés de Diamantina, province de Minas Geyaés, Brésil, 465.— A. Carnot. Sur la composition de la houille, Bulletin, 545. : 5 Tome vi. 4°—6° livraisons de 1884. 1884. Revaux. Etude des travaux exécutés au tunnel de l’Arlberg, 259.— Lariviére. Notes d’un voyage aux ardoisiéres du Pays de Galles, 505. : : -. Tome vii. 1 livraison de 1885. 1885. A. Carnot. Analyses des eaux minérales francaises exécutées au Bureau d’essai de l’Ecole des Mines, 79.—Braconnier. Note sur l’eau minérale sulfatée magnésienne de Cruzy (Hérault), 148—Bulletin des travaux de chimie exécutés en 1883, par les ingénieurs des mines dans les laboratoires départementaux, 145. ——. Annales des Sciences Géologiques. Tome xvi. Nos. 1 & 2. 1884. Purchased. G. Vasseur. Sur le dépét tertiaire de Saint-Palais prés Royan (Cha- rente-Inférieure).—G. Cotteau. Echinides du terrain éocéne de Saint- Palais—F. Fontannes. Note sur quelques gisements nouveaux des terrains miocénes du Portugal et description d’un portunien du genre Achelous—H. Filhol. De la restauration du squelette d’un Dinocerata.— L. Dieulafait. Etude sur les roches ophitiques des Pyrénées.—L. Dollo. Les découvertes de Bernissart. : —. Nos.38&4. 1885. Presented by M. Hébert and M. A, Milne-Edwards. P. Gourret. Constitution géologique du Larzac et des Causses méri- dionaux du Languedoc. ADDITIONS TO THE LIBRARY. 149 Paris. Annales des Sciences Naturelles. Zoologie et Paléontologie. Série 6. Tome xvii. Nos. 1-6. 1884-85. Purchased. G. Lindstro6m. Sur un Scorpion du terrain silurien de Suéde, No. 10. ———. ——. Tome xviii.’ Nos. 1-3. 1884. Pieced é ——. Association Francaise pour l’Avancement des Sciences. - Compte Rendu de la 2° Session, Rouen, 1883. 1884. Pur- chased. R. P. Denza. La Météorite d’Alfianello, 337.—E. Bucaille. Sur la répartition des échinides dans le systéme crétacé du département de la Seine-Inférieure, 429.—J. Clotiet. Etude sur la chaux phosphatée natu- relle de la Seine-Inférieure, 435.—G. Cotteau. Note sur les échinides ter- tiaires des environs de Saint-Palais, 444.—C. Barrois. Recherches sur les terrains anciens des Asturies et de la Galice, 445.—J. J. Amielle. Origine des houilles et des combustibles minéraux, 458.—A. Péron. Sur un groupe de fossiles de la craie supérieure, 461.—P. Petiton. Etude pétrographique des roches de l’Indo-Chine, 470.—A. Le Marchand. Rapport sur les excursions faites par la section de Géologie pendant le Congrés de Rouen, 1883, 481.—A. Guyerdet. Fragments de Géologie Normande, 485. ——. Journal de Conchyliologie. Série 3. Tome xxiv. No. 2. 1884. Purchased. : é : No. 3. 1884. Purchased. EK. Vassel. Description d’une nouvelle espéce de Pecten fossile du Canal de Suez, 331.—Dante Pantanelli. Surle Murex Hornesi, d’ Ancona (non Speyer), 332. SS NO 2 1684. Purchased. ; : . Tome xxv. No.1. 1885. Purchased. L. Morlet. Description de Coquilles fossiles du Bassin Parisien, 48. ——. Muséum d’Histoire Naturelle. Nouvelles Archives. Série 2. Tome vi. Fase. 2. 1884, ——. RevueScientifique. Série3. Tomexxxiii. No. 26. 1884. —. —. —. Tome xxxiy. Nos. 1-26. 1884. —. ——. —. Tome xxxv. Nos. 1-25. 1885. ——. Société Géologique de France. Bulletin. Série3. Tomeix. (1881). No.7. 1884. C. Lory. Course du 4 Septembre, aux carriéres de la Porte de France, aux exploitations de ciment et au plateau de la Bastille, 582.—C. Lory. Course du 5 Septembre, de Grenoble 4 la Grande Chartreuse, 595.—C. Lory. Course du 7 Septembre de Grenoble 4 Sassenage et a |’Kchaillon, 610.—C. Lory. Course du 8 Septembre de Grenoble a Vizelle et au~ Bourg-d’Oisans, 620.—C. Lory. Excursion des 9 et 10 Septembre du Bourg-d’Oisans a la Grave, et retour, 632.—C. Lory. Sur les schistes cristallins des Alpes occidentales et sur le rdle des failles dans la structure géologique de cette région, 652.—E. Hébert. Sur la position des calcaires de l’Hchaillon dans la série secondaire, 683.—J. Gosselet. Comparaison 150 ADDITIONS TO THE LIBRARY. entre l’Ardenne et les Alpes, 689.—C. Lory. Résumé de la course du lundi, 12 Septembre 1881, 696, 701.—H. Kiss. Note sur les filons de fer spathique du canton d’Allevard, 699. Paris. Société Géologique de France. Bulletin. Série 3. Tomex. (1882). No.7. 1884. E. Hébert. Apercu général sur la géologie des environs de Foix, 523. —E. Hébert. Compte-rendu de la course du 18 Septembre 4 Varilhes et Saint-Jean de Verges, 531.—C. de Lacoivier. Compte-rendu de l’excur- ~ sion de Vernajoul 4 Baulon, 538.—C. de Lacoivier. Compte-rendu de l’ex- cursion de Foix a Pradiéres, 543.—E. Hébert. Sur la structure géologique du vallon de Pradiéres, 548.—C. de Lacoivier. Compte-rendu de l’excur- sion de Montgaillard, 551.—E. Hébert. Compte-rendu de l’excursion de Foix 4 Lavelanet, et sur l’étage garumnien, 556.—E. Hébert. Surl’Etage garumnien, 557.—EH. Hébert. Coupe au nord du Moulin d’Illat, sur la route du Carla, 558.—E. Hébert. Coupe de la Cluse de Péreille, 560.— EK. Hébert. Disposition du terrain tertiaire 4 Lavelanet, 565.—C. de Lacoivier. Compte-rendu de l’excursion de Benaix et de Villeneuve- d’Olmes, 570.—E. Hébert. Observations sur la coupe de Villeneuve- d’Olmes 4 Montferrier, et par suite sur la position des Grés de celles dans la série crétacée, 573.—E. Hébert. Succession des couches du terrain crétacé supérieur 4 Saint-Girac, 577.—E. Hébert. Compte-rendu de Vexcursion du 22 Septembre 4 Tarescon et Ussat, 585.—Pouech. Note sur le massif calcaire de Tarascon-Ussat, 588.—C. de Lacoivier. Compte- rendu de l’excursion du samedi, 23 Septembre, a Vicdessos, 600.— E. Hébert. Compte-rendu de l’excursion du mardi, 26 Septembre, de Saint-Girons 4 Saint-Croix, 614.—E. Hébert. Compte-rendu del’excursion du mercredi, 27 Septembre, de Saint-Croix a Audinac, 622.—Pouech. Coupes géo- logiques dans la région N.-O. du département de l’Ariége, 632.—Mayer- Eymar. Note sur les terrains tertiaires de l’Ariége, 637.—H. Hébert. Résumé de la Session, 643.—E. Hébert. Le renversement de Cadarcet et le Gault de Garradoumency, 660.—E. Hébert. Sur la faune de l’étage danien (assises supérieure et moyenne) dans les Pyrénées, 664. : : : . Tome xi. (1883). No.8. 1884. J. Gosselet. Compte-rendu de la course du 2 Septembre aux carriéres a chaux hydraulique de Charleville et 4 la tranchée du moulin Brion, 634.—J. Gosselet. Exposé général de la structure de l’Ardenne, et rap- port des couches primaires avec les terrains secondaires et tertiaires, 636.— A. Renard. Note sur la structure et la composition des phyilades arden- nais, 638.—J. Gosselet. Compte-rendu de la course du 5 Septembre de Charleville 4 Monthermé, 642.—J. Gosselet. Exposé de la structure du terrain déyonien aux environs de Charleville, 646.—J. Gosselet et A. Renard. Compte-rendu de l’excursion du 4 Septembre, de Deville a Revin, 649.—J. Gosselet. _Compte-rendu de la course du 5 Septembre, sur le plateau du Franc-Bois, dans le ravin de lOurs, et a la roche-aux- Corpias, 659.—J. Gosselet. Observations sur le limon des plateaux de l’Ardenne, sur les arkoses métamorphiques du Franc-Bois de Willergie et sur la structure du massif cambrien de la presqu’ile de Rocroi, 662.—J. Gosselet. Géographie de l’Ardenne au commencement de l’époque dévo- nienne, 668.—J. Gosselet. Compte-rendu de la course du 6 Septembre de Fumay 4 Vireux, 673.—J. Gosselet. Compte-rendu de la course du 7 Septembre, de Vireux 4 Givet, et aux environs de Givet, 677.—M. Mour- lon. Sur le grés du Signal d’Asfeld, observé prés de la citadelle de Charlemont, 680.—J. Gosselet. Classification du terrain dévonien de VArdenne, 682.—E. Dupont. Compte-rendu de la course du 8 Septembre, de Mariembourg & Dourbes et 4 Fagnolle, 686.—M. Mourlon. Sur la ADDITIONS TO THE LIBRARY. I51 question des: faciés, 4 propos du classement stratigraphique des dépéts famenniens de la Belgique et du nord de la France, 692.—E. Dupont. Compte-rendu de lexcursion du 10 Septembre de Merlemont 4 Sautour, Neuville, Roly et Matagne, 702.—E. Dupont. Observations sur les cal- caires coralliens du dévonien supérieur, 704.—M. Mourlon. Compte- rendu de l’excursion du 11 Septembre, de Heer a Hastiére, dans le terrain fammenien (dévonien supérieur), 708.—. Dupont et M. Mourlon. Compte-rendu de la seconde partie de l’excursion du 11 Septembre, de Hastiére 4 Waulsor, Freyr et Dinant, 715. Paris. Société Géologique de France. Bulletin. Série 3. Tome xii. (1884). Nos.4-8. 1884. E. Jannettaz, Mémoire sur les clivages des roches (schistosité, lon- grain), et sur leur reproduction, 211.—F. Ameghino. Résumé d’un mé- moire de M. Adolphe Deering sur la Géologie Argentine, 236.—C. Depéret. Nouvelles études sur les ruminants pliocénes et quaternaires d’ Auvergne, 247,—A. de Lapparent. Note sur les roches éruptives de l’ile de Jersey, 284.—E. Fallot. Note sur un gisement crétacé fossilifére des environs de la gare d’Eze (Alpes maritimes), 289.—H. Kiiss. Note sur la constitution géologique d’une partie de la Zambézie, 303.—M. Bertrand. Rapports de structure des Alpes de Glaris et du bassin houiller du Nord, 318.—F. Fon- tannes. Note sur la faune et la classification du “ Groupe d’ Aix,” dans le Gard, la Provence et le Dauphiné, 330.—M.de Raincourt. Note sur des gisements fossiliféres des sables moyens, 343.—E. Haug. Note sur quelques espéces d’Ammonites nouvelles ou peu connues du Lias supérieur, 346.—F. Fontannes. Sur une des causes de la variation dans le temps de faunes malacologiques, 4 propos de la filiation des Pecten restitutensis et latissimus, 357.—P. de Rouville. Note sur le Dévonien de l’Hérault, 364. —R. Zeiller. Sur la dénomination de quelques nouveaux genres de Fou- géres fossiles, 366.—Cossmann. Sur un Mémoire concernant la faune de l’étage bathonien en France, 370.—A. Gaudry. Sur un Sirénien d’espéce nouvelle trouvé dans le bassin de Paris, 372.—I’. Fontannes. Sur un nou- yeau gisement fossilifére des marnes plaisanciennes de Saint-Ariés, situé prés d’Hyguiéres (Bouches du Rhone), 376.—A. Parran. Notice sur les travaux géologiques de Louis Gruner, 380.—D. Céhlert. Etudes sur quelques Brachiopodes dévoniens, 411.—Bleicher. Note sur la limite inférieure du Lias en Lorraine, 442.—F. Fontannes. Note sur la présence des sables & Potamides Basteroti dans la vallée de la Céze (Gard), 447,— M. Bertrand. Failles courbes dans le Jura, et bassins d’affaissement, 452.—F, Fontannes. Note sur la constitution du sous-sol de la Crau, et de la plaine d’Avignon, 463.—L. Dru. Note surla géologie et ’hydrologie de la région de Bechtaou (Russie-Caucase), 474.—J. Marcou. Notes & Voccasion du prochain Congrés géologique international avec des remarques sur les noms des terrains fossiliféres les plus anciens, 517.—J. Bergeron. Note sur les strobilés du Walchia piniformis, 533.—H. Gorceix. Gisement de diamants de Grao-Mogor (province de Minas-Geraés), Brésil, 538,.— Marquis de Raincourt. Note sur la faune de Septeuil, 549.—L. de Sarran d’Allard. Recherches sur les dépéts fluvio-lacustres antérieurs et posté- rieurs aux assises marines de la craie supérieure du département du Gard, 553.—Bourgeat. Note sur la découverte de trois lambeaux nouveaux de cénomanien dans le Jura, 630.—G. Rolland. Résumé des observations de M. T. Kjerulf sur les dislocations de la vallée de Christiania, 637,— Lodin. Note sur la constitution des gites stanniféres de la Villeder (Mor- bihan), 645.—E. de Boury. Observations sur quelques espéces nouvelles du bassin de Paris, décrites par M. le Marquis de Raincourt, 667.—R. Zeiller. Sur des traces d’insectes simulant des empreintes végétales, 676. —R. Zeiller. Note sur la compression de quelques combustibles fossiles, 152 ADDITIONS TO THE LIBRARY. 680.—A. Pavlow. Notions sur le systéme jurassique de |’ Est de la Russie, 686.—A. Tardy. Nouvelles observations sur la Bresse ou de la jonction du Pliocéne et du Quaternaire, 696.—C. Lory. Remarques au sujet des Alpes de Glaris et des allures du terrain €éocéne dans les Alpes, 726.—W. Kilian. Note sur les terrains tertiaires du territoire de Belfort et des en- virons de Montbéliard (Doubs), 729.—A. Locard. Note sur un Cépha- lopode nouveau de la famille des Loliginide, Pleuroteuthis costulatus, 759. —Pouech. Note sur la constitution géologique de Pech de Foix, 765. Paris. Société Géologique de France. Bulletin. Série 3. Tome xiii. (1885). Nos. 1-3. 1885. Davy. A propos d’un nouveau gisement du terrain dévonien supé- rieur a Chaudefonds (Maine-et-Loire), 2.—Zurcher. Note sur la zone a Ammonites Sowerby: dans le S. O. du département du Var, 9.—H. Dou- villé. Sur quelques fossiles de la zone 4 Amm. Sowerbyi des environs de Toulon, 12.—A. Gaudry. Nouvelle note sur les reptiles permiens de la _ Moussage, 44.—A. Gaudry. Sur une dent de Neosodon trouvée dans les sables ferrugineux de Wimille, 51.—Baron de Diicker.: Observations générales sur la géologie de ’Europe, 56.—F. Fontannes. Note sur les alluvions anciennes des environs de Lyon, 59.—E. Fallot. Note sur les étages moyens et supérieurs du Crétacé du sudest de la France, 65.— G. Poirier. Rectification des contours de Vargile plastique sur la feuille géologique de Provins, 68.—G. Poirier. Sur Vallure et la composition de Vargile plastique dans le Montois, 70.—Viguier. Note sur un lehm fossilifére de la vallée de la Sorgue, prés d’A vignon, 79.—De Brignac. Les dépots diluviens dans la vallée du Vidourie, 83.—S. Calderon. Les roches cristallines massives de l’Espagne, 89.—M. Bertrand. Coupes de la chaine de la Sainte-Beaume, Provence, 115.—R. Zeiller. Note sur la flore et sur le niveau relatif des couches houilléres de la Grand’Combe, Gard, 151. —J. Lambert. Présentation d’un travail sur le Jurassique moyen du département de l’Yonne, 153.—F. Delafond. Note sur les sables a Mastodon arvernensis de Tréyoux et de Montmerle (Ain), 161.—Bour- geat. Sur la limite du bajocien et du bathonien dans le Jura; caractéres et degrés de développement que ce dernier présente, 167.—G. de Saporta. Note a l’appui de son mémoire sur les organismes problématiques des anciennes mers, 179.—R. Zeiller. Observations au sujet de la présenta- tion de l’ouvrage de M. de Saporta: “ Les Organismes problématiques des anciennes mers,” 189.—E. Chelot. Rectifications pour servir 4 |’étude de la faune éocéne du bassin de Paris, 191.—V. Lemoine. Etude sur quelques Mammiféres de petite taille de la faune cernaysienne des environs de Reims, 203.—M. Mieg. Note sur un gisement des couches 4 Posido- nomya Bronni & Minversheim (Basse-Alsace), 217. ; Mémoires. Série 3. Tome iii. No. 2. 1884. P. Thomas. Recherches stratigraphiques et paléontologiques sur quel- ques formations d’eau douce de l’ Algérie, 1. Penzance. Royal Geological Society of Cornwall. Transactions. NVoliix, fart 7. gl8so: W. W. Smyth. Presidential Address, cexxii.—A. Somervail and H. Fox. On the Occurrence of Volcanic Tuffs, Breccia, &c. in the Meneage District, 189.—R.N. Worth. The Raised Beaches on Plymouth Hoe, 204. —T. W. Millett. Notes on the Fossil Foraminifera of the St. Erth Clay- pits, 213.—R. J. Frecheville. The Umber Deposits at Ashburton, 216,— C. Le Neve Foster. Note to accompany a Specimen of Native Gold from Leadville, Colorado, 220. ADDITIONS TO THE LIBRARY. 153 Philadelphia. Academy of Natural Sciences. Journal. Ser. 2. Vol.ix. Part1l. 1884. A. Heilprin. The Tertiary Geology of the Eastern and Southern United States, 115. ae Proceedings, 1884. Part 2. 1884. EK. N.S. Ringueberg. New Fossils from the four Groups of the Nia- gara Period of Western New York, 144.—H. C. Lewis. Volcanic Dust from Krakatoa, 185.—J. Willcock. Notes on the Geology and Natural History of the West Coast of Florida, 188.—A. E. Foote. A large Zircon, 214.—F. D. Chester. Preliminary Notes on the Geology of Delaware: Laurentian, Paleeozoic, and Cretaceous Areas, 237. : Part 3. 1885. A. Heilprin. On aremarkable Exposure of Columnar Trap near Orange, New Jersey, 318.—A. Heilprin. Notes on some new Foraminifera from the Nummulitic Formation of Florida, 321. —. ——. ——, 1885. Partl. 1885. G. A. Koenig. A new Locality for Beegerite, 19.—J. Leidy. Rhino- ceros and Hippotherium from Florida, 32.—S. H. Scudder. New Genera and Species of Fossil Cockroaches from the older American Rocks, 34.— J. Leidy. Remarks on Mylodon, 49. ——. American Philosophical Society. Proceedings. Vol. xxi. Nos. 115 & 116. 1884. HK. W. Claypole. On the Clinton and other Shales &c. composing the Fifth Group in the First Survey of Pennsylvania, 492.—E. D. Cope. Synopsis of the Species of Oreodontide, 503.—E. D. Cope. On the Structure of the Skull in the Elasmobranch genus Didymodus, 572.—P. Frazer. Trap Dykes in the Archean Rocks of South-eastern Pennsyl- vania, 691.—F. A. Genth. On Heredite, 694.—C. A. Ashburner. Notes on the Natural Bridge of Virginia, 699. , Photographie Society of Great Britam. Journal and Transactions. N.S. Vol. ix. Nos. 1-9. 1884-85. Physical Society of London. Proceedings. Vol. vi. Parts 2-4, 1884-85, Pisa. Societa Toscana diScienze Naturali. Atti. Memorie. Vol. iv. Fase. 3. 1885. —. ——. ——. Processi Verbali. Vol. iv. (1884). Pp. 73- 146. 1884. G. Meneghini. Nuove specie di Ammoniti dell’ Apennino centrale, 75. —M. Canavari. A proposito di una recente pubblicazione del dott. Wahner sulle ammoniti delle Alpi orientali, 84.—J. Cocchi. Nuovi fos- sili del Vingone in Val di Chiana, 84.—G. Meneghini. Ellipsactinia del Gargano e di Gebel Ersass in Tunisia, 106.—M. Canavari. Brachiopodi retici della Calabria Citeriore, 113. Plymouth. Devonshire Association for the Advancement of Science, Literature, and Art. Report and Transactions. Vol. xvi. 1884. W. Pengelly. The Literature of Kent’s Cavern, Part V., 189.— 154 ADDITIONS TO THE LIBRARY, W. Pengelly. Kent’s Cavern and Glacial or Pre-Glacial Man, 480.—W. Downes. On a newly-discovered Dyke of Mica-trap at Roseash, near Southmolton, 498.—F. Parfitt. On Earthquakes in Devonshire, 640.— W. Pengelly. Notes on Notices of the Geology and Paleontology of Devonshire, 755. Plymouth. Devonshire Association for the Advancement of Science, Literature, and Art. Report and Transactions. Supplement, 1884. The Devonshire Domesday. Part 1. (8vo.) 1884. Plymouth Institution and Devon and Cornwall Natural History Society. Annual Report and Transactions. Vol. viii. Part 3 (1883-84). 1884. Prague. Naturwissenschaftliche Landesdurchforschung von n Bohmen. Archiv. Band iii. Abth.1. 1884. ‘Fan iv. Most: tage: A, Frié. Te Weissenberger und Malnitzer Schichten. 1. » No 2) ) 1879. J. KrejGi und R. Helmhacker. Erlauterungen zur geologischen Karte der Umgebungen von Prag, 1. _.. No. 4. 1882. E. Bot icky. " Petrologische Studien an den Porphyrgesteinen Bohmens, I, Theil, 1. : No. 6. 1881. C. Feistmantel. Der Hangendflétzzug im Schlau-Rakonitzer Stein- kohlenbecken, 1. . Bandy. No.1. 1882. . J. Krej di und R. Helmhacker. Erlauterungen zur geologischen Karte | des Eisengebirges (Zelezné Hory) und der angrenzenden Gegenden im dstlichen Bohmen, 1. No. 2. 1883. A. Frit, Die Iserschichten, at: : : ANo! Ss) A883: ©. Feistmantel. Die mittelbdhmische Steinkohlen-A blagerung, 1. — a Princeton, N. J. E. M. Museum of Geology and Archeology. Third Annual Report, 1884. 1884. (8vo.) Quekett Microscopical Club. Journal. Ser. 2. Vol. u. No. 9. 1884. —. 1+—.. —. —. No. 10. 1884. —. ——. —-. —. No. 12. 1885. Rio de Janeiro (Ouro Preto). Escola de Minas de Ouro Preto. Annaes. No.3. 1884. H. Gorceix. Lund e suas obras no Brazil, 9—P. W. Lund. Cavernas existentes no calcareo do interior do Brazil, contendo algumas dellas os- sadas fosseis, 59.—H. Gorceix. Bacias terciarias d’ague doce nos arre- ADDITIONS TO THE LIBRARY. 155 dores de Ouro Preto (Gandarela e Fonseca), Minas Geraes, Brazil, 95.— H. Gorceix. Noticia relativa a alguns mineraes dos cascalhos diamanti- feros contendo acido phosphorico, alumina e outras terras da familia do cerium, 197.—H. Gorceix. Noticia relativa a um zeolitho de uma rocha eae da bacia do Abaeté, Minas Geraes, 205.—J. C. da Costa-Sena. oticia sobre a Seorodita existente nas visinhangas do Arraial de Antonio Pereira e sobre a Hydrargillita dos arredores de Ouro Preto, 211.—H. Gorceix. Estudo dos mineraes que accompanhio o diamante na jazida de Solobro, provincia da Bahia, Brazil, 219. Rome. Reale Accademia dei Lincei. Atti. Serie 3. Memorie. Vol. xiv. (1882-83). 1883. J. Cafici. La formazione miocenica nel territorio di Licodio-Eubea, 59.—E. Mattirolo. Su tre roccie di San Piero in Campo (Isola d’ Elba), 173.—L. Bombicci. Sull’ aerolito caduto presso Alfianello e Verolanuova (provincia di Brescia); sulla causa delle detonazioni che accompagnano la caduta dei bolidi; et sulla costante presenza del ferro nelle meteoriti, 675. ‘ . . Vol. xv. (1882-83). 1883. G. Spezia. Osservazioni sulla melanoflagite, 300.—C. de Stefani. Os- servazioni stratigrafiche sui dintorni di Serravezza, 467.—A. Verrie C. F. Parona. I. Studi geologici sulle conche di Terni e di Rieti. II. Con- tributo allo studio della fauna lassica dell’ Appenino centrale, 565. — #—. —. —. —. Vol. xvi. (1882-83). 1883. —. s—. ——. —. —. Vol. xvii. (1883-84). 1884. —._ «—. —-. ——. Transunti. Vol. viii. Fasc. 11-16. 1884. A. Cossa e G. La Valle. Sopra un silicato basico idrato di barite, 299. —. —. —. Serie 4. Rendiconti. Vol.i. Fasc. 1-12. 1884, . G. Capellini. Del Zifiode fossile (Chenoziphius planirostris) scoperto nelle sabbie plioceniche di Fangonero presso Siena, 6.—G. Striiver. Sulla columbite di Cravezzia in Val Vigezzo, 8.—G. Capellini. Resti fossili di Dioplodon e Mesoplodon raccolti nel Terziario superiore in Italia, 171.— G. Striiver. Contribuzione alla mineralogia dei vulcani sabatini: Parte I. Sui proietti minerali vulcanici trovati ad est del lago di Bracciano, 173. —G, Ponzi. Conglomerato del Tavolato; trivellazione del fortino sulla via Appia presso la tomba di Cecilia Metalla. Storia dei vulcani laziali, accresciuta e corretta, 319. ——. Reale Comitato Geologico d’ Italia. Bollettino. Anno xv. (1884). 1884. L. Mazzuoli ed A. Issel. Nota sulla zona di coincidenza delle forma- zioni ofiolitiche eocenica e triasica della Liguria occidentale, 2.—A. Issel. Della existenza di una zona ofiolitica terziaria a Rivara Canavese, 23.— A. Negri. Le valli del Leogra, di Posina, di Laghi e dell’ Astico, nel Vicentino, 33, 81—B. Lotti. Osservazioni geologiche sulle isole dell’ Arcipelago toscano, 56.—H. Forstner. Sunto di uno studio sui feldi- spati di Pantellaria, 61.—B. Lotti. Considerazioni sulla eta e sulla ori- gine dei graniti toscani, 115.—G. B. Rocco. Appunti di una escursione I 56 ADDITIONS TO THE LIBRARY. mineraria in Toscana, 129.—Quintino Sella: necrologia, 139.—S. Speciale. Le Isole Pelagie, 161.—D. Zaccagna. Sulla costituzione geologica delle Alpi marittime, 167.—F. Coppi. Il Miocene medio nei colli modenesi; appendice alla Paleontologia modenese, 171.—E. Cortese e M. Canavari. Nuovi appunti geologici sul Gargano, 225, 288.—L. Bucca. Sopra alcune roccie della serie cristallina di Calabria, 240.—-A. Bittner. Note geolo- giche sul trias di Recoaro, 249.—Ferdinando vy. Hochstetter: Necrologia, 288.—D. Lovisato. Nota sopra il permiano ed il triasico della Nurra in Sardegna, 305.—G. Vom Rath. Escursioni geologiche in Corsica e Sardegna, 325.—K. Dalmer. Sulle condizioni geologiche dell’ isola @ Elba, 329.—L. Baldacci e M. Canavari. Le regione centrale del Gran Sasso d’ Italia, 345.—B. Lotti. La miniera cuprifera di Montecatini (Val di Cecina) e i suoi dintorni, 359.—L. Mazzuoli. Nota sulle formazioni ofiolitiche delle valle de Penna nell’ Appennino ligure, 394. Royal Agricultural Society of England. Journal. Ser. 2. Vol. xx. Part 2. No. 40. 1884. hs Bt EE eee ear Pale NeoPa ees Royal Asiatic Society of Great Britain and Ireland. Journal. N.S. Vol. xvi. Part 4. 1884. —. 1—«——. —. Vol. xvu. Parts1&2. 1885. Royal Astronomical Society. Memoirs. Vol. xlvui. Part 1. 1884. Royal College of Surgeons. Calendar, 1884. 1884. Royal Geographical Society. Proceedings. Vol. vi. Nos. 7-12. 1884. C. M. Doughty. Travels in North-western Arabia and Nejd, 382. a a Vol va. Nos: 1-6. 2 as. Royal Institution of Great Britain. Proceedings. Vol. x. Part 3. Now f7.7; 1884; : ¢: Nol as" Pant ion No fo. 2 loos: T. G. Bonney. The Building of the Alps, 53.—J. W. Judd. Kraka- toa, 895. z Royal Meteorological Society. Quarterly Journal, 1884. Vol. x. Nos. 50-52. 1884. ——. ——, 1885. Vol. xi. Nos. 53 & 54. 1885. Royal Microscopical Society. Journal. Ser. 2. Vol. iv. Parts 4-6. 1884. : - Vol. v. Parts1 &2. 1885. E. Wethered. On the Structure and Origin of Carboniferous Coal- seams, 406, ADDITIONS TO THE LIBRARY. 157 Royal Society. Philosophical Transactions. Vol. clxxiv. Part 3. 1884. : . Vol. clxxv. Part1l. 1884. R. Owen. Description of Teeth of a large Extinct (Marsupial ?) genus Sceparnodon, Ramsay, 245.—R. Owen. Evidence of a large Extinct Lizard (Notiosaurus dentatus, Owen) from Pleistocene Deposits, New South Wales, Australia, 249.—R. Owen. Evidence of a large Extinct Monotreme (Echidna Ramsay, Owen), from the Wellington Breccia Cave, New South Wales, 273. —. Proceedings. Vol. xxxvi. No. 231. 1884. T. G. Bonney. Notes on the Microscopic Structure of some Rocks from the Andes of Ecuador, collected by Edward Whymper: No. I. Anti- sana, 426. —-. . Vol. xxxvii. Nos. 232 & 234. 1884. T. G. Bonney. Notes on the Microscopic Structure of some Rocks from the Andes of Ecuador, collected by E. Whymper: No. III. Cotopaxi and Chimborazo, 114.—T.G. Bonney. Notes on the Structure of some Rocks fromthe Andes of Ecuador, collected byE. Whymper: No.IV.Carihuairazo, Cayambe, and Corazon, 131.—T. G. Bonney. Notes on the Microscopic Structure of some Rocks from the Andes of Ecuador, collected by E. Whymper: No. V. Conclusion: Altar, Ulinizar, Sinchologua, Cato- cachi, Sara-urcu, &c., 394. ; . Vol. xxxvii. Nos. 235 & 236. 1885. J.S. Gardner. On the Evidence of Fossil Plants regarding the Age of the Tertiary Basalts of the North-east Atlantic, 14—Coutts Trotter. On some Physical Properties of Ice and on the Motion of Glaciers, with special reference to the late Canon Moseley’s Objections to Gravitation- Theories, 92.—J. Prestwich. On Underground Temperatures, with Obser- vations on the Conductivity of Rocks, on the Thermal Effects of Satura- tion and Imbibition, and on a special Source of Heat in Mountain Ranges, 161.—Obituary Notices: Robert Alfred Cloyne Godwin-Austen, iv; John Gwyn Jeffreys, xiv. Rugby School Natural History Society. Report for the year 1884. 1885. St. Louis. Museum of the University of the State of Missouri (Columbia, Mo.). Bulletin. Vol.i. No.1. 1884. (8vo.) J. W. Spencer. Niagara Fossils, 1. St. Petersburg. Académie Impériale des Sciences. Bulletin. Tome xxix. Nos.3 & 4. 1884. =SS=: Zo lome xxx. Nos... 1885. —. ——. Mémoires. Série 7. Tome xxxi. Nos. 15 & 16. 1883. : P. W. Jermejew. Russische Caledonit- und Linarit-Krystalle, No. 15, : . : . Tome xxxil. Nos. 1-13. 1884. A. Karpinsky. Die fossilen Pteropoden am Ostabhange des Urals, No. 1.—S. Nikitin. Die Fluss-Thaler des mittleren Russlands, No. 5. 158 ADDITIONS TO THE LIBRARY. Salem. Peabody Academy of Science. Annual Reports of the Trustees, 1874-84. 1885. San Francisco. Californian Academy of Sciences. Bulletin. Nos. 2 & 3 (1885). 1885. A. W. Jackson. On the Morphclogy of Colemanite, 3—J. T. Evans. The Chemical Properties and Relations of Colemanite, 37. Sanitary Institute of Great Britain. Transactions. Vol. v. (1883- 84). 1884. W. Eassie. The Relationship between Geology and Sanitation, 21. Society of Arts. Journal. Nos. 1649-1675. 1884. —. ——. Nos. 1676-1700. 1885. _——. ——. Index to Volumes xxi.—xxx. (1871-82). 1884. | Society of Biblical Archeology. Proceedings. Vol. iv. (1883-84). 1884. | Stockholm. Geologiska Forening. Forhandlingar. Bandet vii. Haft. 5-11. 1884-85. A. W. Cronquist. Om nagra forvittringsprodukter i Granrotsgrufvan af Klackbergsfaltet i Norbergs bergslag, 244.—A. W. Cronquist. Nagra ord om orsaken till qvartstegels svallning, 255.—A. W. Cronquist. Ce- mentskiffern fran Styggforsen i Boda socken af Kopparbergs lan, 260.— M. Weibull. Mineralogiska notiser 1-8, 263.—A. Sjogren. Om Kata- pleiitens kemiska sammansattning och konstitution, 269.—G. Nordenstrom. NGgra erinringar om 4sigterna 1 aldre tider rérande vara malmers fore- komstsitt, 276.—G. C. v. Schmalensee. Om lepteenakalken plats i den siluriska lagerserien, 280.—W. Lindgren. Annu nagra ord om Berzeli- iten, 291.—E. Svedmark. Om nagra svenska skapolitforande bergarter, 293.—S. L. Tornquist. Till sporsmalet om lepteenakalkensalder, med an- ledning af G. C. v. Schmalensées bestémning af densamma, 304.—A. G. Hogbom. En modifikation af Wredes afvagningsinstrument, 328.—H. vy. Post. Om sodahaltigt vatten frén borrhalet n:o0 3 vid Bjuf, 331.—F. Eichstidt. Muikroskopisk undersdkning af olivinstenar och serpentiner fran Norrland, 333.—H. Sjogren. Kristallografiska studier, 369.—P. Gu- melius. Ett par iakttagelser om inlandsisens verkan p& underliggande berget, 389.—L. J. Igelstrom. En for norden ovanlig blyglansbildning, 393.—H. Sjogren. Om manganarseniaternas fran Nordmarken forekomst- satt och paragenesis, 407.—W. C. Brogger. Om en ny konstruktion af et isolations-apparat for petrografiske undersdgelser, 417.—W. C. Brog- ger. Om Katapleitans tvillglove, 427.—L. J.Igelstrém. Kristalliserad albit och titanit fran St. Morkhultsgrufvan i Filipstads bergslag; Igel- strémit fran Knipgrufvan, Ludvika socken, St. Kopparbergs lin, 434.— G. de Geer. Om den skandinaviska landisens andra utbredning, 436.— G. de Geer. Om Actinocamazx quadratus, Bly., i nordéstra Skane, 478.— S. L. Térnquist. Genmale p& M. Stopes uppsatts “Om Dalarnes sand- stenar IT.,” 480.—O. Gumeelius. jon hjelmarens forna vattenhojd, 488. —O. Gumelius. Samling af underrattelsar om jordstotar 1 Sverige, 500. —A.E. Tormebohm. Om de geologiska svaérigheterna kring riksegrinsen, 501.—H. Sjogren. Om jernmalmerna vid Moravicza och Dognacska 1 Banatet, 514.—A. G. Nathorst. Nagra ord om slipsandstenen i Dalarne, ADDITIONS TO THE LIBRARY. 159 537.—A. E. Tornebohm. Om de geologiska forh@llandena i trakten kring Atvidaberg och Bersbo, 562.—W. C. Brégger. Forelébig meddelelse om to nye norske mineraler, Lavenit og Cappelenit, 598.—G. Nordenstrom. Preliminart meddlande om jordbafningarna i Spanien i December 1884, 600.—L. J. Igelstrém. Manganoxidul-arseniater frin Langvik, Gry- thytte socken, Orebro lan, 609.—F. Eichstiidt. Om qvartsit-diabaskon- glomeratet frén bladen “ Nydala,” “ Vexio,” och “ Karlshamn,” 610.—F, Svenonius. Nagra profiler inom mellersta Skandinaviens skifferomrade, 631. Stuttgart. Neues Jahrbuch fir Mineralogie, Geologie und Palion- tologie, 1884. Band ii. Heft 3. 1884. P. Scharizer. Die basaltische Hornblende yon Jan Mayen nebst Be- merkungen iiber die Constitution der thonerdehaltenden Amphibole, 143. —C. Rammelsberg. Ueber den Boronatrocalcit und die natiirlichen Borate iiberhaupt, 158.—F. Rinne. Beitrage zur Kenntniss des Krystall- systems des Zinkoxyds (Zinkits, Rothzinkerzes),164.—P. Mann. Unter- suchungen iiber die chemische Zusammensetzung einiger Augite aus Phonolithen und verwandten Gesteinen, 172.—P. Jannasch. Ueber die Bestimmung des aus Mineralen durch Trockenmittel abscheidbaren Wassers, speciell bei Heulandit und Hpistilbit, 206.—H. Fischer. Ueber Nephritbeile aus Brasilien und Venezuela, 214.—C. Dilter. Erhit- zungsversuche an Vesuyian, Apatit, Tourmalin, 217—H. Sommerlad. Leucit- und Nephelinbasalt aus dem Vogelsberg, 221.—S. L. Penfield. Ueber Erwarmungsversuche an Leucit und anderen Mineralien, 224,—L. v. Werveke. Rutil in Diabascontactproducten—Durch Diabas veranderte Schiefer im Gebiet der Saar und Mosel, 225, —-. , 1885. Bandi. Hefte 1-3. 1885. B. Kolenko. Mikroskopische Untersuchung einiger Eruptivgesteine von der Banks-Halbinsel, Neu-Seeland, 1.—A. Streng. Ueber einige mikro- skopisch-chemische Reaktionen, 21—C. Délter. Ueber die Abhangig- keit der optischen Eigenschaften von der chemischen Zusammensetzung beim Pyroxen, 43.—J. TE. Wolff. Nephelingesteine in den Vereinigten Staaten, 69.—M. von Miklucho-Maclay. Beobachtungen an einigen Schiefern von dem Berge Poroschnaja bei Nischne-Tagilsk im Ural, 69.— A. G. Nathorst. Ueber die Beziehungen der islandischen Gletscherabla- gerungen zum norddeutschen Diluvialsand und Diluvialthon, 74.—T. Liebisch. Ueber eine Goniometervorrichtung, welche zur Messung zer- setzbarer Krystalle dient, 76.—G. Vom Rath. Ueber Colemanit, 77.—M. Websky. Ueber die EKin- und Mehrdeutigkeit der Fundamental-Bogen- Complexe fiir die Elemente monoklinischer Crystall-Gattungen, 79.—P. Jannasch. Ueber den Wassergehalt des Klinochlors vonsder Mussa Alpe, 92.—R. Brauns. Einige Beobachtungen und Bemerkungen zur Beurtheilung optisch anomaler Krystalle, 96.—W. Voigt. LExiirung der Farbenerscheinungen pleochroitischer Krystalle, 119.—G. Greim. Ueber den Diluvialsand von Darmstadt, 142.—M. Neumayr und A. Bittner. Das Schiefergebirg bei Athen, 151.—A. Weisbach.—Ueber Herderit, 154.— H. Trautschold. Ueber Trematina foveolata, 155.—J. v. Siemiradzki. Hypersthenandesit aus W. Ecuador, 155.—G. Vom Rath. Ueber das Gangrevier von Butte, Montana, 158.—F.Sandberger. Borsauregehalt des Glimmers; Mangangehalt eines Apatits, 171.—C. Winkler.—Ueber Her- derit, 172.—A. Streng. Erwiderung [in reference to a paper by A. Wichmann], 174.—E.Cohen. Das labradoritfiihrende Gestein der Kiiste von Labrador, 183.—F. Sandberger. Fairfieldit von Rabenstein. Pseu- domorphosen von Quartz und Albit nach Kalkspath, 185.—J. Graul. Die tertiaren Ablagerungen des Sollings, 187.—K. Obbeke. Ueber das Ge- VOL. XLI. Pp 160 ADDITIONS TO THE LIBRARY. stein vom Tacoma-Berg, Washington Territory, 222.—L. v. Werveke. Ueber Ottrelithgesteine von Ottré und Viel-Salm, 227.—E. Briickner. Ueber die Vergletscherung Ost-Sibiriens, 236.—A. Streng. Diopsid von Zermatt, 238.—A. Kenngott. Nephrit von Jordansmiihl in Schlesien; Magnetismus des Tigerauges; Topas von Ouro Preto, 239.—E. Cohen. Berichtigung beziiglich des “Olivin-Diallag-Gesteins” von Schriesheim im Odenwald, 242.—R. D. M. Verbeek. ‘Ueber Pyroxen-Andesite des Niederlandisch-Indischen Archipels, 243.——. Krakatau, 244.—T. Lie- bisch. Ueber die Totalreflexion an optisch einaxigen Krystallen, 245. Stuttgart. Neues Jahrbuch fiir Mineralogie, Geologie und Paliaon- tologie, 1885. Beilage-Band ii. Heft 2. 1884. H.W.Benecke. Erlauterungen zu einer geologischen Karte des Grigna- Gebirges, 171.—A. Merian. Studien an gesteinsbildenden Pyroxenen, 252.—J. M. Clarke. Die Fauna des Iberger Kalkes, 316.—H. Traube. Ueber die Nephrit von Jordansmiihl in Schlesien, 412. : 5 ~ Heft-3. . 1885, W. Deecke. Beitrige zur Kenntniss der Raibler Schichten der Lom- bardischen Alpen, 429.—C. Klein. Mineralogische Mittheilungen XL., 522.—K. Haug. Beitrage zu einer Monographie der Ammonitengattung Harpoceras, 585. Swansea. South-Wales Institute of Engineers. Proceedings. Vol. xiii. No. 7. 1884. : ; . Vol. xiv. Nos. 1-3. 1884. W. M. Vivian. Notes on a Deposit of Iron Ore at Marbella, Province of Malaga, Spain, 48.—J. Clarke Hawkshaw. The Severn Tunnel Rail- way, 121.—S. Vivian. The Hematite Deposits of the Southern Outcrop of the Carboniferous Limestone of South Wales, 164. Sydney. Linnean Society of New South Wales. Proceedings. Vol. ix. Parts 1-4 (1884). 1884-85. J. Milne-Curran. On some Fossil Plants from Dubbo, N.S. W., 250.— R. v. Lendenfeld. The Eruption in the Straits Settlements and the Even- ing Glow, 438.—R. von Lendenfeld. The Time of the Glacial Period in New Zealand, 806.—N. de Miklouho-Maclay. On Volcanic Activity on the Islands near the North-east Coast of New Guinea, and Evidence of Rising of the Malay Coast in New Guinea, 963.—J. Brazier. List of recent Shells found in Clay on the Maclay Coast, New Guinea, 988.—J. E. Tenison-Woods. The Geology and Physical Geography of the State of Perak, 1175. —. Royal Society of New South Wales. Journal and Proceedings for 1883. Vol. xvii. 1884. J.E. Tenison-Woods. On the Waianamatta Shales, 75.—R. Etheridge, jun. Further Remarks on Australian Strophalosie, and Description of a new Species of Aucella from the Cretaceous Rocks of North-east Aus- tralia, 87. Tokio. Seismological Society of Japan. Transactions. Vol. vii. Part 1 (1883-84). 1884. John Milne. Earth Tremors, 1—F.du Bois. The Earthquakes of Ischia, 16.—Catalogue of Earthquakes felt in Tokio between July 1883 and May 1884, 43. _ ADDITIONS TO THE LIBRARY. 161 Tokio. Seismological Society of Japan. Transactions. Vol. vii. Part 2. 1884. J. Milne. On 387 Earthquakes observed during two years in North Japan, 1. ——. Tokid Daigaku Peaarerethy Appendix to Memoir No. 9. 2544 (1884). (4to.) Toulouse. Socicté d'Histoire Naturelle. Bulletin. 17° Année. 1883. E. Trutat. Excursion au Pic du Gar, prés Saint-Béat (Haute Garonne), 18.—De Rey-Pailhade. Excursion au bassin houiller de Carmaux, 129.— Regnault. La Grotte de Gargas, 257.—Boule. Compte-rendu d’une dé- couverte faite par M. Cartailhac d’un carriére préhistorique de Silex, 258. ——. : . 18° Année. 1884. J. Nery Delgado. Note sur les échantillons de Bilobites envoyés 4 VExposition géographique de Toulouse, 126, Turin. Osservatorio della Regia Universita. Bollettino. Anno xviii. (1883). 1884. ——. Reale Accademia delle Scienze. Atti. Vol.xix. Disp. 4-7. 1884. A. Cossa. Communicazione intorno ad un’ Idocrasia della Valle di Susa, 539.—G. Piolti. Il porfido del Vallone di Robureut, 571.—F. Sacco. L/alta Valle Padana durante I’ epoca delle terrazze in relazione col contemporaneo sollevamento della circostante catena Alpino-Apen- ninica, 795.—E. Mattirolo ed E. Monaco. Sulla composizione di un dial- lagio proveniento dal distritto di Syssert (Monti Ural), 826. —-. Vol. xx. Disp. 1-5 (1884-85). 1885. F. Sacco. Sul’ origine delle vallate e dei alpini in rapporto coi solleva- menti delle Alpi e coi terreni pliocenici e quaternari della Valle Padana, 639.—F. Sacco. Sopra alcuni fenomeni stratigrafici osservati nei ter- reni pliocenici dell’ alta Valle Padana, 664. —, ——. Matias! Serie 2. Tomoxxxvi. 1885. University College. Calendar, 1884-85. 1884. Victoria Institute. Journal of the Transactions. Vol. xvii. No. 70. 1884. ——. : . Nos. 71-73. 1884-85. J. M. Mello. The Prehistoric History of Flint Implements at Spiennes, 253.—S. R. Pattison. The Evolution of the Pearly Nautilus, 270. Vienna. Beitrage zur Palaontologie Oesterreich-Ungarns und des Orients. Bandiv. Hefte1 & 2. 1884. Purchased. J. Velenovsky. Die Flora der bohmischen Kreideformation, 1.—K. A. Penecke. Beitriige zur Kenntniss der Fauna der slavonischen Palu- dinenschichten, 15.—F. Teller. Neue Anthracotherienreste aus Siidsteier- mark und Dalmatien, 45, —. . Bandy. Heft 1. 1885. Purchased. J. Velenovshy. Die Flora der bohmischen Kreideformation, 1. p2 162 ADDITIONS TO THE LIBRARY. Vienna. Kaiserliche Akademie der Wissenschaften. Anzeiger, 1884. Nos. 9-28. 1884. F. Toula. Uebersicht tiber die Reiserouten und die wichtigsten Re- sultate der Reise [Centrale Balkan], 197.—F. Toula. Ueber Amphicyon, Hyemoschus, und Rhinoceros (Aceratherium) von Goriach bei Ternau in Steiermark, 244. ae : , , 1885. Nos. 1-12. 1885. M.Neumayr. Ueber die geographische Verbreitung der Juraformation, 45,—F. v. Hauer. Die Fauna der Juraablagerung von Holmstein in Sachsen, 51.—F.v. Hauer. Ein Beitrag zur Kenntniss der Fische der bohmischen Turons, 85.—E. Stiss. Ueber die Kenntniss der Structur des Libanon und des Anti-Libanon, 104. ; . Denkschriften. Mathematisch-Naturwissenschaft- liche Classe. Band xlvi. 1883. C. von Ettingshausen. Beitrage zur Kenntniss der Tertiarflora Austra- liens, 101.—M. Neumayr. Ueber klimatische Zonen wahrend der Jura- und Kreidezeit, 277. ————— : Sitzungsberichte. Band Ixxxyiii. Abth.1. Hefte 1-5 (1883). 1883-84. F. Wahner. Das Erdbeben von Agram am 9 November 1880, 15.— G. Tschermak. Beitrag zur Classification der Meteoriten, 347.—C. v. EKttingshausen. Zur Tertiarflora von Borneo, 372.—M. Neumayr. Zur Morphologie des Bivalvenschlosses, 385.—H. Foullon. Ueber die Mine- ralogische und chemische Zusammensetzung des am 16 Februar 1883 bei Alfianello gefallenen Meteorsteines, 433.—A. Bittner. Micropsis vero- mensis, ein neuer Echinide des oberitalienischen LEKocans, 444.—L. Teisseyre. Hin Beitrag zur Kenntniss der Cephalopodenfauna der Orna- tenthone im Gouvernement Rjasan, 538.—D. Stur. Zur Morphologie und Systematik der Culm- und Carbonfarne, 633.—C. v. Ettingshausen. Zur Tertiarflora Japans, 851.—J. N. Woldrich. Diluviale Fauna von Zuzla-— witz bei Winterberg im Bohmerwalde, 978.—J. Blaas. Ueber Romerit, Botryogen und natiirlichen Magnesia-Hisenvitriol, 1121.—G. Tschermak. Die Skapolithreihe, 1142.—F. Toula. Geologische Untersuchungen im westlichen Theile des Balkan und in den angrenzenden Gebieten, 1279.— V. Hilber. Recente und im Loss gefundene Landschnecken aus China, 1349. —. —. ——. Bandlxxxix. Hefte 1-5(1834). 1884. —=. Kaiserlich-Konigliche Bergakademien zu Leoben und P7i- bram und die K oniglich-Ungarische Bergakademie zu Schemnitz. Berg- und Hittenmannisches Jahrbuch. Band xxxu. Hefte 2-4, 1884. : : Band xxxii. Hefte 1&2. 1885. C. Blomeke. Ueber die Erzlagerstatten des Harzes und die Geschichte des auf demselben gefitihrten Bergbaues, 1. —. Kaiserlich-Konigliche Geologische Reichsanstalt. Abhand- lungen. Band xi. Abth.1. 1885. D. Steir. Die Carbon-Flora der Schatzlarer Schichten: Abth. 1. Die Farne der Carbon-Flora der Schatzlarer Schichten, 1. ADDITIONS TO THE LIBRARY. 163 Vienna. Kaiserlich-Kénigliche Geologische Reichsanstalt. Jahr- buch. Band xxxiv. Hefte3& 4. 1884. F. Toula. Ueber einige Siiugethierreste yon Gériach bei Turnau, in Steiermark, 385.—F. Bassani. Ueber zwei Fische aus der Kreide des Monte 8. Agata im Gorzischen, 403.—C. v. Camerlander. Geolo- gische Mittheilungen aus Central-Mihren, 407.—A. Bittner. Die Ter- tiar-A blagerungen von Trifail und Sagor, 433.—F. v. Hauer. Zur Erinne- rung an Ferdinand v. Hochstetter, 601—M. Vacek. Beitrag zur Geo- logie der Radstidter Tauern, 609.—H. Foullon. Ueber die petrogra- ee Beschaffenheit krystallinischer Schiefergesteine aus Radstadter auern und deren westlichen Fortsetzung, 635.—C. Diener. Ein Beitrag zur Geologie des Centralstockes der julischen Alpen, 659:—R. Scharizer. Ueber Mineralien und Gesteine von Jan Mayen, 707.—G. Di Stefano. Ueber die Brachiopoden des Unteroolithes von Monte San Giuliano bei Trapani, Sicilien, 729.—J. Wagner. Ueber die Wirmeverhiltnisse in der Osthalfte des Arlbergtunnels, 743.—-Fr. v. Hauer. Erze und Mine- ralien aus Bosnien, 751. . ——. Verhandlungen, 1884. Nos.10-17. 1884. V. Uhlig. Ueber Jura-Fossilien aus Serbien, 178.— A. Rzehak. Con- chylien aus dem Kalktuff von Radziechow in Westgalizien, 185.—D. Stur. Todes-Anzeige: Heinrich Robert Goppert, 189.—N. Andrussow. Ueber das Auftreten der marin-mediterranen Schichten in der Krim, 190. —G. C. Laube. Glacialspuren im bohmischen Erzgebirge, 194.—E. Drasche. Chemische Analysen einiger persischer Eruptivgesteine, 196. —V. Uhlig. Diluvialbildungen bei Bukowna am Dniester, 198.—V. Uhlig. Zur Ammonitenfauna der Baliner Oolithe, 201.—A. Bittner. Neue Hinsendungen tertidrer Gesteinssuiten aus Bosnien, 202.—H. Lech- leitner. Notizen uber den Gebirgsstock des Sonnenwendjoches im Unter- Innthale, Tirol, 204.—A. Rzehak. Conchylien aus dem Kalktuff von Rossrein bei Lettowitz in Mahren, 208.—T. Posewitz. Geologischer Aus- flug in das Tanahlaut, Stid-Borneo, 237.-E. Hussak. Mineralogische und petrographische Notizen aus Steiermark, 244.—F. Herbich. Schiefer- kohlen bei Frek in Siebenbiirgen, 248.—R. Zuber. Neue Inoceramen- funde in den ostgalizischen Karpathen, 251.—F. Bieniasz und R. Zuber. Notiz tiber die Natur und das relative Alter des Eruptivgesteines von Zalas im Krakauer Gebiete, 252.—E. Reyer. Reiseskizzen aus Califor- nien, 256,—Fr. v. Hauer. Cephalopoden des unteren Trias vom Han Bulog an der Miliaka, O.S.0. von Sarajewo, 217.—F. Toula. Ueber die ' Tertiarablagerungen bei St. Veit an der Triesting und das Auftreten von Cerithium lignitarum, Hichw., 219.—-H. Keller. Funde im Wiener- und Karparthen-Sandstein, 233.—A. Bittner. Geologische Verhaltnisse der Umgebung von Gross-Reifling a. d. Enns, 260.—V. Uhlig. Ueber den penninischen Klippenzug und seine Randzonen, 263.—H. Foullon. Ueber gediegen Tellur von Faczebaja, 269.—M. Lomnicki. Vorlaufige Notiz uber die altesten tertiiren Siisswasser- und Meeresablagerungen in Ost- galizien, 275.—J. Blass. Ueber eine neue Belegstelle fiir ene wieder- holte Vergletscherung der Alpen, 278.—H. Pohlig. Geologische Unter- suchungen in Persien, 281.—H. Tietze. Ueber ein Kohlenvorkommen bei Cajutz in der Moldau, 284.—K. Tietze. Das Eruptivgestein von Zalas im Krakauer Gebiete, 289.—V. Uhlig. Reisebericht aus Westga- lizien. Ueber ein neues Miocinvorkommen bei Sandec inmitten der westgalizischen Sandsteinzone, 292.—C. v. Camerlander. Aufnahmen in Schlesien, 294—V. Bieber. Ein Dinotherium-Skelet aus dem EKger- Franzensbader Tertiarbecken, 299.—R. Hornes. Ein Vorkommen des Pecten denudatus, Reuss, und anderer “ Schlier”-Petrefacte im inneral- 164 ADDITIONS TO THE LIBRARY. pinen Theil des Wiener Beckens, 305.—M. Staub. Die Schieferkohlen bei Frek in Siebenbiirgen, 306—H. Commenda. Riesentipfe bei Stey- rego in Oberdsterreich, 308.—A. Bittner. Valenciennesienschichten aus Rumanien, 311.—F. Teller. Notizen tiber das Tertiar yon Stein in Krain, 313.—V. Uhlig. III. Reisebericht aus Westgalizien, iiber die Umgebung von Rzegacina bei Bochnia, 318.—C. v. Camerlander. I. Reisebericht aus Oesterr.-Schlesien, 321.—F. v. Hauer. Erze und Mine- ralien aus Bosnien, 331.—C. Diener. Mittheilung iiber den geologischen Bau des Centralstockes der julischen Alpen, 33].—H. Foullon. Ueber die Warmeverhaltnisse der Ostseite des Arlbergtunnels nach den Beob- achtungen des Herrn k. k. Oberingenieurs und Sectionsleiters C. Wagner, 333.—H. Foullon. Ueber ein neues Vorkommen yon kxystallisirtem Magnesit mit saulenformiger Ausbildung, 334.—V. Uhlig. Ueber ein Vorkommen yon Silurblécken im nordischen Diluyium Westgaliziens, 335.—V. Uhlig. Reisebericht aus Westgalizien. Ueber die Gegend von Bochnia und Czchéw, 336.—G. C. Laube. Ueber das Auftreten von Protogingesteinen im nérdlichen Bohmen, 343.—F. Lowl. Eime Hebung durch intrusive Granitkerne, 346.—V. Uhlig. Neue Hinsendungen aus den Kalkalpen zwischen Médling und Kaltenleutgeben, 346.—V. Hilber. Geologische Aufnahme der Niederung zwischen Troppau in Schlesien und Skawina in Galizien, 349.—Fr. v. Hauer. Geologische und monta- nistische Karten aus Bosnien: Paleophonius nuncius, 355.—M. Vacek. Ueber einen Unterkiefer von Aceratherium, cf. minutum, Kaup, aus Con- gerienschichten bei Brunn, 356.—A. Bittner. Aus den Salzburger Kalk- gebirgen : die Ostauslaufer des Tannengebirges, 358. Yienna. Kaiserlich-Konigliche Geologische Reichsanstalt. Ver- handlungen, 1885. Nos. 3-6. 1885. A. Bittner. Zur Stellung der Raibler Schichten, 59.—F. Fuchs. Tertiar- fossilien aus dem Becken yon Bahna (Rumanien), 70.—G. C. Laube. Notiz tiber das Vorkommen von Chamiden und Rudisten im béhmischen Turon, 75.—F. Sandberger. Weitere Mittheilung iber tertiare Siiss- und Brackwasserbildungen aus Galizien, 75.— A. Pichler. Notizen zur Geologie von Tirol, 77.—R. Handmann. Ueber eine charakteristische Saulenbildung ~ eines Basaltstockes und dessen Umwandlungsform in Wacke, 78.—G. Teylas. Neue Héhlen in dem siebenbiirgischen Erzgebirge, 79.—A. Heim. Zur Frage der “Glarner Doppelfalte,” 80.—E. Drasche. Che- mische Untersuchung eines Minerals, 81—C. Diener. Ueber das Vorkommen von Hierlatz-Schichten in der Rofangruppe, 82.—V. Uhlig. Ueber eine Mikrofauna aus den west-galizischen Karpathen, 82.—J. Noth. Petroleumvorkommen in Ungarn, 83.—T. Fuchs. Ueber die Fauna von” Hidalmas bei Klausenburg, 101—T. Fuchs. Mioc&n-Fossilien aus Lykien, 107.—A. vy. Klipstein. Ueber die Gosaukreide der Ladoialpi auf dem Sonnenwendjoch bei Brixlegg im Unterinnthal, 115.—P. Hartnige. Notizen aus dem Feistritzthale in der Umgebung von Anger, 117.—S. Roth. Spuren vormaliger Gletscher auf der Siidseite der Hohen Tatra, 118.—C. Marchesetti. Hohlenthiere aus der Umgebung von Triest, 123.— D. Stur. Vorlage der Farne der Carbon-Flora der Schatzlarer Schichten, 124,—A. Bittner. Neue Einsendungen von Petrefacten aus Bosnien, 140. —D.Stur. Vorlage eines von Dir. E. Doll im pinolith von Sung, im Paltenthale Steiermarks, gefundenen Thierrestes, 14]_—A. Bittner. Aus den Ennsthaler Kalkalpen: Neue Fundstelle von Hallstatter Kalk, 148.— H. y. Foullon. Ueber einen neuen Anbruch von Irystallisirtem Schwe- fel bei Truskawiec in Galizien, 146.—H. v. Foullon. Ueber rosenrothen Calcit von Deutsch-Altenburz, 148.—H. v. Foullon. Calcit auf Kohle aus dem Munzenberger Bergbau bei Leoben, 149.—C. vy. Camerlander. Aus dem Diluvium des nordwestlichen Schlesiens, 151.—S. Brusina. Be- ADDITIONS TO THE LIBRARY. 165 merkungen tiber rumanische Paludinen-Schichten mit Bezug auf Pro- fessor G. Cobalescu’s Werk: Studii geologice si paleeontologice a supra unor Téramuri Tertiare din unite Parti ale Romaniei,”’ 157.—L. v. Tausch. Ueber die Beziehungen der neuen Gattung Durga, G. Bohm, zu den Megalodontiden, speciell zu Pachymegalodon, Giimbel, 163.—A. Rzehak. Diatomaceen im Mediterrantegel der Umgebung von Briinn, 166.—D. Stur. Geschenke fiir das Museum der geologischen Reichsanstalt, 166.— K.M. Paul. Das Salinargebiet von Stidrussland, 167.—K. F. Frauscher. Ergebnisse einiger Excursionen in Salzburger Vorlande, mit besonderer Beriicksichtigung der Eocan- und Kreideablagerungen in der Umgebung von Mattsee, 173.—A. Bittner. Diluvialer Siisswasserkalk von Baden, eingesandt vom Herrn Lehrer E. Ebenfiihrer in Gumpoldskirchen, 183.— E. Hussak. Ueber Eruptivgesteine von Steiersdorf im Banat, 185.—A. Rzehak. Ueber das Vorkommen der Foraminiferengattungen Ramulina und Cyclammina in den alteren Tertiarschichten Oesterreichs, 186.—R. Handmann. Zur Conchylien-Ablagerung von St. Veit a. d. Triesting, 188.—H. B. Geinitz. Zur Geschichte des angeblichen Meteoriten-Falles, im Hirschfelde bei Zittau, 188.—A. Pawlow. Der Jura von Simbirsk an der unteren Wolga, 191.—F. Teller. Olgocanbildung im Feistritzthal bei Stein in Krain, 193.—V. Uhlig. Ueber den Verlauf des Karpathen- Nordrandes in Galizien, 201.—M. Schlosser. Notizen iiber die Siuge- thierfauna von Goriach und tber Miocanfaunen im Alleemeinen, 207.— Nic. Andrussow.- Ueber das Alter der unteren dunklen Schieferthone auf der Halbinsel Kertsch, 213.—A. Pichler. Zur Geologie Tirols, 216. Vienna. Kaiserlich-Konigliche Zoologisch-Botanische Gesellschaft. Verhandlungen, 1884. Band xxxiv. 1885. ——. Mineralogische und Petrographische Mittheilungen. N. F. Band vi. Heft 3. 1884. Purchased. C. W.C. Fuchs. Die vulkanischen Ereignisse des Jahres 1883, 185.— K. von Chrustschoff. Ueber eigenthtimliche Flissigkeitsinterpositionen im Cordierit des Cordieritgneisses von Bodenmais, 232.—I’. Becke. Aetz- versuche am Bleiglanz, 237. ; : : Hefte 4-6. 1885. Purchased. F. Loewinson-Lessing. Jie Variolite von Jaleuba im Gouvernement Olonez, 281.—M. Schuster. Studien tber die Flichenbeschaffenheit und Bauweise der Danburit-Krystalle vom Scopi in Graubundten, 301. : : . Bandvu. Hefte1 & 2. 1885. E. M. Rohrbach. Ueber die Eruptivgesteie im Gebiete der schlesisch- mihrischen Kreideformation, 1.—K.von Chrustschoff. Ueber secundire Glaseinschltisse, 64.—H. Hatch. Ueber den Gabbro aus der Wildschénau in Tirol und die aus ihm hervorgehenden schiefrigen Gesteine, 75.—M. Schuster. Ueber ein neues Vorkommen von krystallisirtem Fichtelit, 88. —F. Becke. Ueber Zwillingsverwachsungen gesteinbildender Pyroxene und Amphibole, 93.—M. Weibull. Untersuchung schwedischer Minerale, 108.—A. Becker. Ueber die Schmelzbarkeit des kohlensauren Kalkes, 122.—C. W. C. Fuchs. Die vulkanischen Ereignisse des Jahres 1884, 146. Warwick. Warwickshire Naturalists’ and Archeologists’ Field Club. Proceedings, 1883. 1884. P. B. Brodie. An Account of the Discovery, by Prof. Lapworth, of Cambrian and pre-Cambrian Rocks in North Warwickshire formerly sup- posed to be of Carboniferous Age, 18.—P. B. Brodie. Volcanoes, their Nature and Origin, 17. 166 ADDITIONS TO THE LIBRARY. Washington. Philosophical Society. Bulletin. Vol. vii. (1884). 1885. J.C. Russell. The existing Glaciers of the High Sierra of California, 5.—W. C. Kerr. The Mica Mines of North Carolina, 9 .—J. C. Russell. Doposits of Volcanic Dust in the Great Basin, 18.—J. R. Eastman. A new Meteorite, 32.—J. 8. Diller. The Volcanic Sand which fell at Unalashka, October 20, 1883, and some Considerations concerning its Composition, 33.—G. H. Williams. The Methods of Modern Petro- graphy, 36.—T. Robinson. The Strata exposed in the Hast Shaft of the Waterworks Extension, 69.—T. Robinson. Was the Earthquake of September 19th felt in the District of Columbia? 73.—C. E. Dutton. The Volcanoes and Lava-Fields of New Mexico, 76. Smithsonian Institution, Annual Report for 1882. 1884. (8vo.) ——. -——. BureauofEthnology. 2nd Annual Report, 1830-81. By J. W. Powell. 1883. (4to.) Watford. Hertfordshire Natural History Society and Field Club. Transactions. Vol. ii. Parts 1-4. 1884-85. H.G. Fordham. Notes on Boulders and Boulder-clay in North Hert- fordshire, 33.—J. V. Elsden. On the Microscopic Structure of Boulders found in the North of Hertfordshire, 47. Wellington. New-Zealand Institute. Transactions and Proceedings. Vol. xvi. (1883). 1884. J. A. Pond. On the Pottery Clays of the Auckland District, 443.—R. M. Laing. A few Notes on Thermal Springs at Lyttelton, 447.8. H. Cox. On the Occurrence of some new Minerals in New Zealand, 448.— F..W. Hutton. On the Lower Gorge of the Waima-Kariri, 449.— D. Sutherland. Recent Discoveries in the Neighbourhood of ’ Milford Sound, 454.—A, Hunter. Direct Evidence of a Change in the Elevation of the Waikato District, 459. Wiesbaden. Nassauischer Verein fir Naturkunde. Jahrbiicher. Jahrgang 37. 1884. Winona. Minnesota Academy of Natural Science. Bulletin. , Vol, 11: No: 24 W133i5 N. H. Winchell. The Ancient Copper-Mines of Isle Royale, 29. : : Non. 1883: W. Upham. Lake Agassiz: a Chapter in Glacial Geology, 290. York. Yorkshire Philosophical Society. Annual Report for 1884. 1885. Zoological Society of London. Proceedings, 1884. Parts 2-4. 1884-85. ——. ——, 1885. Partl. 1885. ——. Report of the Council for the year 1884. 1885. ADDITIONS TO THE LIBRARY. 167 2. Booxs. Names of Donors in Italics. Achepohl, L. Das Niederrheinisch-Westfiilische Steinkohlengebirge. Lieferung 10. Fol. Essen, 1883. Purchased. Africa. Instructions nautiques sur la céte occidentale d'Afrique, de Sierra Leone au Cap Lopez, par C. P. de Kerhallet et Francois. 8vo. Paris, 1883. Presented by the Dépét de la Marine. Agassiz’ und seiner Freunde geologische,Alpenreisen in der Schweiz, Savoyen und Piemont. Ein Alpenreisebuch, unter Agassiz’, Studer’s und Carl Vogt’s Mitwirkung vertaszt von E. Desor. Herausgegeben von Carl Vogt. 2° Auflage. 8vo. Frankfurt am Main, 1847. Presented by A. W. Waters, Esq., P.GS. Albrecht, P. Ueber die morphologische Bedeutung der Kiefer-, Lippen- und Gesichtsspalten. S8vo. Berlin, 1884? Sur les éléments morphologiques du manubrium du sternum chez les mammiféres. 8vo. Brussels, 1884. Sur les spondylocentres épipituitaires du Crane. 8yo. Brussels, 1884. Sur la valeur morphologique de la trompe d’Kustache. 8vo. Brussels, 1884. Erwiderung auf Herrn Prof. Dr. Hermann v. Meyer’s Aufsatz, “Die Zwischenkieferknochen und ihre Beziehungen zur Hasenscharte und zur schrigen Gesichtsspalte.” 8vo. Berlin, 1884. Sur les homodynamies qui existent entre la main et le pied des mammiféres. 8vo. Brussels, 1884. Ueber die Zahl der Zihne bei den Hasenschartenverspalten. 8vo. Berlin, 1884. Alert. Report on the Collections made in the Indo-Pacific Ocean during the Voyage of H.M.S. ‘ Alert,’ 1881-82. 8vo. London, 1884. Presented by the Trustees of the British Museum. Alsace-Lorraine. Geologische Specialkarte von Elsass-Lothringen. Abhandlungen. Band ii. Heft 3. 8vo. Strassburg, 1884. Atlas, 4to. Purchased. = Bandiy. Heft 22 1884. Purchased: Anon. Forests, Streams, Lakes, and Resources of Northern Michigan. 8vo. Marquette, Mich., 1884. Presented by W. Whitaker, Esq., F.GS. The Wonders of Geology ; by the Author of Peter Parley’s Tales. 8vo. Boston, 1852. Presented by W. Topley, Esq., F.G.S. 168 ADDITIONS TO THE LIBRARY. Anon (Trevigra). The Reaction of Gravity in Motion, or the Third Motion of the Earth. 8yo. London,n.d. Presented by J. A. Wade, Esq. Australia. Cdte est d’Australie. Vue de cétes par Wallut. S8vo. Paris, 1882. Presented by the Dépét de la Marine. Barrett, C. The Geology of Swyre, Puncknowle, Burton Brad- stock, &e. 8vo. Bridport,1878. Presented by H. B. Woodward, Esq., F. GS. Barrois, C. Le granite de Rostrenen, ses apophyses et ses contacts. 8vo. Lille, 1884. Sur les ardoises 4 Nereites de Bourg oeooe Haute- Garonne. 8vo. Lille, 1884. Bauerman, H, Text-book of Descriptive Mineralogy. 8vo. London, 1884. Belgium. Musée Royal d'Histoire Naturelle de Belgique. Carte géologique. Textes explicatifs de la livraison de 1884, viz.:— Modave, Virton, Ruette, Lamorteau, Landen, St. Trond, Heers. Syo. Brussels, 1884, Bellardi, L. J molluschi dei terreni terziarii del Piemonte e della Liguria, Parte 4. 4to. Turin, 1884. Bercher, C. E. Ceratiocaride from the Chemung and Waverly Groups at Warren, Pennsylvania. 8vo. Harrisburg, 1884. Beust, Fritz. Untersuchung iiber fossile Hélzer aus Gronland. 4to. Basel, 1884. Purchased. | Blanford, W. T. Address to the Geological Section of the British Association at Montreal, 1884. 8vo. London, 1884. Blomeke,C. Die Erzlagerstatten des Harzes und die Geschichte des auf denselben gefiihrten Bergbaues. 8vo. Vienna, 1885. Pur- chased. Blum, J. R. Handbuch der Lithologie oder Gesteinslehre. 8vo. Erlangen, 1860. Presented by A. W. Waters, Esq., F.GS. Bornemann, J. G. Yon Eisenach nach Thal und Wutha. 8vo. Berlin, 1884. Boyd,C. R. Resources of South-west Virginia, showing the Mineral Deposits of Iron, Coal, Zine, Copper, and Lead. 8vo. New York, 1881. Presented by H. Bauermann, Esq., F.GS. British Museum (Natural History). Catalogue of the Fossil Mam- malia. Part I. Containing the orders Primates, Chiroptera, In- sectivora, and Rodentia. By R. Lydekker. 8vo. London, 1885. Presented by the Trustees of the British Museum. Guide to the Collection of Fossil Fishes in the Department of Geology and Paleontology. 8vo. London, 1885. Presented by Dr. H. Woodward, F.BRS., F.GS. ADDITIONS TO THE LIBRARY. 169 Brodie, P. B. Volcanoes, their Nature and Origin. 8vo. Warwick, 1883. An Aecount of the Discovery by Prof. Lapworth of Cambrian and pre-Cambrian Rocks in North Warwickshire. 1883. Brongniart, C. Note sur les tufs quaternaires de Bernouyille prés Gisors, Eure. 8vo. Paris, 1880. Rapport sur une note de M. Maxime Cornu relative 4 Vaction des huiles lourdes de goudron sur les vignes. 8vo. Ro- morantin, 1882. ——. Excursion dans l’Atlas. 8vo. Paris, 1881. —. Notices Scientifiques. 8vo. Gray, 1882. -- Note complémentaire sur le Titanophasma Fayoli et sur les Protophasma Dumasu et Woodwardu. 8vo. Paris, 1883. ——. Sur un nouvel insecte des terrains carbonifcres de Commentry (Allier), et sur la faune entomologique du terrain houiller. 8vo. Paris, 1882. Apercu sur les insectes fossiles en général, et observations sur quelques. insectes des terrains houillers de Commentry (Allier). 8vo. Montlugon, 1883. | Restaurations d’ailes d’insectes provenant du terrain car- bonifére de Commentry (Allier). 8vo. Paris, 1884. Sur un nouvel insecte fossile de Vordre des Orthopteres, provenant des terrains houillers de Commentry (Allier). 4to. Paris, 1884. Sur la découverte d’une empreinte d’insecte dans les grés siluriens de Jurques (Calvados). 4to. Paris, 1884. Sur un gigantesque Neurorthoptére, provenant des terrains houillers de Commentry (Allier). 4to. Paris, 1884. [Respiration des Insectes.] 8vo. Paris, 1885. ——. Insecte fossile des grés siluriens. 4to. Paris, 1885. et M. Cornu, Champignon observé sur un insecte. 8vo. Paris, 1881. Buenos-Ayres. Annuaire statistique de la Province de Buenos- Ayres, publié sous la direction du C. R. Coni, 1882. 8vo. Buenos Ayres, 1883. Presented by the Argentine Scientific Society. Cadell, H. M. The Harz Mountains—their Geological Structure and History. 8vo. Edinburgh, 1884. Calchith, W. W. Shingle on East Coasts of New Zealand. 4to. London, 1884, Presented by J. B. Redman, Esq., M.Inst.C.L., L.GES. 170 ADDITIONS TO THE LIBRARY. California. State Mining Bureau. Fourth Annual Report of the State Mineralogist (H. G. Hanks), for the year ending May 15, 1884, 8vo. Sacramento, 1884. Cameron, P. A Monograph of the British Phytophagous Hymeno- ptera (Tenthredo, Sirex, and Cynips, Linné). Vol. ii. 8vo. London, 1885. Prasented by the Ray Society. Canada. Geological and Natural- -History Survey. Comparative Vocabularies of the Indian Tribes of British Columbia. By W. F. Tolmie and G. M. Dawson. 8vo. Montreal, 1884. Capellim, G. Del Zifioide fossile (Choneziphus planirostris) scoperto nelle sabbie plioceniche di Fangonero presso Siena. 4to. Rome, 1885. ——. Resti fossili di Dioplodon e Mesoplodon. 4to. Bologna, 1885. Carboni-Grio, D. I terremoti di Calabria e Sicilia nel secolo 18. Svo. Naples, 1885. Carlberg, J. O. Historiskt sammandrag om Svenska Bergverkens uppkomst och utveckling samt grufvelagsliftningen. 8yo. Stock- holm, 1879. Presented by R. Henderson, Esq., F.GS. Caruana, A. A. Discovery of a Tomb-Cave at Ghain Sielem, Gozo, in June 1884, 4to. Malta, 1884. . El-Gherien tal-Liebru, Malta: a hypogeum discovered in July 1884. 4to. Malta, 1884. Casley, George. Geology of Lyme Regis. Sm. 8vo. Lyme Regis, 1880. Presented by H. B. Woodward, Esq., F.GS. Challenger. Reports on the Scientific Results of the Voyage of | H.M.S8. ‘Challenger’ during the years 1873-76. Narrative. Vol.i. Parts 1&2. 4to. London, 1885. —. ——. Zoology. Vol. ix. (in 2 vols.). 4to. London, 1884. ——. Vol. x. 4to. London, 1884. Presented by the Lords of HM. Treasury. Chelot, E. Rectification pour servir 4 l’étude de la faune éocéne du bassin de Paris. 8vo. Paris, 1885. China. Instructions nautiques sur les mers de Chine. Intro- duction. 8vo. Paris, 1883. Presented by the Dépot de la Marine. Choffat, P. De Pimpossibilite de comprendre le Callovien dans le Jurassique supérieur. 8vo. Lisbon, 1884. ——. Sur la place & assigner au Callovien. 8vo. Lisbon, 1884. Churchill, J. F. Stechiological Medicine, and its Applications to Diseases of the Lungs and other Organs. 8vo. London, n.d. ee ae ae er ADDITIONS TO THE LIBRARY. E71 Claypole, H. W. On the Clinton and other Shales &c., composing the Fifth Group of Rogers in the First Survey of Pennsy lvania. 8vo. Philadelphia, 1884. Pennsylvania before and after the Elevation of the Appa- lachian Mountains: a Study in Dynamical Geology. 8vo. Salem, 1885. Clinch, G. Note on the Discovery of certain Paleolithic Weapons and Instruments at Church Field, West Wickham, Kent. 8vo. Bromley, 1882. . Some Account of Ancient Excavations in Well Wood and Chalk-pit Field, West Wickham, Kent. 8vo. West Wickham, 1884. Cochin-China &c. Annuaire des Marées de le basse Cochinchine et du Tong-kin pour l’an 1884, 12mo. Paris, 1883. Presented by the Dépot de la Marine. Cohn, F. Heinrich Robert Goppert als Naturforscher. 8vo. Breslau, 1885. Collins, J. H. Mineralogy. 2 vols. 8vo. London, 1878 & 1883. . , and H. T. Collins. The Geological Age of Central and West Cornwall. (2 papers.) 8vo. Truro, 1881 & 1884. Cope, H. D. On the Evolution of the Vertebrata, Progressive and Retrogressive.—The Position of Pterichthys in the System. 8vo. Salem, 1884. ——. Paleontological Bulletin. Nos. 38 &39. 8vo. Philadelphia, 1884. ——. The Choristodore. S8vo. Salem, 1884. ——. The Creodonta. 8vo. Salem, 1884, ——. The Mastodons of North America. 8vo. Salem, 1884. ——. The Tertiary Marsupialia. 8vo. Salem, 1884. ——. Rodentia of the European Tertiaries. S8vo. Salem, 1885. ——. The Amblypoda. 8vo. Salem, 1885. The Lemuroidea and the Insectivora of the Eocene Period of North America. 8vo. Salem, 1885. Cornish, T. Our Gold-Supply: its Effects on Finance, Trade, Commerce, and Industries. 8vo. London, 1884. Presented by H. Bauermann, Esq., F.GS. Corte Real, J.A. Resposta 4 Sociedade Anti-Esclavista de Londres. 8vo. Lisbon, 1884. Cox, Colonel. On the Blue Clay at ape Newspaper-slip, 1872. Presented by W. Whitaker, Esq., F.G.S. Dall, W. H. A Monograph of British Fossil Brachiopoda: a Review. Svo. Cambridge, Mass., 1885. 172 ADDITIONS TO THE LIBRARY. Damon, R. Geology of Weymouth, Portland, and Coast of Dorset- shire from Swanage to Bridport-on-the-Sea. New edition. 8vo. Weymouth, 1884 ; also Supplement, 2nd edition, 1880. Daubrée, A. Exposition Universelle de 18674 Paris. Rapports du Jury International. Substances minérales. Syo. Paris, 1867. Expériences sur la schistosité des roches et sur des dé- formations de fossiles corrélatives de ce phénoméne ; conséquences géologiques qu’on peut en déduire. 8vo. Paris, 1877. ; Applications de la méthode expérimentale & l’étude des dé- formations et des cassures terrestres. 8vo. Paris, 1879. Descartes, l'un des créateurs de la cosmologie et de la géo- logie. 8vo. Paris, 1880. Sur les réseaux de cassures ou diaclases qui coupent la série des terrains stratifiés: Exemples fournis par les environs de Paris. 8vo. Paris, 1880. Essai d’une classification des cassures de divers ordres, que présente l’écorse terrestre. 8vo. Paris, 1882. Etudes expérimentales sur l’origine des cassures. terrestres et sur leur coordination réciproque au point de vue des accidents du relief du sol. 8vo. Paris, 1882. Davies, D. C. A Treatise on Earthy and other Minerals and Mining. 8vo. London, 1884. Presented by H. Bauerman, Esq., F.GS. Dawkins, W. Boyd. On some Apatite near Ottawa, Canada. 8vo. Manchester, 1884. Dawson, J. W. Observations on the Geology of the Line of the Canadian Pacific Railway. S8vo. London, 1884. ~ . Rough Notes of a Naturalist’s Visit to Egypt. 8vo. London, 1884. Dechen, H.v. Geologische Briefe aus America. 8vo. Bonn, 1884. De Rance, C. E., and W. Topley. Report of the Committee ap- pointed for the purpose of inquiring into the Rate of Erosion of the Sea-coasts of England and Wales, and the Influence of the Artificial Abstraction of Shingle or other Material in that Action. 8vo. London, 1885. ; ) Derby, O. A. On the Flexibility of Itacolumite. 8vo. New Haven. 1884. . Peculiar Modes of Occurrence of Gold in Brazil. 8vo. New Haven, 1884. Physical Geography and Geology of Brazil. 8vo. Rio de Janeiro, 1884. Dewalque, G. Catalogue des ouvrages de géologie, de minéralogie et de paléontologie, ainsi que des cartes géologiques quise trouvent dans les principales bibliothéques de Belgique. 8vo. Liége, 1884. Presented by the Société Géologique de Belgrque. ADDITIONS TO THE LIBRARY. 173 Dictionary, Hungarian-German, by M. Ballagi. 8vo. Pest, 1872. Presented by A. W. Waters, Esq., F.GS. Diener, C. Hin Beitrag zur Geologie des Centralstocks der julischen Alpen. 8vo. Vienna, 1884. Ueber den Lias der Rofan-Gruppe. 8vo. Vienna, 1885. Dollo, L. Premiére note sur le Simcedosaurien d’Erquelinnes. 8vo. Brussels, 1884. Doyle, P. Paper-making in India, being Notes of a Visit to the Lucknow Paper-Mill. 8vo. Lucknow, 1885. Duncan, P. Martin. Address to the Linnean Society, 1884. 8vo. London, 1884. A Revision of the Families and Genera of the Sclerodermic Zoantharia, Ed. & H., or Madreporaria (M. rugosa excepted). 8vo. London, 1884. , and W. P, Sladen. On the Family Arbaciade, Gray, Part 1. 8vo. London, 1885. ) . The Classificatory Position of Hemiaster elongatus, Duncan & Sladen: a Reply to a Criticism of Prof. Sven Lovén. 8vo. London, 1884. Dupont, H. La chronologie géologique. 8vo. Brussels, 1884. Elsden, J. V. On the Microscopic Structure of Boulders found in the North of Hertfordshire. 8yvo. Hertford, 1884. Encyclopedia Britannica. 9th edition. Vols. xviii., xix. Orn—Pro. 4to. Edinburgh, 1885. Purchased. Encyclopedic Dictionary. Vol. iv. Part 1. Glot—Int. 4to. London, 1884. Presented by the Rev. R. Hunter, F.GS. England and Wales. Geological Survey. Memoirs. Explanation of Quarter-sheet 50 N.W. The geology of the country around Diss, Eye, Botesdale, and Ixworth, by F. J. Bennett. 8vo. London, 1884. 66S8.W. The geology of the country een Attleborough, Watton, and Wymondham, by F. J. Bennett. 8vo. London, 1884. 63 N.W. and 8.W. The geology of the country around Fakenham, Wells, and Holt, by H. B. Wood- ward. 8vo. London, 1884. . 93 N.E. The geology of the country north-east of York and south of Malton by C. Fox-Strangways. 8vo. London, 1884. 94.N.E. The geology of Bridlington Bay, by J. a9 Dakyns and C. Fox-Strangways. 8vo. London, 1885. : 95 N.W. The geology of the country between Whitby and Scarborough, by C. Fox-Strangways and G. Barrow. 8vo. London, 1882. 174 ADDITIONS TO THE LIBRARY. England and Wales. Geological Survey. Memoirs. Explanation of Quarter-sheet 96 N.E. The geology of Eskdale, Rosedale, &e., by CO. Fox-Strangways, C. Reid, and G. Barrow. Syo. London, 1885. . The Vertebrata of the Forest Bed Series of N orfolk and Suffolk, by E. T. Newton. 8vo. London, 1882. . Guide to the Geology of London and the N eichbourhood, by W. Whitaker. 4th edition. 8vo. London, 1884, English Channel. Annuaire des Courants de Marée de la Manche pour l’an 1883. 8vo. Paris, 1883. Presented by the Dépdt de la Marine. Evans, John. Address delivered at the Anniversary Meeting of the Royal Society on Monday, Dec. 1, 1884. 8vo. London, 1884. Physiography. 8vo. London, 1884. Favre, E. Revue géologique suisse pour l’année 1884. xv. 8vo. lane, 1885. Felix, J. Korallen aus agyptischen Tertiirbildungen. S8vo. Berlin, 1884. Flower, W. H. On the Development and Succession of the Teeth in the Marsupialia. 4to. London, 1867. Presented by Prof. P. M. Duncan, F.R.S. Fordham, H. G. Notes on Boulders and Boulder-Clay in | North Hertfordshire. 8vo. Hertford, 1884. France. Dépét dela Marine. Annuaire des Marées des Cétes de France pour an 1884. 12mo. Paris, 1883. _ ——. ——. —— 1885. 12mo. Paris, 1884. : Catalogue par ordre géographique des Cartes, Plans, etc. S8vo. Paris, 1883. French, H. H. A Paper on Bournes. 8vo. Sutton, 1884. Fritsch, A. Fauna der Gaskohle und der Kalksteine der Permfor- mation Bohmens. Bandii. Heft 1. 1885. Gardner, J.S. A Monograph of the British Eocene sui Vol. ii. Part 2. 4to. London, 1884. On the Relative Ages of the American and the English Cretaceous and Eocene Series. S8vo. Jondon, 1884. The Age of the Basalts of the North-east Atlantic. 8vo. Belfast, 1884. Gaudry, A. Sur un Sirénien d’espéce nouvelle trouvé dans le bassin de Paris. 8vo. Paris, 1881. ——. Nouvelle note sur les Reptiles Permiens. 8vo. Paris, 1885. ADDITIONS TO THE LIBRARY. 175 Genitz, H. B. Ueber die Grenzen der Zechsteinformation und der Dyas tiberhaupt. 4to. Dresden, 1885. Genth, F. A., and G. Vom Rath. On the Vanadates and Iodyrite from Lake Valley, Sierra Co., New Mexico. 8vo. Philadelphia. Gilpin, E. Notes on the De Bert Coal-Field, Colchester Co., N.S. Goodchild, J. G. Contributions towards a List of the Minerals occurring in Cumberland and Westmoreland. S8vo. Carlisle, 1885. Gosselet, J. Note sur deux roches cristallines du terrain dévonien du Luxembourg. 8yo. Lille, 1884. Note sur les schistes de St. Hubert dans le Luxembourg et principalement dans le bassin de Neufchateau. 8yo. Lille, 1884. Note sur quelques affleurements des poudingues dévonien et liassique et sur lexistence de dépdts siluriens dans |’Ardenne. 8vo. Lille, 1884. Remarques sur la faune de Vassise de Vireux 4 Grupont. 8vo. Lille, 1884. Sur la faille de Remagne et sur le métamorphisme quelle a produit. 8vo. Lille, 1884. ——. Note sur les schistes de Bastogne. 8vo. Lille, 1885. . Sur la structure géologique de lArdenne d’aprés von Lasaulx. Svo. Lille, 1885. Great Britain. Geological Survey. Memoirs. Vol. iii. (North Wales.) 2nd edition. 8vo. London, 1881. Green, W. L. The Voleanic Problem from the point of view of Hawaiian Volcanoes. 8vo. Honolulu, 1884. Greenland. Meddelelser om Gronland. Hefte4—6. 8vo. Copen- hagen, 1883. And Tilleg til Heft 5. 4to. Copenhagen, 1883. Presented by Prof. F. Johnstrup. Grimes, J. S. Geonomy: Creation of the Continents by Ocean Currents. 8vo. Philadelphia, 1885. Groth, E. R. G. An Essay on the Origin and Development of the Solar System. 8vo. London, 1884. Groth, P. Physikalische Krystallographie und Einleitung in die krystallographische Kenntniss der wichtigeren Substanzen. Zweite Auflage. 8vo. Leipzig, 1885. Purchased. Gimbel, K. W. von. Geologie von Bayern. 1° Theil. Grundzige der Geologie. Lief.1 &2. 8vo. Cassel,1884&1885. Purchased. . Ueber die Beschaffenheit der Mollusken-Schalen. 8vo. Stuttgart, 1884. VOL. cXLE q 176 ADDITIONS TO THE LIBRARY. Gunn, J. OnCoal-Fieldsin the Eastern Counties. 8vo. Norwich, 1885. Haast, J. von. In Memoriam: Ferdinand R. von Hochstetter, 8vo. Christchurch, N.Z., 1884. Hail, James. Descriptions of the Species of Fossil Reticulate Sponges constituting the Family Dictyospongide. 8vo. Albany, 1884. Harker, A. Graphical Methods in Field-Geology. 8vo. London, 1884. | ——. On the Successive Stages of Slaty Cleavage. 8vo. London, 1885. The Cause of Slaty Cleavage: Compression v. Shearing. 8vo. London, 1885. The Oolites of the Cave District. S8vo. 1885. Harrison, J.T. On the Sources of Water Supply for the Metropolis. 4to. London, 1884. Parliamentary Return. Hatle, E. Die Minerale des Herzogthums Steiermark. Hefte 1 & 2. 8vo. Graz, 1884. Purchased. Hébert, EZ. Notes sur la géologie du département de l’Ariége. 8vo, Paris, 1884. Heilprin, A. Contributions to the Tertiary Geology and Paleon- tology of the United States. 4to. Philadelphia, 1884. Heim, A. Handbuch der Gletscherkunde. 8vo. Stuttgart, 1885. Purchased. ) Hesse. Grossherzoglich-Hessische Geologische Landesanstalt 2u Darm- stadt. Abhandlungen. Bandi. Heft1l. 4to. Darmstadt, 1884. Hinde, G. J. Description of a new Species of Crinoids with Articu- lating Spines. 8vo. London, 1885. Hornes, R., and M. Auinger. Die Gasteropoden der Meeres-Abla- gerungen der ersten und zweiten miocinen Mediterran-Stufe in der osterreichisch-ungarischen Monarchie. Lief.4. 4to. Vienna, 1884, Purchased. Hopkinson, J. Remarks on the Land Mollusca, with reference to their Investigation in Hertfordshire. 8vo. Hertford, 1884. Hull, E. Mount Seir, Sinai, and Western Palestine. Svo. London, 1885. Presented by the Committee of the Palestine Exploration Fund, Hunt, T. Sterry. The Taconic Question in Geology. Part 2. 4to. Montreal, 1884. . The Origin of Crystalline Rocks. 4to. Montreal, 1884. Hussak, E. Anleitung zum Bestimmen der gesteinbildenden Mine- ralien. S8vo. Leinzig, 1885. Purchased. ADDITIONS TO THE LIBRARY. ae iy Hutton, F. W. On the Geology of the North Head of Manukau Harbour. 8vo. Wellington, 1870. . On the Alluvial Deposits of the Lower Waikato, and the Formation of Islands by the River. 8vo. Wellington, 1872. Description of three new Tertiary Shells in the Otago Museum. 8vo. Wellington, 1875. On the Cause of the former great Extension of the Glaciers’ in New Zealand. 8vo. Wellington, N.Z., 1875. On the Relation between the Pareora and Ahuriri Forma- tions. S8vo. Wellington, 1877. Descriptions of some new Tertiary Shells from Wanganui. Svo. Wellington, 1883. ——, Revision of the recent Lamellibranchiata of New Zealand. 8vo. Sydney, 1884. ——. The Origin of the Fauna and Flora of New Zealand. 8vo. Dunedin, 1884. : India. Geological Survey. Memoirs. Vol. xxi. Parts 1 & 2. Svo. Calcutta, 1884. ee Clee athe 4. LOoo, Palzontologia Indica. Series 4. Indian Pre- Tertiary Vertebrata. Vol. i. Part 1. By R. Lydekker. 4to. Calcutta, 1885. : : : Series 10. Indian Tertiary and Post-Tertiary Vertebrata. Vol. ii. Parts 2-4. By R. Lydekker. 4to. Calcutta, 1884. SO. Part 5. By R. Lydekker. 1884. ——, = e Series 13. Salt-range Fossils. By W. Waagen. aig Productus-limestone Fossils; IV. (fase. 3 & 4). Ato. Calcutta, 1884. a : Series 14: Tertiary and Upper Cretaceous Fossils of Western Sind. Vol. i. No. 3. The Fossil Echinoidea. Fasc. 4. By P. M. Duncan and W. P. Sladen. 4to. Calcutta, 1884. . . Records. Vol. xvii. Parts 3&4. 1884. 8vo. Cileuten: 1884. ; Vol. xviii. Parts 1&2. 1885. Irving, R. D. Divisibility of the Archean in the North-west. 8vo. New Haven, 1885. , and C. R. van Hise. On Secondary Enlargements of Mineral Fragments in certain Rocks. 8vo. Washington, 1884. Italy. Ministerio di Agricolture, Industria e Commercio. Direzione generale dell’ Agricoltura. Relazione sul servizio minerario nel 1882. 8vo. Rome, 1884. q 2 178 ADDITIONS TO THE LIBRARY. Jack, R. L. Lecture on the Bowen River Coalfield. Newspaper slip, 1885 (‘ Port Denison Times’). Jamieson, T'. E. The Inland Seas and Salt-Lakes of the Glacial Period. 8vo. London, 1885. Jannettaz, EH. Les Roches. 2e édition. 8vo. Paris, 1884. Jeffreys, J. Gwyn. On the Mollusca procured during the ‘ Lightning’ and ‘ Porcupine’ Expeditions, 1868-70. Pt. 8. 8vo. London, 1884, On the Concordance of the Mollusca inhabiting both sides of the North Atlantic and the intermediate Seas. 8vo. London, 1885. Johnstrup, F. Nogle Iagttagelser over Glacial Phenomenerne og Cyprina-Leret 1 Danmark. 8vo. Copenhagen, 1882. Jones, T. Rupert. Review of ‘Second Annual Report of the United States Geological Survey to the Secretary of the Interior,’ 1880-81. Demonstration on Marbles and other Monumental Stones. 8vo. London, 1884. Notes on Paleozoic Bivalved Entomostraca. No. 17. Some North-American Leperditie and allied Forms. 8vo. London, 1884. Notes on the Paleozoic Bivalved Entomostraca. No. 18. Some species of the Entomidide. 8vo. London, 1884. — Notes on the Foraminifera and Ostracoda from the Deep Boring at Richmond. S8yvo. London, 1884. Notes on the late Mr. George Tate’s Specimens of Lower Carboniferous Entomostraca from Berwickshire and Northampton- shire. 8yvo. London, 1884. On the Geology of South Africa. S8vo. London, 1884. On the Implementiferous Gravels near London. 8vo. London, 1884. Intermittent Streams in Berkshire. S8vo. London, 1885. , and J. W. Kirkby. Notes on the Paleozoic Bivalved Ento- mostraca. No. XIX. 8vo. London, 1885. : , and G. S. Brady. A Monograph of the British Fossil Bivalved Entomostraca from the Carboniferous Formations. Part 1. No. 2. 4to. London, 1884. , and Henry Woodward. Notes on Phyllopodiform Crustaceans, referable to the Genus Hchinocaris, from the Paleozoic Rocks. 8vo. London, 1884. Jones, Sir Willoughby. The Arterial Drainage of Norfolk. 8vo. Norwich. 1849, P-»-ted by H, B. Woodward, Esq., F.GS. ADDITIONS TO THE LIBRARY. 179 Journet, F, L’Australie. 8yvo. Paris, 1884. Kneeland, S. The Subsidence Theory of Earthquakes, 8vo. Boston, 1884. Konen, A. von. Beitriige zur Kenntniss der Placodermen des nord- deutschen Oberdevon’s. 4to. Gottingen, 1883. Ueber eine Paleociine Fauna von Kopenhagen. 4to. Gdot- tingen, 1885. Kunize, O. Ueber gasogen-sedimentiire peas der Urgesteine. 8vo. Leipzig, 1884. Kusta, J. Thelyphonus bohemicus, n. sp. Ein Geisselscorpion aus der Steinkohlenformation von Rakonitz. 8vo. Prag, 1884. Lapworth, C. The Mason College and Technical Education. 8vo. Birmingham, 1884, ——. On the Close of the Highland Controversy. 8vo.. London, 1885. Lasaulx, A. von. LEinfiihrung in die Gesteinslehre. 8vo. Breslau, 1885. Purchased. La Touche, J. D, A Handbook of the Geology of Shropshire. 4to. London, 1884. Lebour, G. A. Deposit of Lacustrine Marl in West Yorkshire. 8vo. London, 1884. On the Breccia-Gashes of the Durham Coast, and some recent EKarth-shakes at Sunderland. 8vo. Newcastle-on-Tyne, 1884. On the Geological Distribution of Endemic Goitre in Eng- land. 8vo. n.d Lendenfeld, R. v. Der Tasman-Gletscher und seine Umgebung. Ato. Gotha. 1884. Purchased. Leonardelli, G. I] Saldame, il Rego e la Terra di Punta Merlera in Jstria come formazione termica. 8vo. Rome, 1884. Lesquereux, Leo. Description of the Coal Flora of the Carboniferous Formation in Pennsylvania and throughout the United States. Vols. i. & uu. 8vo. Harrisburg, 1880. Also Atlas. 8vo. 1879. Description of the Coal Flora of the Carboniferous Formation in Pennsylvania, and throughout the United States. Vol. iii. 8vo. Harrisburg, 1884. Lewis, H. C. On supposed Glaciation in Pennsylvania south of the Terminal Moraine. 8vo. Newhaven, 1884. . Notes on the Progress of Mineralogy in i884. 8vo. Phila- delphia, 1885» Lindstrom, G. On the Silurian Gastropoda and Pteropoda of Gotland. 4to. Stockholm, 1884. 18e ADDITIONS TO THE LIBRARY. Inversidge, A. Rocks from New Britain and New Ireland. 8yvo. Sydney, 1883. The Deniliquin or Barratta Meteorite. 1st and 2nd Notice. 8vo. Sydney, 1883. On the Chemical Composition of certain Rocks, New South Wales, &. 1st Notice. S8vo. Sydney, 1883. Loretz, H. Ueber Echinosphirites und einige andere organische — Reste aus dem Untersilur Thiringens. 8vo. Berlin, 1884. Lovén, 8, On Pourtalesia, a genus of Echinoidea. 4to. Stockholm, 1883. Liwl, F. Die Granit-Kerne des Kaiserwaldes bei Marienbad. 8vo. Prag, 1885. Iney, W. C. The Terrace Gravels of pena oe Ross-shire : Hoch Crib, Fretherne. 8vo. Gloucester, 1883. Section of a Well-sinking at the Island, Gloucester, by Messrs. Robertson and Co., and some Remarks upon the Thickness of the Lower Lias at Gloucester and the Neighbourhood. $8vo. Gloucester, 1884, Section of Birdlip. Some Remarks on a Boring for Water near Birdlip for the City of Gloucester. Svo. Gloucester, 1884. Inundgren, B. Anmirkningar om Spondylusarterna i Sveriges Kritsystem. 4to. Stockholm, 1885. ——. Undersékningar 6fver Brachiopoderna i Sveriges Kerteyptem- Ato. Lund, 1885. Liitken, C. Des cranes et des autres ossements humains de Minas Geraés dans le Brésil Central. 8vo. Copenhagen, 1884. LIydekker, R. Synopsis of the Fossil Vertebrata of India ; Note on the Bijori Labyrinthodont ; and Note on a Skull of Hippothertum antilopinum. 8vo. Calcutta, 1883. Catalogue of Vertebrate Fossils from the Siwaliks of India, in the Science and Art Museum, Dublin. 4to. Dublin, 1884. —. Notes on some Fossil Carnivora and Rodentia. $8vo. London, 1884. Note on the Distribution in Sine and Space of the Genera of Siwalik Mammals and Birds. 8vo, London, 1884. Note on three Genera of Fossil Artiodactyla, with De- scription of a new Species. 8vo. London, 1885. Lyell, Sir C., and P. M. Duncan. The Student’s Elements of Geology, by Sir Charles Lyell. Fourth Edition, revised by P. Martin Dunean, 8vo, London, 1885. Presented by L. Lyell, Esq., F.GS. Iyman, B. S. A Review of the Atlas of the Western Middle Anthracite Field. 8vo. 1884. ADDITIONS TO THE LIBRARY. 181 Marcou, J. Biographical Notice of Joachim Barrande. 8vo. Cam- bridge, Mass., 1884. Notes 4 Voccasion du prochain Congrés géologique inter- national, avec des remarques sur les noms des terrains fossiliféres les plus anciens, 8vo. Paris, 1884, ——. The “Taconic System” and its Position in Stratigraphic Geology. 8vo. Cambridge, Mass., 1885. , and J. B. Marcou. Mapoteca Geologica Americana. A Catalogue of Geological Maps of America (North and South), 1752- 1881, in geographic and chronologic order. 8vo. Washington, 1884. Marcou, J. B. A Review of the Progress of North American In- vertebrate Paleontology for 1883. 8vo. Salem, 1833. Marion, A. F. Sur les caractéres d’une Conifére tertiaire, voisine des Dammarées (Doliostrobus Sternbergi). Ato. Paris, 1884. Marsh, O. C. Dinocerata: A Monograph of an Extinct Order of gigantic Mammals. 4to. Washington, 1884. Massalongo, A. Sopra le piante fossili dei terreni terziarj del Vicentino. 8vo. Padova, 1851. Presented by A. W. Waters, Esq., F.G.S. - ——. Plants fossiles nove in formationibus tertiariis regni Veneti nuper invente. S8vo. Verona, 1853. Presented by A. W. Waters, Esq., F.GS. Paleophyta rariora formaticnis tertiarie agri Veneti. 8vo, Venice, 1858. Presented by A. W. Waters, Esq., F.G.S. Reliquie della flora fossile eocena del Monte Pastello nella provincia Veronese. Svo. Venice, 1858, Presented by A. W. Waters, Esq., P.GS. Medlicott, H. B. Submerged Forest on Bombay Island. 8vo. Calcutta, 1882 ? Mercalli, G. Contribuzioni alla geologia delle Isole Lipari. 8vo. Milan, 1879. Natura delle eruzioni dello Stromboli ed in generale dell’ attivita sismo-vulcanica nelle Kolie. 8vo. Milan, 1881. Le inondazioni et i terremoti di Verona. 8vo, 1882. ——. Sul! eruzione Etnea del 22 marzo 1883. 8vo. Milan, 1883. ——. Notizie sullo stato attuale dei vulcani attivi Italiani, 8vo. Milan, 1884. Metcalfe, A. T. On the Mammoth at Creswell. 8vo. Derby ?, 1885. Meunier, Stanislas. Encyclopédie Chimique. Tome 2. Meétalloides. Appendice 2me cahier. Météorites. 8vo. Paris, 1884. ——. ‘raité de Paléontologie pratique. 8vo. Paris, 1884. 182 ADDITIONS TO THE LIBRARY. Miller, H. Tynedale Escarpments; their Pre-glacial, Glacial, and Post-glacial Features. 8vo. Newcastle-upon-Tyne, 1880. River-terracing ; its Methods and their Results. 8vo. Edin- burgh, 1884. ' On Boulder-glaciation. 8vo. Edinburgh, 1885. Moreton, S. H. Milford Sound and the Scenery of the West Coast of the Middle Island of New Zealand. 8vo. Invercargill, N. Z., 1882. ——. A Scramble over the Lake Mountains. 8vo. Invercargill, NoFelesa: Moseley, H. N. On the Structure of the Stylasteride, a Family of the Hydroid Stony Corals. 4to. London, 1878, Presented by Prof. P. M. Duncan, F.R.S. ~ Naumann, E. Ueber den Bau und die Entstehung der japanischen Inseln. S8vo. Berlin, 1885. Purchased. Navarro, EH. J. studio prehistorico sobre ia Cueva del Tesora. 8vo. Malaga, 1884. Newberry, J. S. Descriptions of some peculiar screw-like Fossils from the Chemung Rocks. 8vo. New York, 1885. Newfoundland. Pilote de Terre-Neuve, par G. Cloué. 2me édition. 2 vols. 8vo. Paris, 1882. Presented by the Dépét de la Marie. New South Wales. Australian Museum. Keport of the Trustees for 1888. 4to. Sydney, 1384. : . Department of Mines, Annual Report of the, for the year | 1883. 4to. Sydney, 1834. New Zealand. Control and Inspection of Mines (Report on), 1884. Ato. Wellington, 1884. Presented by G. J. Binns, Esq. . Geological Survey. Reports of Geological Explorations during 1883-84. 8vo. Wellington, 1884. ——. ——_. Meteorological Report, 1883. 8vo. Wellington, 1884. Nicholson, C. The Work and Workers of the British Association, 18381-1884. 8vo. London, 1884. Miediwiedzki, J. Ueber die Salzformation von Wieliczka und Bochnia sowie die an diese angrenzenden Gebirgsglieder. 8vo. Lemberg, 1884. Nikitin, S. Die Cephalopodenfauna der Jura-Bildungen des Gou- vernements Kostroma, 4to. St. Petersburg, 1884. Norway. Instructions nautiques sur les cotes ouest de Norvége. Svo. Paris, 1883. Presented by the Dépot de la Marine. ADDITIONS TO THE LIBRARY. 183 Norwegian North Sea Expedition. Den Norske Nordhavs Expe- dition 1876-78. XI. Zoologi. Asteroidea ved D. C. Danielssen og J. Koren. 4to. Christiania, 1884. ~~ XIT. Zoologi. Pennatulida ved D. C. Danielssen og Johan Koren. -4to. Christiania, 1884. XIII. Zoologi. Spongiade ved G. A. Hansen. 4to. Christiania, 1885. Presented by the Meteorological Institute, Christiania. Nova Scotia. Department of Mines. Report for the year 1884. 8vo. Halifax, N. 8., 1885 Omboni, G. Delle Ammoniti del Veneto che furono descritte e figurate da T. A. Catullo. 8vo. Venice, 1884. Owen, R. A History of British Fossil Reptiles. Parts 1-5. 4to. London, 1849-51. Purchased. Vols. 1-4. 4to. London, 1849-84. Purchased. Owen, Sir R. Antiquity of Man as deduced from the discovery of a Human Skeleton during the Excavations of the East and West India Dock Extensions at Tilbury. 8vo. London, 1884. Pacific Ocean. Instructions nautiques sur locéan Pacifique Sud. Iles Samoa. 8vo. Paris, 1884. Presented by the Dépét de la Marine. : Paléontologie Frangaise. Ire série. Animaux invertébrés. Ter- rain jurassique. Livraison 70. Crinoides, par P. de Loriol. 8vo. Paris, 1884. Purchased. : : ‘ Livraison 71. Kchinides réguliers, par G. Cotteau. 8vo. Paris, 1884. Purchased. ; : . lLivraison 72. Crinoides, par P. de Loriol. 8vo. ae 1884. Purchased. : ‘ : Livraisons 73 & 75, Echinides régu- liers, par G. Cotteau. S8vo. Paris, 1884. Purchased. ; : . lLivraison 74. Crinoides, par P. de Loriol. 8vo. Pere 1884. Purchased. : : : Livraison 77. Brachiopodes, par Deslongchamps. 8vo. Paris, 1885. Purchased. : : ; . Livraisons 76 & 78. KEchinides réguliers, par G. Cotteau. 8vo. Paris, 1885. Purchased. Paris. Muséum Whistoire naturelle. Nouvelle galerie de Paléon- tologie. 8vo. Paris, 1885. Parsons, J. Discovery of Coprolites at bape (India). 8vo. Roorkee, 1884. Paviow, A. Notes sur Vhistoire géologique des oiseaux. 8vo. Moscow, 1885. Notions sur le systéme jaraneigue de l'Est de la Russie. 8vo. Paris, 1884. 184 ADDITIONS TO THE LIBRARY. Peacock, R. A. Second Supplement to ‘Saturated Steam.’ 8vo. London, 1884. Penck, A. Die Hiszeit in den Pyrenaen. 8vo. Leipzig, 1883. Alte und neue Gletscher der Pyrenien. 8vo. Salzburg, 1884. ——. Geographische Wirkungen der Eiszeit. 8vo. Berlin, 1884. Mensch und Eiszeit. 4to. Brunswick, 1884. Pennsylvania. Second Geological Survey. Reports. Presented by the Survey. A. Historical Sketch of Geological Explorations in Pennsylvania sae other States, by J. P. Lesley. 8vo. Harrisburg, 1876, A,. A Special Report to the Legislature upon the Causes, Kinds, and amount of Waste in mining Anthracite, by Franklin Platt; with a Chapter on the Methods of Mining, by John Price Wetherill. .8vo. Harrisburg, 1881. A,. First Report of Progress in the Anthracite Coal Region. The Geology of the Panther Creek Basin or Eastern End of the Southern Field, by C. A. Ashburner. 8vo. Har- risburg, 1883. And Atlas. 8vo. A,. Atlas, Western Middle Anthracite Field. Part 1. 8vo. A,. Grand Atlas. Division II. Anthracite Coal Fields. Part 1. Fol. Harrisburg, 1884. | AC. Report on the Mining Methods and Appliances used in the Anthracite Coal Fields, by H. M. Chance. 8yvo. Harris- burg, 1883. And Atlas. 8vo. B. Preliminary Report on the Mineralogy of Pennsylvania, by F. A. Genth; with an Appendix on the Hydrocarbon Compounds, by 8. P. Sadtler. S8vo. Harrisburg, 1875. . Second Preliminary Report on the Mineralogy of Pennsyl- vania, by F. A. Genth. 8vo. Harrisburg, 1876. C. Report of Progress in the district of York and Adams Coun- ties, by Persifor Frazer, Jun. 8vo. Harrisburg, 1876. C,. Report of Progress in the Counties of York, Adams, Cumber- land, and Franklin, by Persifor Frazer, Jun. 8vo. Har- risburg, 1877. C,. The Geology of Lancaster County, by Persifor Frazer, Jun. 8vo. Harrisburg, 1880. And Maps. . The Geology of Chester County. Edited by J. P. Lesley. 8vo. Harrisburg, 1883. C,- The Geology of Philadelphia County and of the Southern Parts of Montgomery and Bucks, by C. E. Hall. 8vo. Harrisburg, 1881. ADDITIONS TO THE LIBRARY. 185 . Report of Progress on the Brown Hematite Ore Ranges of Lehigh County, by Frederick Prime, Jun. 8vo. Harris- burg, 1875. ; Report of Progress on the Brown Hematite Deposits of the Siluro-Cambrian Limestones of Lehigh County, lying be- tween Shimersville, Millerstown, Schnecksville, Balliets- ville, and the Lehigh River, by Frederick Prime, Jun. 8vo. Harrisburg, 1878. . Vol. 1. The Geology of Lehigh and Northampton Counties, by J. P. Lesley, R. N. Sanders, H. M. Chance, F. Prime, and C. KE. Hall. 8vo. Harrisburg, 1883. e Vol: 2- The Geology of the South Mountain Belt of Berks County, by HE. V. d’Invilliers. S8vo. Harrisburg, 1883. . Vols. Li&-2: © Atlas; “Svo; . Atlas. 8vo. Special Report on the Trap Dykes and Azoic Rocks, by T. Sterry Hunt. Part 1. 8vo. Harrisburg, 1878. Report of Progress in the Juniata District on the fossil Iron - Ore Beds of Middle Pennsylvania, by John H. Dewees; with a Report of the Aughwick Valley and East Broad Top District, by C. A. Ashburner. 8vo. Harrisburg, “tone. Report of Progress in Bradford and Tioga Counties, by Andrew Sherwood, Franklin Platt, and John Fulton. 8vo. Harrisburg, 1877 (?). . The Geology of Lycoming and Suilivan Counties, by Andrew Sherwood and Franklin Platt. S8vo. Harrisburg, 1880. . The Geology of Potter County, by Andrew Sherwood; with Report on the Coal Fields, by Franklin Platt. 8vo. Harrisburg, 1880. . The Geology of Clinton County, by H. M. Chance. 8vo. Harrisburg, 1880. . The Geology of Susquehanna County and Wayne County, by I. C. White. 8vo. Harrisburg, 1881. . The Geology of Pike and Monroe Counties, by I. C. White ; Special Surveys of the Delaware and Lehigh Water Gaps, by H. M. Chance. 8vo. Harrisburg, 1882. . The Geology of the Susquehanna River Region in the six counties of Wyoming, Lackawanna, Luzerne, Columbia, Montour, and Northumberland, by I. C. White. 8vo. _ Harrisburg, 1883. Report of Progress in the Clearfield and Jefferson District of the Bituminous Coal Fields of Western Pennsylvania, by Franklin Platt. 8vo. Harrisburg, 1875. to ool ADDITIONS TO THE LIBRARY. >» Report of Progress in the Cambria and Somerset District of the Bituminous Coal Fields of Western Pennsyl- vania, Part I., by F. and W.G. Platt. 8vo. Har- risburg, 187 rik , Part Il, by F. and W. G. Platt. 8vo. Harris- burg, 1877. . Report of Progress in Indiana County, by W. G. Platt. 8vo. Harrisburg, 1878. . Report of Progress in eee County, bg W.G. Platt. 8vo. Harrisburg, 1880. . Report of Progress in Jefferson County, by W. G. Platt. 8vo. Harrisburg, 1881. . A Revision of the Bituminous Coal Measures of Clear- field County, by H. M. Chance. 8vo. Harrisburg, 1884. Report of Progress in the Venango County District, by John F. Carll, with Observations on the Geology around Warren, by F. A. Randall, and Note on the comparative Geology of north-eastern Ohio and north- western Pennsylvania and western New York, by J.P. Lesley. 8vo. Harrisburg, 1875. . Report of Progress, Oil-well Records and Levels, by John F. Carll. 8vo. Harrisburg, 1877. . The Geology of the Oil Regions of Warren, Venango, Clarion, and Butler Counties, including Surveys of the Garland and Panama Conglomerates in Warren and Crawford, and in Chatanqua Co., N. Y.; descriptions of Oil-well rig and tools, and. a discussion of the Pre- glacial and Postglacial drainage of the Lake-Erie country, by John F. Carll. 8vo. Harrisburg, 1880. With maps, &c. ; , Geological Report on Warren County and the neighbour- ing Oil Regions, with additional Oil-well Records, by J. F. Carll. 8vo. Harrisburg, 1883. . Special Report on the Petroleum of Pennsylvania, its pro- duction, transportation, manufacture, and statistics, by Henry E. Wrigley. 8vo. Harrisburg, 1875. . Report of Progress in the Green and Washington District of the Bituminous Coal Fields of Western Pennsylvania, by J. J. Stevenson. 8vo. Harrisburg, 1876. » Report of Progress in the Fayette and Westmoreland District of the Bituminous Coal Fields of Western Pennsylvania, Part L., by J. J. Stevenson. 8vo. Harrisburg, 1877. , Part IL, by J.J. Stevenson. S8vo. Harrisburg, 1878. ADDITIONS TO THE LIBRARY. 187 L. Special Report on the Coke Manufacture of the Youghio- gheny River Valley in Fayette and Westmoreland Counties, with geological notes of the Coal and Iron-ore Beds, by Franklin Platt. 8vo. Harrisburg, 1876. M. Report of Progress in the Laboratory of the Survey at Harrisburg, by Andrew 8. McCreath. 8vo. Harrisburg, 1875. M,. Second Report of Progress in the Laboratory of the Survey at Harrisburg, by A. 8. McCreath. 8vo. Harrisburg, 1879. M,. Third Report of Progress in the Laboratory of the Survey at Harrisburg, by A. S. McCreath. 8yo. Harrisburg, 1881. N. Report of Progress. Two hundred Tables of Elevation above tide-level of the railroad stations, summits, and tunnels; canal locks and dams, river riffles, &c., in and around Pennsylvania, by Charles Allen. 8vo. Harris- burg, 1878. O. Catalogue of the Geological Museum, by Charles E. Hall. Pare 1. 8vo. Harrisburg, 1878. O,——. Part 2. 8vo. Harrisburg, 1880. 2 P. Description of the Coal Flora of the Carboniferous Forma- tion of Pennsylvania and throughout the United States, by Leo Lesquereux. Vols. i. and ii. (in one vol.). 8vo. Harrisburg, 1880. Atlas. 8vo. Harrisburg, 1879. ——. Vol. iii. 8vo. Harrisburg, 1884 (Text and Plates in one vol.). P,. The Permian or Upper Carboniferous Flora of West Vir- ginia and S.W. Pennsylvania, by W. M. Fontaine and I. GC. White. 8vo. Harrisburg, 1880. P,. Ceratiocaride from the Upper Devonian Measures in Warren County, by C. E. Beecher ; Eurypteride from the Lower Productive Coal Measures in Beaver County, and the Lower Carboniferous, Pithole Shale, in Venango County, by J. Hall. 8vo. Harrisburg, 1884. Q. Report of Progress in the Beaver River District of the Bituminous Coal Fields of Western Pennsylvania, by I. C. White. 8vo. Harrisburg, 1878. Q,. The Geology of Lawrence County, by I. C. White. 8vo. Harrisburg, 1879. Q,. The Geology of Mercer County, by I. C. White. 8vo. Harrisburg, 1880. Q,. The Geology of Erie and Crawford Counties, by I. C. White. Discovery of the Preglacial Outlet of Lake Erie, by J. W. Spencer. 8vo. Harrisburg, 1881. 188 = ADDITIONS TO THE LIBRARY. R. The Geology of McKean County and its connection with that of Cameron, Elk, and Forest, by Chas. A. Ash- burner. 8vo. Harrisburg, 1880. Also Maps and Charts. 8vo. R. (Appendix A.) Drillings for Coal in Sergeant Township, McKean County, by N. F. Jones, J. P. Lesley, and C. A. Ashburner. 8Svo. Harrisburg, 1881. T. The Geology of Blair County, by F. Platt. 8vo. MHarris- burg, 1881. T. Geology of Blair County, by J. J. Stevenson. Atlas. 8vo. T,. The Geology of Bedford and Fulton Counties, by J. J. Stevenson. 8vo. Harrisburg, 1882. T,. The Geology of Centre County, by E. VY. d’Invilliers. 8vo. Harrisburg, 1834. VY. Partl. The Northern Townships of Butler County. Part 2. A special Survey made in 1875, along the Beaver and Shenango rivers, in Beaver, Lawrence, and Mercer Counties, by H. M. Chance. 8vo. Harrisburg, 1884. V,. The Geology of Clarion County, by H. M. Chance. 8vo. Harrisburg, 1880. Z. Report on the Terminal Moraine in Pennsylvania and Western New York, by H.C. Lewis. 8vo. Harris- burg, 1884. Pennsylvania. Second Geological pu yey. Reports A,, B, B,, CC. 0. U. & , 6, Gy a. Gee HoH, HL LT, I. K., Kk, L, M,N, 0, 0, P, P,, Q, Q,, Q,, 8, TV, V. Syo. Harrisburg, 1875-84. Presented by H. Panbrman, Ean. EGS. Pery, G. A. Estatistica agricola do Districto de Beja. Parte 2&3. 4to. Lisbon, 1884-85. Petzholdt, A. Silicification organischer Korper. 4to. Halle, 1853. Presented by Prof. P.M. Duncan, F.R.S. Phillips, J. Arthur. A Treatise on Ore Deposits. 8vo. London, 1884. Pichler, A. Beitriige zur Geognosie Tirols. 8yvo. Insbruck, 1859. Presented by A. W. Waters, Esq., F.GS. Portis, A. Les Chéloniens de la mollasse Vaudoise conservés dans le Musée Géologique de Lausanne. 4to. Geneva, 1882. Il caleare del Monte Tabor, Piemonte. 8vo. Turin, 1883. ——, Il cervo della torbiera di Trana. 8vo. Turin, 1883. ‘___. Nuovi chelonii fossili del Piemonte. 4to. Turin, 1883. ——, Nuovi studi sulle traccie attribuite all’ uome Pliocenice. to. Turin, 1883. ——. Contribuzione alla ornitolitologia Italiana. 4to. Turin, 1884. s ADDITIONS TO THD LIBRARY. 189 Portugal. Communicacédes da seccfio dos trabalhos geologicos de Portugal. Tomo i. Fasc. 1.1885. 8vo. Lisbon, 1885. Pre- sented by that Survey. Putman, C. H. Elephant Pipes in the Museum of the Academy of Natural Sciences, Davenport, Iowa. S8vo. Davenport, 1885. Queensland. Report on the Tin Mines of Herberton, Western, and Thompson’s Creek Districts, and the Silver Mines of the Dry River, by &. LZ. Jack. 4to. Brisbane, 1883. Report on the Mount Morgan Gold Deposits, by R. L. Jack. 4to. Brisbane, 1884. . Report on the Hodgkinson Gold-field, by 2. LZ. Jack. Ato. Brisbane, 1884. Quenstedt, Fr. Aug. Die Ammoniten des schwiibischen Jura. Hefte+&5. 8vo. Stuttgart, 1884. And Atlas, 4to. Pur- chased. . Handbuch der Petrefaktenkunde. 3e Auflage. Abth.3 & 4. 8vo. Tubingen, 1884, 1885. Purchased. Petrefaktenkunde Deutschlands. Abth. 1. Band vii. Hefte 5&6. Gasteropoden, Hefte5&6. 8vo. Leipzig, 1884. Atlas, 4to. Purchased. Reade, T. M. Denudation of the two Americas. S8vo. Liverpool, 1885. Reid, C. On Norfolk Amber. 8vo. Norwich, 1884. On recent Additions to the Fauna and Flora of the Cromer Forest-Bed. 8vo. Norwich, 1884. Reid, J. Notes on the Origin and Development of Granitic and other allied Varieties of Plutonic Rocks. 8vo. Edinburgh, 1885. Reinsch, P, F. Micro-Palaeo-Phytologia Formationis Carboniferae. ~2vols. 4to. Erlangen, 1884. Purchased. Renard, A. : Recherches sur la composition et la structure des phyllades ardennais. S8vo. Brussels, 1884. Renevier, HE. Le Musée Géologique de Lausanne en 1883. 8vo. Lausanne, 1884. Les facies géologiques. 8vo. “Geneva, 1884. ——. Rapport sur la marche du Musée Géologique Vaudois en 1884, avec une notice sur lVichthyosaure acquis pour le musée. 8vo. Lausanne, 1885. Rogers, W. B., A Reprint of Annual Reports and other Papers on the Geology of the Virginias, by the late. 8vo. New York, 1884. Presented by Mrs. Rogers. 190 ADDITIONS TO THE LIBRARY. Romanowski, G. Materialien zur Geologie von Turkestan. Lief. 1. 4to. St. Petersburg, 1880. Lief. 2. [In Russian.] 4to. St. Petersburg, 1884. Presented by the Russian Geological Society. Russia. Comité géologique dela Russie. Mémoires. Vol.i. Nos. 2 '& 3. 4to. St. Petersburg, 1884. —. —. —. Vol. it. No. 1. 4to. St. Petersburg, 1884. —. . Reports for 1884. Tome in. Nos. 3-10. 8vo. St. Petersburg, 1884 & 1885. - Reports. Vol. iv. Parts 2-5. 1885. Saporta, G. Les organismes problématiques des anciennes mers. 4to. Paris, 1884. Purchased. , et A. F. Marion. L’évolution du regne végétal.—Les Phanérogames. 8yo. Paris, 1885. Sartorius von Waltershausen, W. Untersuchungen iiber die Klimate der Gegenwart und der Vorwelt mit besonderer Beriicksichtigung der Gletscher-Erscheinungen in der Diluvialzeit. 4to. Haarlem, 1865. Presented by A. W. Waters, Esq., F.GS. Saxony. Geologische Specialkarte des Konigreiehs Sachsen. Erlau- terungen. Blatt 29, Mutzschen ; Blatt 125, Kirchberg; Blatt 129, Zoblitz; Blatt 137, Schwarzenberg; Blatt 145, Eibenstock ; Blatt 147, Wiesenthal. 8vo. Leipzig, 1884. Scoresby, J. W. Journal of a Voyage to the Northern Whale Fishery ; including Researches and Discoveries on the Eastern Coast of West Greenland made in the summer of 1822 in the ship ‘Baffin’ of Liverpool. 8vo. Edinburgh, 1823. Presented by A. W. Waters, Esq., F.G.S. Scudder, S. H. Nomenclator Zoologicus. 8vo. Washington, 1882-84. Purchased. Scudder, S. H. A Contribution to our Knowledge of Palzozoic Arachnida. 8vo. 1884. Triassic Insects from the Rocky Mountains. 8yvo. New Haven, 1884. Dictyoneura and the Allied Insects of the Carboniferous Epoch. 8vo. Boston, 1885. New Genera and Species of Fossil Cockroaches from the older American Rocks. 8vo. Philadelphia, 1885. The earliest Winged Insects of America. 4to. Cambridge, Mass., 1885. Seeley, H. G. Manual of Geology, Theoretical and Practical; by John Phillips, edited by R. Etheridge and H. G. Seeley. Part 1. Physical Geology and Paleontology, by H. G. Seeley. 8vo. London, 1885. ADDITIONS TO THE LIBRARY. Igt Selwyn, A. R. C., and G. M. Dawson. Descriptive Sketch of the Physical Geography and Geology of the Dominion of Canada. 8vo. Montreal, 1884. Shipman, J. Geology of the Parish of Lenton, part of the Borough of Nottingham. 8vo. London, 1884. Shrubsole, O. A. On certain less familiar Forms of Palolithic Flint-Implements from the Gravel at Reading. S8vyo. London, 1884. Simpson, Martin. The Fossils of the Yorkshire Lias, described from Nature, with a carefully measured section of the strata and the fossils peculiar to each. 2nd edition. 8yo. Whitby, 1884. Purchased. Smith, J. R. Expository Thoughts on the Creation. 8yvo. London, n. d. Sollas, W. J. On the Origin of Freshwater Faunas: a Study in Evolution. 4to. Dublin, 1884. South Australia. Mr. Winnecke’s Explorations during 1883. Ato. Adelaide, 1884. Presented by the Colonial Government. ——. Report of Government Geologist (H. Y. L. Brown). 4to. Adelaide, 1884. Presented by the Colonial Government. , 1884. Ato. Adelaide, 1884. Presented by the Colonial Government. —-. Report of Government Geologist re Visit to Far North. 4to. Adelaide, 1884. Presented by the Colonial Government. . Work in Progress in Geological Department (H. Y. L. Brown). 4to. Adelaide, 1884. Presented by the Colonial Government. Spain. Comision del mapa geolégicade Espatia. Boletin. Tomo xi. Cuaderno 1. 1884. Terremotos de Andalucia. Informe de la Comision nom- brada para su estudio dando cuenta del estado de los trabajos en 7 de Marzo de 1885. Presented by the Commission. Spratt, T. A. B. Report on the Present State of the Navigation of the River Mersey (1883). 8vo. London, 1884. Stanley, W. F. On certain Effects which may have been produced in the Atmosphere by Floating Particles of Volcanic Matter from the Eruptions of Krakatoa and Mount St. Augustin. 8vo. London, 1884. Steno, Nicolaus. The Prodromus to a Dissertation concerning Solids naturally contained within Solids. Englished by H. 0. 8vo. London, 1671. Presented by Clement Reid, Esq., F.GS. Stirling, J. Notes on a Geological Sketch-section through the Australian Alps. 8vo. Adelaide, 1884. . The Phanerogamia of the Mitta-Mitta Source Basin. Art. 2. 8vo. Melbourne, 1884. VOL. XII. r 192 ADDITIONS TO THE LIBRARY. Stoppani, A. Studii geologici e paleontologici sulla Lombardia. Svo. Milan, 1858. Presented by A. W. Waters, Esq., F.GS. Stur, D. Ueber Steinkohlen-Pflanzen von Llanelly und Swansea in South Wales, England. 8vo. Vienna, 1884. Sweden. Geologiska Onilersilentiy, Ser. Aa. Beskrifningar till Kartbladen i skalen ~ Nos. 88 (1883) & 91 (1884). 8vo. Stockholm. vo00? Ser. Ab. Beskrifning till Kartblad i skalan = = = No. 10. 8vo. Stockholm, 1883. . Ser. Ba. Cartes générales avec descriptions. No. 4. Annexe explicative 4 la carte géologique générale de la Suéde. Echelle Feuille méridionale. 8vo. Stockholm, 1884. 1 1000000° . Ser.C. Afhandlingar och uppsatser. No.58. Om Basalttuffen vid Djupadal i Skane, af F, Hichstaédt. S8vo. Stock- holm, 1883. . No. 60. Mikroskopisk undersék- ning af de vid Djupadal i i Skane forekommande basaltbergarterna, af E. Svedmark. 8vo. Stockholm, 1883. : : : . No.61. Studier vid Svenska Joklar, af F. Svenonius. 8vo. Stockholm, 1884. : : : No. 62. Om Siljanstraktens Sand- stenar, af M. Stolpe. 8vo. Stockholm, 1884. . No. 63. Cephalopoderna 1 Sveriges Kritsystem, ae qe Moberg. Partl1. 4to. Stockholm, 1884. No. 64. Praktiskt geologiska under- sékningar - inom norra delen af Kalmar lin 4to. Stockholm, 1884. —_, . No. 66. Undersdkningar 6fver Siljansomradets Trilobitfauna, af 8. L. Tornquist.. 4to. Stock- holm, 1884. Symons, B. The Maidanpec Wet Process for the Reduction of certain poor Cupreous Ores. 8vo. Truro, 1884. Szajnocha, L. Zur Kenntniss der mittelcretacischen Cephalopoden- Fauna der Inseln Elobi an der Westkiiste Afrika’s. 4to. Vienna, 1884. Tasmania. Report of Inspector of Mines for 1883. 4to. Hobart, 1884. Presented by that Government. Tate, R. Description of new Species of Mollusca of the Upper - Eocene beds at Table Cape. 8vo. Adelaide, 1834. Notes of a Critical Examination of the Mollusca of the older Tertiary of Tasmania alleged to have living representatives. 8vo. Adelaide, 1884. ADDITIONS TO THE LIBRARY. 193 Tate, R. Notes on the Physical and Geological Features of the Basin of the Lower Murray River. 8vo. Adelaide, 1884. Tausch, L. Ueber einige Conchylien aus dem Tanganyika-See und deren fossile Verwandte. 8vo. Vienna, 1884. Teisseyre, L. Der podolische Hiigelzug der Meodoboren als ein sarmatisches Bryozoen-Riff. 8vo. Vienna, 1884. Thomé de Gamond, A. Etude pour l’avant-projet d’un Tunnel sous-marin entre l’Angleterre et la France reliant sans rompre charge les chemins dle fer de ces deux pays par la ligne de Grisnez a Eastware. 4to. Paris, 1857. Purchased. Account of the Plans for a new project of a Submarine Tunnel between England and France, produced at the Universal Exhibition of 1867. Second edition. 4to. London, 1870. Purchased. Thoroddser, T. Oversigt over de islandske Vulkaner Historie. 8vo. Copenhagen, 1882. Topley, W. Report upon the National Geological Surveys of Europe. 8vo. London, 1884. Toula, F. Grundlinien der Geologie des westlichen Balkan. Ato. Vienna, 1881. Geologische Uebersichtskarte der Balkan-Halbinsel. Ato. Gotha, 1882. Die im Bereiche der Balkan-Halbinsel geologisch unter- suchten Routen. S8vo. Vienna, 1883. Materialien zu einer Geologie der Balkanhalbinsel. 8vo. Vienna, 1883. Geologische Untersuchungen im centralen Balkan und in den angrenzenden Gebieten. 8vo. Vienna, 1884. Geologische Untersuchungen im westlichen Theile des Balkan’s und in den angrenzenden Gebieten. S8vo. Vienna, 1875-84. Ueber Amphicyon, Hyemoschus und Rhinoceros (Acera- theriwm) von Goriach bei Turnau in Steiermark. 8vo. Vienna, n, d. Tryon, George W., Jun. Structural and Systematic Conchology : an Introduction to the Study of the Mollusca. 3 Vols. 8vo. Philadelphia, 1882-84. Purchased. Tschernyschew, T. Der permische Kalkstein im Gouvernement Kostroma. 8vo. St. Petersburg, 1885. Turstig, J. See Dorpat, Nat. Gesellsch. Tylor, A. New Points in the History of Roman Britain, as illus- trated by Discoveries at Warwick Square, within the City of London. 4to. London, 1884. r2 194 ADDITIONS TO THE LIBRARY. United States. Geological Survey. Monographs. Vol. v. The Copper-bearing Rocks of Lake Superior, by R. D. Irving. Ato. Washington, 1883. - . Third Annual Report (1881-82). Roy. 8vo. Washington, 1883. : Geology of the Comstock Lode and the .Washoe | District, by G. F. Becker. 4t0. Washington, 1882., Atlas, fol. Mineral Resources of the United States, by Albert Williams, Junr. 8vo. Washington, 1883. Atlas to accompany the Monograph on the Geology and Mining Industry of Leadville, Colorado, by S. F. Himmons. Fol. Washington, 1883. - Van den Broeck, E. Réponse aux critiques de M. O. van Ertborn relatives aux données utilitaires de la feuille de Bilsen de la carte ‘ géologique détaillée de la Belgique. 8vo. Renaix, 1884. Velains, C. Les Volcans, ce quils sont et ce qu’ils nous apprennent. 8vo. Paris, 1884. Verbeek, R. D. M. Krakatau. Partie 1. 8vo. Batavia, 1885. Presented by the Netherlands Government. Victoria. Gold Fields. Reports of the Mining Surveyors and Re- gistrars. Quarter ended 3lst March, 1884. 4to. a 1884. ——. ——. Quarter ended 30th June, 1884. Ato. Mel- eee 1884. ——. Quarter ended 30th sditernben 1884. Ato. Moipeeea! 1884. ——. Quarter ended 31st’ December, 1884. 4to. Melbourne, 1884. Presented by the Minister of Mines. Mineral Statistics for 1883. 4to. Melbourne, 1884. Pre- sented by the Minister of Mines. . Patents and Patentees. Indexes for the year 1878. Vol. xiii. (by R. Gibbs, Registrar-General). 4to.. Melbourne, 1882. : Indexes for the year 1879. Vol. xiv. 4to. Mel- bourne, 1884. Report of the Chief Inspector of Mines to the Honourable the Minister of Mines for the year 1883. 4to. Melbourne, 1884. Vine, G. R. Reports L-V. of the Committee appointed for the | purpose of reporting on the Carboniferous Polyzoa. 8vo. Lon- don, 1880-84. . Notes on the Carboniferous Polyzoa of North Yorkshire. 8vo. Leeds, 1881. ADDITIONS TO THE LIBRARY. 195 Vine, G.R. Notes on the Carboniferous Polyzoa of West Yorkshire and Derbyshire. 8vo. Leeds, 1883. —. 8yvo. Leeds, 1884. Notes on the Carboniferous Entomostraca and Foraminifera of the North-Yorkshire Shales. 8vo. Leeds, 1883. 8vo. Leeds, 1884. ——. Notes on Species of Ascodictyon and Rhopalonaria from the Wenlock Shales. 8yvo. London, 1884. . Further Notes on new Species and other Yorkshire Car- boniferous Fossil Polyzoa described by Prof. John Phillips. 8vo. - Leeds, 1884, Vom Rath, G. Mineralogische Notizen. 8vo. Bonn, 1885. Vortrige und Mittheilungen. 8vo. Bonn, 1885. Walker, J. F. On Waldheimia Bernardina. 8vo. York, 1884. Wappeus, J. HE. A geographia physica do Brasil. 8vo. Rio de Janeiro, 1884. Presented by O. A. Derby, Esq. War Office. Army Medical Department. Report for 1882. Vol. xxiv. 8vo. . London, 1884. Webster’s Royal Red Book for 1885. Presented by Messrs. Webster and Larkin. Western Australia. Report on the Geology of the Kimberley District, W. A., by #. 7. Hardman. 4to. | Perth, 1884. Report upon the Work carried out by the joint Admiralty and Colonial Marine Survey Department during the year 1884, comprising also a Report upon the capabilities of Cambridge Gulf as a Port, with other information regarding the N.W. coast of Australia, by Stafi-Commander J. E.Cochlan, R.N. 4to. Perth, 1835. Presented by the Colonial Grovernment. Wheatley, H. B. A List of English Indexes. 8vo. London, 1879. Whitaker. W. On the Area of the Chalk as a Source of Water- Supply. 8vo. London, 1884. Williams, H. S. On the Fossil Faunas of the Upper Devonian along the meridian of 76° 30’, from Tompkins County, N.Y., to Bradford County, Pa. 8vo. Washington, 1884. Wilson, E. The Lias Marlstone of Leicestershire as a Source of Iron. 8vo. Birmingham, 1885. Wilson, J. S. G., and H. M. Cadell. The Breadalbane Mines. 8vo. Edinburgh, 1884. Wisconsin. (Descriptive America.) Fol. New York, 1884. Pre- sented by J. Hobbies, Esq. Witchell, EH. The Geology of Stroud and the Area drained by the Frome. 8vo. Stroud, 1882. 196 ADDITIONS TO THE LIBRARY. Wood, J. J. General Geological Section. (Table.) Woodward, H. On the Wing of a Neuropterous Insect from Australia; Fossil Shells from South Australia; New Trilobites from South Australia. 8yvo. London, 1884. Woodward, H. B. “Karthquakes and Subsidences in Norfolk. 8vo. Norwich, 1884. ——. Life of R. A. C. Godwin-Austen. S8vo. London, 1885. Wright, T. Monographs on British Fossil Echinodermata. [Pub- lished in the Monographs of the Paleontological Society, and bound in 3 vols.| Bequest. Yearbook of Scientific and Learned Societies of Great Britain and Ireland. First Annual Issue. 8vo. London, 1884. Second Annual Issue. 8vo. London, 1885. Presented by Messrs. Griffin & Co. Zigno, Baron A. de. Due nuovi Pesci Fossili della famigha dei Balistini scoperti nel terreno eocene del Veronese. 4to. Naples, 1884. Flora Fossilis Formationis Oolithicae. Vol. ii. Part iv.a, v.a. Ato. Padova, 1885. Zittel, K. A. Handbuch der Paleontologie. Bandi. Abth. 2, Lief. 3. 8vo. Munich, 1884. Purchased. 3. Maps &c. The names of Donors in Italies. Belgium. Carte géologique. Feuille de Modave, Virton, Ruette, Lamorteau, Landen, St. Trond, Heers. Scale =,;4,). Presented by the Royal Museum of Natural History of Belgium. Canada. Geological Survey. Map of the Dominion, geologically coloured from surveys made by the Geological Corps, 1842 to 1882. 2sheets. Scale 45 miles = 1 inch. England and Wales. Geological Survey. Sheets and quarter-sheets. Solid. 488.W.; 51 N.W.,S.E.; 68 N.W.; 91 N.E.; 93 N.E. ; 96 N.E., S.E.; 98 N.W.,S.W.; 99 S.E.; 102 N.E. Drift. 48 N.W., N.E.,8.W.; 49 N.,8.; 50 N.W., N.E., 8.W., S.E.; 51 N.W., N.E., S.E.; 66 N.E., S.W., S.E.; 67 5.W.; 68 N.W.,S.W.; 84; 85; 918.E.; 93. N.E.; 94N.W., N.E., S.W., S.E.; 96 N.W., N.E., S.W., S.E.; 102 N.E.; 103 S.W., S.E.; 104 8.W. Horizontal Sections. Sheets 122, 123, 125, 128, 130 to 139 inclusive. Vertical Sections. Sheets 68, 69. France. Carte géologique détaillée de la France. Feuilles 15, 44, 46, 63, 96, 99, 115, 138, 148, 178, 188, 216, 217 ,228, 229. Scale sydyy- Purchased. ADDITIONS TO THE LIBRARY. 197 Norway. Geologiske Undersogelse. Kartbladet 25 », 26 a, 46, 47 v, 50 ¢, sooloa7- Ordnance Survey Maps. Presented by the First Commissioner of Works. One-inch General Maps. England and Wales. Outline. New Series. Quarter-sheet 242. Ireland. Hills. Quarter-sheets 174, 198, 192. Scotland. Hills. Sheets 107 and 114. Outline. Sheets 50, 59, 68, 78, 80, 88, 90. Six-inch County Maps. Bedfordshire. Quarter-sheets 7 N.W., N.E., S.W., S.E.; SSW .: B9eseW 3) LL.N.E., SB. ¢ LOW NE 14 S.W.; 17 S8.W.; 18 N.E.; 19 N.W.,8.W.; 20 N.W.; 21 N.E., S.E.; 22 N.E., 8.W.; 23 N.E., §.E.; 24 N.W., Nik S.W ss 80 NW: 32 NE SW. 82 35. N.W., N.E., S.W. . Brecknockshire. Quarter-sheets 32 N.W.; 45 N.W., N.E., S.W., S.E.; 50 N.W., N.E.; 51:N.W. Buckinghamshire. Sheets 28, 29, 30, 35. on Cornwall. Quarter-sheets 1 N.E.; 1S.W.andS.E. in one; 2 NeW... We. caWen4 NB S.W.2)5°N.E..8. W. S.E.; 6 N.W., S.W.; 7S.E.; 8 S.W., S.E.; 10 N.W., N-E., S: W., S:H.3 11 N.W.;-N.E: S.W., S.E.; 12 8.E.; TaN 14° 5:Wo; 16 NE SW. S.K.: 21 S.E.; 22 N.E., 8.E.; 23 8.W.; 29 S.E. Derbyshire. Quarter-sheets 3 N.E.; 19 S.E.; 28 N.W., N.E. S.W., 8:E.; 29 N.W., N.H.,S.E.; 30 N.W., S-W.y, S.E.; 33 N.W.,58.W., S.E.; 34 N.W., N.E., S.W., S.E.; oo NAW. Nob S.W., S.H.3 38 NE. S.Bee 39 NOW., N.E. 2 40)8:H. »- 43: N.E.. 45 8.W.; 57 N.EL: 6 N.W. and Leicester. Quarter-sheets 63 N.E. & 22N E. pled hohe Deere and Nottinghamshire. Quarter-sheets 58.W. & 568.W., SSS Se ee es Cl eee ee 26 N.E. & 17 N.E., 26 S.E. &1758.E., 31 N.E. & 22 N.E., SS SSS. es Ce Ra 31 S.W. &228,.W., 31S.E. & 228.E., 40 N.E. & 32 N.E., 46 S.W.& 37 S.W.. 51 S.W. & 41 SW. pot and Staffordshire. Quarter-sheets 27 N.W. & 5 N.W., 27 N.E.& 5N.E., 279E.& 5S.E., 329.E.&9SE, 37 NEG & 14N.E., 33 S.W. &158.1 W., 57 N.W. & 41 N.W., 57 8.7 .W. W.&415.W, 57 SE. & 40S.E., 59 NE. & 47 NE., 598.W.& 47 S.W., SW. 63 N.E. & 53 NE. 198 ADDITIONS TO THE LIBRARY, Devonshire. Quarter-sheets 26 N.E.,S.E.; 27 N.W., N.E., S.W., S.E.; 28 N.E., S.W., S.E.; 38 N.E., S.E.; 39 N.W., NE. 8.W.; 8.Hus 40 SW: 49 NUNS Bee N.W., N.E., S.W., S.E.; 51 N.E., S.E.; 57 N.W., S.W.; 61 N.W., N.E., S.H.; 62 N.W., N.E., S.W., S.E.; 63 N.W., N.E., S.W., S.E.; 74 N.E., S.W., S.E.; 75 N.W., Bo. W., S-BLS 76 NOW... INORS 77 NN Wet ea eo S.W.; 83 N.E.; 87 N.E.,S.W., S.E.; 88 N.W., S.W.; 90 N.W., N.E., S.W.; 97 N.W., N.E., S.W.; 98 N.W.; 104 N.E., S.E.; 105 N.W., N.E., S.W.; 106 N.E., S.W., S..; 107° N.W.; 112° NW. S:W.: 132 SW. S.2-: 136 N.W. Glamorganshire. Sheets 9, 10, 14, 16, 17, 18, 21, 21a, 22, 23, 24, 26, 31, 32, 39, 44, 46, Glaneenseraee: Gone Bhece: 13 S.W., S.E.; 16 N.E., S.E.; 17 N.W., S.W.; 19 N.W., N.E., S:W., S.E.; 20 N.W., S.W.; 21 S.E.; 248.W.; 26 N.W.; 27 N.W.; 30 8.E.; 31 N.E.; 32 N.W.; 33 N.E.,S.W., S.E.; 34 _N.W.; 36 N.E., SE); 38 N.E., SB So °N.E.. S. Ee: 41 §.E.; 42 N.W., N.E., S.W., S.E,; 48 S.E.; 44N.W., S.W.; 46 N.W., N.E.; 47 N.E., S.E.; 48 N.E.; 49 N.W.; 50 N.E., S.W.; 52 N.W.; 56 N.W., S.W.; 58 N.W. . SE ee and Warwickshire. Quarter-sheets 1 S.E. & 43 S.E., ee 3 N.E. & 49 N.E., 48.W. &50 S$. W., 12 N.W. & 55 N.W., awe ee ee ee 128.E. & 55 8.E.,13 N.W. & 56 N.W., 18 N.W. & 60 N.W., —_ OO M#€#!@[{""—T"_—“—. 21 N.W. & 61 N.W. —— and Worcestershire. Quarter-sheets 3 S.W.& 43 S.W., ee 3 S.E. & 43 8.E., 6 N.E. & 49 N.E., 68. W. & 49 8.W., N88 SSS SSE 6 S.E. & 49 8.E., 8S.W. & 51 8.W., 11 N.E. & 54 N.E., 11 S.W. & 54AS.W, 11S. & 54 S.E., 12 NE. & 55 N-E., peri oebci es es 7 SI SE ee ed eR cles Sa A RE 128. W. & 558.W., 15 NW. BGS oP 175S.E. & 59 S.E., SESS SS PS 21 N.E. & 61 N.E. Herefordshire. Quarter-sheet 7 S.E. ——— and Shropshire. Quarter-sheet 7 N.E. & 82 N.E. Hertfordshire. Sheets 6, 7, 11, 12, 18, 15, 18, 19, 20, 22, 25, (21, 295 29, 01,307,005 BO, (ee and Bedfordshire. Sheet 26 and 31. -_—— and Shropshire. Quarter-sheet 7 N.E. & 82 N.E. Inverness (Isle of Higg). Sheet 70. Leicestershire. Quarter-sheets 3 N.W., 8.W.; 7 N.E., 5.W., SB; 3'5.W-;-105.W.; 13. N.Waswe; 14 NW; N.E., S.W3 SE; AT NW 8 We ey NE. 8. W-, ADDITIONS TO THE LIBRARY. 199 pie yee NO. 8. W., SE: 5 20 NEL, BW.37 2d NE. ; 24 N.W., N.E., S.W., S.E.; 25 N.W., N.E., 8.W., S.E. ; 26 NW. Se W., SE. 3 27 N.W.; 3d N.W., 5. Ww. Leicestershire and Derbyshire. Quarter-sh. 228.E. & 638.E. m . . ge and Nottinghamshire. Quarter-sheets 28.W.& 448.W., pA eS re eh ee 28.E. & 44 8.E., 5 S.E. & 458.E., 6 N.E. & 47 N.E., ee 6 S.E. & 47 8.E., 7 N.W. & 48 N.W. , 11 S.E. & 50 S.E., = SF ~ aD 12 N.E. &51N.E., 128.W.& & 518.W., 12 S.E. & 51 8.E., 17 N.E. & 52 NE. oer and Rutlandshire. Quarter-sheets 20 S.E. & 1 8.E., ——$ A. _______ ee 21 S.W. & 2 ‘S.W,, 21 8.5. & 23.E., 27 N.E. & 4 NE, 27 8.5. & 48.E., 33 NE. & BNE, 33 SE. & 8 SE. Lincolnshire and Nottinghamshire. Quarter- sheets 21 N.W., S.W.; 69 N.W., N.E. Merionethshire. Quarter-sheets 16 N.W., N.E., S.E. Middlesex. Sheet 17. a aN Monmouthshire and Glamorganshire. Sheets 10 and 6. Montgomery. Sheet 10 N.W., S.W.; 15 N.E., S.E.; 16 N.W.; 48 N.W.,S.W., S.E.; 44 N.W.; 49 N.W., N.E. Norfolk. Quarter-sheets 22 N.E., S.E.; 23 N.W., S.W.; 33 N.E., S.E.; 34 N.W., N.E.,S.W.; 35 S8.E.; 41 N.W., N.E., S.H.; 42 N.W., S.W.; 45 N.W., N.E., S.E.; 46 N.W., N.E., S.W., S.E.; 47 N.W., S.W., N.E., 8.E.; 49 NeW.,.5.Was, 00 NW. 5. W., S.E.; 53 N.E., S.B.; 54 Dae yo, Mle seoo NeWes.W.> 59 S.B.; 60 NW oH. 5 oh ON Wie Go. Nor pt, : 66 N.W.; 69 NOB 70 NOW. S.W.e ¢2 NOW.ON.E., S.W., S.B.5 73 S.Es 82 N.W., N.E.,S.W.; 84 N.E., S.W.; 85 8.E.; 868.W., SH: COON FL. Ostia: OO ONG W'S. W.3. OL NB 92N.W., INJE: 95 (N. Es 96 NOE: : 97 N.W., N.E., Si Ree 98 N.W.; 104 N.W., N.E., S.E.; 105 N.W., S.W. ; 106 NW., N.E.. and Suffolk. Quarter-sheets 89 S.E. & 3 S8.E., ESS SEES SSS SSE 918.E.&5S8.E., 92 8.W. & 6.58.W., 928.E. & 658.E., ee ee of pe 93 8.E. & 7 8.E., 98 N.E. & 8 N.E., 98 8.W. & 8 8.W., een ae ele 98 S.E.& 8S.E., 99 N.E. & 9 NE, 99 S.W. &9S.W,, em eg eg a ee ee ee 100 N.W. &10 N.W.,1038.E.&14 S.E., 108 N.E.& 22 N.E. Northamptonshire. Quarter-sheets 29 N.E.,S.E.; 30 N.W., N.E., 8.W., S.E.; 31 N.E., 8.W., S.E.;.328.W., S.E. ; 36 N.W., N.E., S.W., S.E.; 37 N.W., N.E., 8.W., S.E. ; 200 ADDITIONS TO THE LIBRARY. 38 N.W., N.E., S.W., S.E.; 40 N.W., N.E., S.W.; 43 N.W., N.E., S.W., 8.E.; 44 N.W., N.E.,S.W.; 45 S.E.; 46 N.W., N.E., S.W., S.E.; 47 N.W., N.E.; 49 S.E.; 50: N.W.) NE, S.W., 5:2 ol NW. N_ES SW. 5 Bee 52 N.W., N.E., S.W., S.E.; 53 N.W., N.E., SW.; 54 N.W., N.E., S.W., 8.E.; 55 N.W., N.E., 8.W., S.E.; 56 NW. ; 58 N.W., NE; 59 8.E. ; 62 N.W., ate SE. Northamplonsbired Warwick. Qu.-sh. 59N.W.& W.&29N.W., 29 S.W. & 29 S.W., 35 N.E.& 35 NE N.E., 35 S.E.& 35 SE. S.E., SS ee ee ee eS See 42N.E. & 41 N.E., 42 8. W. & 4158.W., 42S.E. & 41 S.E., 49 N.W. & 47 N.W., 49 N.E. & 47 N.E., 49 S.W. & 478. W.., —_em@~ ——————————————e 92 S.W.&658.W., 99 N.E. & 9 NE. Nottinghamshire. Quarter-sheets 18 N.W., N.E., S.W., S.E.; 19 N.W., N.E., S.W., S.E.; 20 N.W., S.W.; 23 N.E., S.W.., SE. ; 24 N.W.. N.E., 'S.W., S.E.; 25 NW. NE. S.W., S.E.; 26 S.W.; 28 N.E., S.E.; 29 N.W., NE, S.W., SE; 30 N.W., N.E., S.W., SE. ; oe N.W., S.W.; 33 N.W., N.E.; 34 N.W., NE, S.W., S.E. ; 35 N.W.. S.W., S.E.; 36 N.W., S.W.; 39 N.E.; 41 N.E., S.E.; 44N.W.; 47 N.W., S.W.; 50 N.W. Mo and Derby. Quarter-sheet 32 N.W. & 41 N.W. — and Leicester. Quarter-sheets 41 8.W. & 3258.W., ee 50 N.E. & 11 N.E., 508.W. &11 8.W., 50 8.E. & 1158.E., SS SS SSE 51 N.W. & 12 N.W., 56 N.E. & 45 N.E. =. and Lincoln. Quarter-sheets 28 N.E. & 68 N.E., See ee D1 NE. & 69 N.E., 21S8.E. & 69 S.E., 53 N.W.& 28 N.W. Oxfordshire. Sheets 21, 26, a pity — and Berkshire. Sheets 37 a nad 4, 46 and 11. a8 and Buckinghamshire. Sheets 28 fe and 1d 24, 50 panes —— 2 53 and 50. and Wiltshire. Sheet 36 and 2a. Rutlandshire. Quarter-sheets 3S8.W., S.E.; 5 N.W., N.E., S.W., S.E.; 6 N.W., N.E., S.W., S.E. Shropshire. Quarter-sheets 1S.E.; 4S.W.; 5 N.E., S.W., S.E.; 68.W.,S.E.; 75.W., SE. ; 8N.E., SE. ; 9 N.W., N.E., S.W. ; 11 NE, S-E. ; 12 NW., S.W.; 13 N.W., NE., S.W., S.E. ; 14 N.W., N.E., S.W., S.E.; 15 N.W., NE. SWi 36 16. NE S.Was “LA SLW.5 AS UNE So N.E., 8.W., S.E.; 20 N.W., N.E.; 21 N.W., N.E., 8.W., S.E.: 22 N.W., S.W., S.E.; 23 N.W., N-E., S.W., S.E.; ADDITIONS TO THE LIBRARY. 201 24 N.W., S.W., S.E.; 25 N.E.; 268.W.; 27 N.W., N.E., S.W., S.E.; 28 N.W., N.E., S.E.; 29 N.W., N.E.; 30 N.E., S.W.; 31 N.W., S.W.; 34N.E., S.W., S.E.; 35 N.W., 5.W., S.E.; 36 N.W.; 40S.W.; 438 S.W.; 49 Nese to Nokes, (Oo N.E.: -76 Ne SoWig 8.Bas 79 N.E., 8.E. Shropshire and Herefordshire. Quarter-sh. 77N.W.&2N W., Jet SS ee oe Oe ee eee (CNH 2 N.E., 77 SW. & 28.W., 78 NW. & 3 NW., SSS EE 78 N.E. & 3 N.E., 738 SE. & 38.E., 79 SW. & 458.W., ————— 82 N.W. & 7 N.W., 83 N.W. & 8 NW. SS —— and pe ety’ shire. Quarter-sh. 53 S.E. & &37 S. i 61 N.E. 1 &44NE, 618.W. & 445.W., 618.5. & 44S.E, 68 N.W. & 49 N.W. Somersetshire. Quarter-sheets 18.E.; 2 N.W., N.E., S.W., S.H.;0.W.: 4.N.W., N.E., S.W.;, S.E.; & N.W., N.E:. owes. Hes- 6 NW: N.E., “SiW., SB: 7 NW., NB. SB. Wis. ; 8 N.W.,8.W.,.8.H.;-10 NOW., NE, S.W., Selina NW. NOES. W., S.K.s 12 NW..N.K.. 5. We, S.E.; 13 N.W., N.E., S.W.,8.E.; 14. N.E.,S.E.; 16 N.W., Sai oon. 7 NW. Sins; £8 NW... N-R: 8S. W., S.Be: 19 N.W., N.E., S.W:, S.E.; 20 N.W.; S:W.: 21 N.W., N.E., S.W., S.E.; 24 N.E., S.E.; 25 N.W., N.E., S.E. ; 25 NeW. NESE. 3-2 f NW.,, N:E.,. S.W.,. S.B.; 28 NEW... ON. 29) NES SE: = 30 NW. .N.E: 3) 31 N.W.: 42 N.E., S.E. Staffordshire. Quarter-sheets 2 8.W.; 3 S.W.; 7 N.E.; SN.W.; 10 N.W.; 128.E.; 15S8.E.; 318.E.; 32N.W., SeW.5 oO b.h.>, 39 Nowe; 40 N.W., S:W.; 45 N.ES S.W., S.E.; 445.W.; 45 N.W.; 46 N.W., N.E., S.W., SH. 3 4/-N.W.5, 49 NOW. NES S.W.; 50 NES SAW SH; Oo UN. : od S.W.; 6! N.W., N-ES SW. SB: 66 N.W., N.E.; 68 N.E., S.W., S.E.; 70a S.E. ————— re and Derbyshire. Quarter-sheet 14 8.E. & 378.E. ———— 7 and Warwickshire. Quarter-sheets 59 S.E. & 2 S.E., eS SS ee eee 64 N.W. & 4N.W., 64N.E. & 4 N.E., 648.W. &48.W., 65 N.W. & 5 N.W., 65 N.E. & 5N.E,, 69 N.W.&80.W., SS eet SS 71 S.W.& 68.W., 73 N.E. & 7 N.E., 748.W. & 8 S.W. Suffolk. Quarter-sheets 10 S.E.; 17 N.E.; 22 S.E.; 23 N.W., S.E:;\ 27 N.W.; 32 N:E.S.H.; 33 N.W.., S.Ees 34 8.E.; 38 N.W., 8.W., S.E.; 39 N.E., S.E.; 40 N.W., S.W.; 43 N.E.; 44 N.W., S.W.,S.E.; 45 N.W., N.E., S.W., S.E.; 47 N.W., N.E., S.W., S.E.; 48 N.W., N.E., 202 ADDITIONS TO THE LIBRARY. S.W., S.E.; 49 N.W.; 50 N.W., SE.; 51 N.W.; 53 N.E., 8.E.; 54.N.E.,8.W., S.E.; 55 N.W., NE, S.W., S.E.; 56 8.W., S.E.; 57 N.W., N.E., S.W., S.E.; 58 N.W., N.E., §.W., S.E.; 59 N-E., S.W., S.E.; 60 8.W.; 63 N.W., N.E.,8.W.,8.E.; 64.N.W., N.E., §.W., S.E.; 65 N.W., N.E., 8.W.; 66 N.W., N.E.; 69 N.W.; 70 S.W.; 748.W.; 75 N.W., NE, S.E.; 76 N.W., NE; 82 N.W., N.E.; 85 N.W. —_ a ##[{T?————-"_ Suffolk and Cambridgeshire. Quarter-sh. 31 N.E. & 36 N.E., eee 318.W. & 368.W., 318.E.& 36 8.E., 328.W. & 37 8.W., Se ee 42 N.E. & 42 N.E., 42 S.E. & 42 S.E. and Norfolk. Quarter-sheets 2 N.W. & 78 N W., ee AS.W. & 9058.W., 75.W. & 938.W., 9 S.E. & 99 S.E., —————- 2 qt oe. ___—___. 10 8.W. & 100 8. W., 17 N.W. & 107 N.W. Warwickshire. Quarter-sheets 17 N.W.; 50 S.W.; 57 S.W. ; —— & Worcestershire. Quarter-sheets 24 N.W. & 31 N.W., 30 N.E: & 23 N.E., 308.E. & 23 S.E., 36 N.E. & 30 NE, 36 S.E. & 30 8.E., 42 N.E. & 35 N.E., 48 N.E. & 42 N.E. Worcestershire. Quarter-sheets 8S.E.; 9 N.E.,S.W.,8.E.; 10 N:W., N.E.,S.B. 12 NOE. SW. 8: bee 13 NeW NEw. Wi, 58a; 1a 5B 16 8 Wes 18 Nuns Sho N.W., N.E., S.W., S.E.; 20 N.W., N.E., S.W.,S.E.; 21 N.W., S.W., S.E.; 22 N.E.,S.W., S.E.; 28 N.W.,S.W.; 25 N.E.; 26 N.W., N.E.; 27 N.E.,8.W., S.E.; 28 N-W., N.E.,.8.W.; 29 N.W., N.E.,S.W.,S.E.; 30N.W.,S.W.; | 3bS.K.5 32 NAV. NE S.Ws 8. E.e co NW INeWe : 34 N.W.,. N-H;, S.W.;- 5.4; 35 58.W. 3 38N. E239 q NW. : 40 0NCW.,, N.EG Se AL NOWo INCE SW. q S.E.; 42 8.W.; 48 N.E. and Gloucester. Suances 48 S.W. &5 S.W., 48 SE. &5 S.E., 49 N.W. & 6N.W., 50 N.W.&7 NW. 50 N.E. & 7 N.E., 508.W. &78.W., 508.E.&7 SE, 54 NE. & 11 NE. ——., Warwickshire, and Gloucestershire. Quarter-sheets I OS ee 43 N.W., 49 N.W., &3N.W.; 44N.E., 50 NE, &4 NE. Paris. Dépdt de la Marine. 15 Sheets of Charts and Plans of various Coasts, &c. Russia. Geological Commitice. Sheet 71. zsp'5n0- ADDITIONS TO THE MUSEUM. 203 Russia. Geological Committee. Geologische poe des Ostabhanges des Urals, von A. Karpinsky, in 3 sheets. = 55), 420000° Saxony. Geologische Landesuntersuchung des Konigreichs Sachsen. Geologische Specialkarte. Blatt Mutzschen, 29; Kirchberg, 125; Zoblitz, 129; Schwarzenberg, 137; Eibenstock, 145; Wicsen- thal, TAT: ssp: Sweden. Geologiska Undersokning. Ser. A. a, 88,91. szp45a5- ase (ee a 000° Karta ofver berggrunden inom norra delen af Kalmar lin Se pa bekostnad af lanets norra Hushallnings Sillskap. ’ F00000" . ——. Geologisk Ofversigtskarta dfver Sverige. Sdédra bladet. poo Switzerland. Geological Commission. Sheet 18. y55505- Il. ADDITIONS TO THE MUSEUM. Specimens illustrating the paper on the Serpentine of Porthalla Cove, in Q. J. G. 8. vol. xl. p. 458. Presented by J. H. Collins, Esq., F.GS. Two slides with Cretaceous Lichenoporide, illustrating the paper in Q. J. G. S. vol. xl. p. 850. Presented by G. R. Vine, Esq. Casts of Footprints in the Lower New Red Sandstone of Penrith, illustrating the paper in Q. J. G. 8. vol. xl. p. 479. Presented by G. V. Smith, Esq., F.GS. Specimens illustrating Mr. A. W. Waters’s paper on Chilostomatous. Bryozoa from Muddy Creek, Victoria (Q. J. G. S. vol. xxxix. p. 423). Presented by J. B. Wilson, Hsq., of Geelong. A specimen of Fulgurite from Mont Blane, illustrating the paper in Q. J. GS. vol. xli. p. 152. Presented by F. Rutley, Esq., F.G.S. 204 ADDITIONS TO THE MUSEUM. Ten Sandworn Stones from Hokitika, New Zealand. Presented by _W. D. Campbell, Esq., F.GS. Six slides of Cyclostomatous Bryozoa from Muddy Creek, South Australia, illustrating the paper in Q. J. G.S. vol. xl. p. 674. Presented by J. B. Wilson, Esq., F.GS. vif i; ir yh) ‘ i} ae Bas es dee ens See * 7 %: @i oy DY ° a ‘6 . ° ee \@. ee “iit vA Le Y ae Pith. paeme e, “a Yi tad y o lL ” w x < re a - z Q ke r=) E | oe o = z < z ie} 7) xr E = 7) — Ge . t as cap + - ent =e : oS re