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AWARD OF THE WOLLASTON MEDAL AND DonaTIon Funp. THE preceding Reports having been read, the President, Masor- GENERAL Porttock, addressed the Meeting as follows :— The Report of the Council has pointed out that its Members have on this occasion awarded two medals, thinking it desirable to mark, without delay, their high appreciation of the great merits of two most distinguished men, who, labouring in countries very distant from each other, have contributed largely to our knowledge of the ancient Na- tural History of the earth. The first Medal has been assigned to a veteran Palzontologist, Hermann von Meyer, who commenced his labours twenty-three years ago by investigating the principle of determining the order and classi- fication of mineral deposits by their natural-history relations, From that time he has been engaged in an uninterrupted course of Palzeon- tological inquiries of the most varied nature, and he has become one of the leading authorities upon the subject in Germany. Sixteen years ago he was associated with Germar, Count Minster, and Professor Unger in that important work ‘ Beitrage zur Petrefaktenkunde,’ or Contributions to the Knowledge of Fossils, which was rich in ever branch of organic remains, whether animal or vegetable; and I find in the fifth part the description of a species of Pterodactyle, Ptero- dactylus Meyeri, discovered by Von Meyer himself, and named by Minster after his able coadjutor. Fossil Fishes and Fossil Plants were equally the subject of discussion in this able work, which ex- tended to seven parts. He was associated with Plieninger in de- scribing the paleeontology of Wiirtemberg, and he is now engaged with Dunker in publishing a general ‘ Paleeontographica,’ which has already recorded many interesting discoveries in this most rich and fascinating science. It will, I am sure, therefore, be felt that we are only doing justice to the claims of a man who has produced no less than 57 treatises upon Paleontological subjects, not one of which can be considered undeserving of respect and attention. Sir C. Lyevzy,—lIt is with great pleasure that I place the Medal VOL. XIV, € XXil PROCEEDINGS OF THE GEOLOGICAL SOCIETY. in your hands, requesting that you will convey to M. Hermann von Meyer our high appreciation of the value of his labours, and our gratification at conveying it to him through one so fully able to value the services of a great Palzeontologist. Sir C. Lyext thus replied :— Mr. President,—It will give me great pleasure to take charge of the Medal which has been awarded by the Geological Society of London to my friend M. Hermann von Meyer. The importance of his Paleontological labours is now, as you have truly stated, universally acknowledged ; but for my own part, I con- fess that I should scarcely have been aware of their vast extent had I not enjoyed opportunities of visiting Frankfort from year to year, and seeing the author engaged in his preparations for those mono- graphs on fossil reptiles with which he has enriched our science. 1 see that one of the most splendid of these elaborate treatises, which contains I believe descriptions and illustrations of about 80 species of Triassic Reptiles, is now lying on our table—a work of which it is not too much to assert, that it would have secured a very high repu- tation for its author had it been the only labour of his life. For this and for his other publications, M. von Meyer has executed all the drawings with his own hand, and has done them all on transparent paper, so that his lithographer, when transferring them to stone, has not had to reverse the figures—a process during which the spirit and accuracy of the originals are often found to suffer. Allow me, Sir, in conclusion, again to express to you the satisfac- tion I feel at being requested to transmit this well-earned tribute of our esteem to one of the most distinguished of our Foreign Members. The PresipENT proceeded :— __ | The Council has awarded the second Medal to Mr. James Hall, of New York, as a testimonial of its high opinion of his merits as a pa- leontologist and geologist. Twenty-one years ago Mr. Hall exhibited his taste for paleontology by describing two species of Trilobites be- longing to the genus Paradowides, a genus very remarkable in its con- formation, and which our friend Mr. William Rogers has lately dis- covered in a highly metamorphosed rock, long considered a crystalline schist, near Boston. Huis notes upon the geology of the Western States soon followed as a testimony to his love of pure geology ; but the paleontology of New York proved him to be worthy of the re- “spect of all lovers of natural science. He has gone steadily forward, and we are now indebted to him for an accurate knowledge of the geology and paleontology of the great State of New York, which is in itself equal to a large kingdom in magnitude. The last of his works, ‘‘ Descriptions of New Species of Paleozoic Fossils from the Lower Helderberg, Oriskany Sandstone, Upper Helderberg, Hamil- ton, and Chemnung groups,”’ published last year, is full of descriptions of new species ; and, although I am myself prone to hesitate respect- ing new species when closely allied to previously known species, the ANNIVERSARY MEETING.—WOLLASTON MEDAL. XXxili work proves the continued energy and ability of Mr. Hall in his fa- vourite study. To me it has always appeared, that the history of any of the past epochs of the earth’s history may best be studied in countries which have not undergone any great disturbance during its continuance. In England, from its insular position, it is easy to observe that numerous disturbances must have interfered with the tranquil course of events, whilst in large continents, such as America, and a large portion of the continent of Europe, such as Russia, &c., little comparative disturb- ance may be looked for, and the succession of organic existences may be supposed to have gone on under the influence of ordinary and natural causes alone. Such considerations as these are the more interesting at the present moment as Sir R. Murchison has lately been enabled to establish the Silurian age of certain rocks in Scotland, by the dis- covery in them of Silurian fossils, not of the English type, but of the American type, amongst which may be mentioned the genus Maclurea, so called after one of the first writers on American Geology, the well- known Mr. Maclure. This curious fact adds to our interest in the award of this Medal, which we wish to be considered as a testimony of the high respect which our Society entertains for the labours of American geologists, and especially for those of Mr. James Hall. I should have felt much pleasure in transmitting the Medal through Professor Ramsay, who during the last summer represented our So- ciety at the Meeting of American Naturalists in Canada; but in his absence, I naturally turn to you, Sir Roderick Murchison, as the natural leader on every question relating to the Silurian Formation, and. who would have been our representative in America had you not found it necessary, from ill-health, to decline the pleasing duty in fa- vour of Professor Ramsay, who may be considered almost your pupil. Let me then request you to undertake the task of conveying the Me- dal to Mr. James Hall, and expressing our high respect for him and his labours. The Council has added the proceeds in the hope that the sum, though small, may be of use to Mr. Hall in the publication of his fossils. In reply Sir R. Murcuison said :— _ Sir,—Although I am unexpectedly called upon, through the acci- dental absence of Professor Ramsay, to receive the Wollaston Medal for Mr. James Hall, I beg to assure you, that no one of my country- men can more truly rejoice than I do in the adjudication of the highest honour this Society can bestow, to so eminent an American geologist, In my earnest desire to have visited the United States and Canada last summer—a desire which was alone frustrated by the state of my health,—my chief gratification would have been to have examined, under the guidance of James Hall, those great expanses of the Silu- rian and other palzozoic rocks of the Western Continent which he has so truthfully and ably described ; for it is he who has shown us that, however widely separated by the Atlantic, the fossil remains of the earliest traceable living things in the New World have, like the present inhabitants, the strongest relationship with the old country. Permit | ee ae XXI1V° PROCEEDINGS OF THE GEOLOGICAL SOCIETY. me, Sir, also to say, that the high estimate of the merits of our medallist, which I have imbibed, both from a study of his own works and by reference to the opinions of Lyell, De Verneuil, and Logan, has been much strengthened by the animated reports of Professor Ramsay, who since his return has lost no opportunity of recording the deep sense he entertains of the very important services rendered to Geological science by the arduous and meritorious researches of James Hall. THE ANNIVERSARY ADDRESS OF THE PRESIDENT. Proceeding now to the more special duty which devolves on your President this day, I have once more to perform the melancholy task of recalling to your memory the names of those Fellows of our Society who have been removed from amongst us, by death, during the year; and it is with sorrow that I find how erroneous was the hope I entertained last year, that the very magnitude of the losses I then commemorated would insure me from having to dwell in the present year, for any length of time, upon so sad a subject. It was indeed scarcely to be expected that we should have been, as a large Society, entirely exempted from the common lot of humanity; but the blow has fallen most heavily upon us, and amongst our losses we have to record the names of men distinguished in almost every branch of literary or scientific lore. The first I shall notice was indeed a patriarch of our science, one of those illustrious men who assisted at the very birth of Geology amongst us, one who was long looked up to as a sure guide in the path of truth and science. You will at once perceive that I allude to the late Dean ConyBrarz, who last came amongst us only a very short: time before the summer recess, when he appeared to take as lively an interest as ever in the proceedings of the Society he had once cheered by his frequent attendance, and adorned by his labours ; and as he was going away he assured me that it was always with pleasure and satisfaction he came to meetings from which duty and distant residence could alone keep him away. . It has been justly said that he was one of a race of clergymen, and those men of intellectual eminence. His grandfather was Dean of Christchurch and Bishop of Bristol, the friend of Bishop’ Berkely, and the author of a work distinguished even in an age of deep thinkers and profound theologians, and entitled ‘The Defence of Revealed Religion.? The Bishop’s only son, Dr. Wiliam Conybeare, Rector of Bishopsgate, left behind him two sons, both of whom were eminent men. The elder, John Josias, Vicar of Bath Easton, was an accomplished scholar, no inconsiderable chemist, a sound geologist, and filled with credit the University offices of Professor of Poetry and of Anglo-Saxon, as well as that of Bampton Lecturer: he pro- moted the revival of Saxon literature, and left behind him, on his death in early life, a volume of translations which it was his brother’s office to complete and edit. That brother, the second son of Dr. William Conybeare, was the illustrious object of this notice, ANNIVERSARY ADDRESS OF THE PRESIDENT. XXV- William Daniel Conybeare: he was born in June 1787, and in due time sent to Westminster School, where he received his early edu- cation. From Westminster he proceeded to Oxford, and entered Christ Church in the same year as his fellow collegian Sir Robert Peel, taking a first class in classics, in which he was classed with Sir Robert, and a second class in mathematics, in which he was classed with Archbishop Whately. Until he took his M.A. degree, he continued to reside at the University, pursuing various studies, and assisting by his exertions to lay the foundation of Geology, which was then only a rising science. At the early portion of the present century, an indifference, such as we can now scarcely understand, as to the cultivation of the natural sciences prevailed at Oxford; but, in the midst of the consequent general neglect, a small band of indi- viduals, residents of the University, were united in the effort to keep alive a taste for at least one branch of natural science, and succeeded in enlisting others in its cause. The first lectures given at Oxford on Mineralogy, which was then as a study not accurately distinguished from Geology, were, it is believed, those delivered by Sir Christopher Pegge, then Regius Pro- fessor of Medicine ; and although it may not be possible, either from written records or from the personal testimony of any one now living, to form an accurate opinion of the merits of those lectures, it may be fairly assumed that they were not destitute of attractiveness, as the same individual delivered long afterwards lectures on Anatomy, remarkable for an elegance and a fluency of diction which have caused them to continue fresh in the recollection of many. Sir Christopher Pegge was succeeded by Dr. Kidd, who for several years gave courses of lectures at Oxford on both the allied sciences, Mine- ralogy and Geology, and collected around him a knot of persons interested in similar pursuits, who formed themselves into a little club of Oxford Geologists. This club included amongst its mem- bers the late Dr. Buckland, the two brothers Conybeare, the late Rev. Philip Serle, of Trinity College, afterwards Rector of Adding- ton, Oxford, and many others, who, though less vigorously devoting themselves to geological research, were still, from their eminent qualities and high character, most instrumental in keeping alive the ‘growing interest for the new science, and in raising the cha- racter of the club so high, that some of the early members of the Geological Society of London, then in its infancy, amongst whom “were the late Mr. Greenough and the present patriarch of our science, Dr. Fitton, were in the habit of paying an annual visit in Whitsun- week to the University, in order to explore, under the guidance of the geologists of Oxford, the physical structure of the rocks in its neighbourhood; whilst, on their part, they thus judiciously enlisted local inquirers in the service of general geology. The venerable Principal of Magdalen College, Dr. Macbride, ‘is the only survivor, at Oxford, of this memorable club, and he preserves at ‘an advanced age the vigour of his faculties, and exhibits all his former “interest in the progress of learning and of science; but of non-resi- dents, there still survive Archdeacon Hony, now Prebendary of Sarum, XXV1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. and Mr. Philip Duncan, who now resides at Bath: the latter and his brother, Mr. John Grant, were Fellows of New College, were honoured by the degree of D.C.L., and were remarkable, not only for their love of natural history, but for their zealous support of every philan- thropic and scientific object. The Rev. Wiliam D. Conybeare was, however, in the first rank of this little body, and stood so high in the estimation of all its members, that Dr. Buckland, when first lecturing as the successor to Dr. Kidd, expressed in the warmest terms his sense of the obligations he owed to him for the information he had imparted on points relating to geology, and his persuasion that it would not have been fitting for him to offer himself to fill the office of lecturer on that subject, had Mr. Conybeare been desirous to occupy it. Let me add here, that another equally eminent individual, the founder of the new school of geology at Cambridge, as Dr. Buckland was of that of Oxford, has assured me, with a similar frankness, so characteristic of Professor Sedgwick, that he too looked upon Dean ’ Conybeare as his early master in geology. In 1814 Mr. Conybeare married, and retired from the University, the scene of his early triumphs, to undertake the quiet work of a country curacy, and nine years afterwards removed to the vicarage of Sully in Glamorganshire, on the presentation of the late Evan Thomas, Esq., his brother-in-law ; but, whilst holding the curacy of Banbury and Lectureship of Brislington, near Bristol, he had been mainly instrumental, in conjunction with Sir Henry Delabeche, in founding the Bristol Philosophical Institution and Museum, and it was at that time he received a visit from the great French geologists, M. Elie de Beaumont and M. Dufrénoy, who came for the purpose of acquiring a knowledge of the secondary rocks of England, as a standard of reference for those of France; and he so impressed them, whilst acting as their companion and guide in an exploration of the neighbourhood, with a deep sense of his geological knowledge, that they were prepared on their return to cooperate with Cuvier in ob- taining the election of Mr. Conybeare as a corresponding member of the Institute, for Geology. Nor must it be supposed that this excel- lent man neglected his sacred duties whilst storing his mind with the richest treasures of geological research, as it was during his resi- dence at Sully that he delivered, gratuitously, at the request of his friend Dr. Prichard, a course of theological lectures at Bristol College, of which institution he had become a visitor. In 1836 he left Sully and went to Devonshire, having presented himself to his family living of Axminster, and, whilst there, preached, at the request of the authorities of the University of Oxford, the Bampton Lecture for 1839. The living of Axminster he resigned after a few years, on being called by his friend Bishop Copleston to the care of the Cathedral of Llandaff. Here he continued zealously to carry on the good work of restoration which had been com- menced by his predecessor Dean Bruce Knight; and, as at all times in his life, was ever ready to distribute the rich and varied stores of his mind for the benefit of his fellow-men, in whatsoever station of life they might have been. This venerable, much-loved man, and ANNIVERSARY ADDRESS OF THE PRESIDENT. XXVi admired philosopher, left Llandaff to attend the death-bed of his eldest son, and, whilst pausing in his return, at the house of an- other son, was stricken with pulmonary apoplexy, and died on the morning of the 12th of August, after an illness of only three hours, in the 71st year of his age. Such is the general picture of the life of a truly estimable man ; and I shall now add to it a very brief notice of his most characteristic works, premising, however, that, even before the peace of 1815 had opened the Continent to British geologists, Mr. Conybeare had formed, from the imperfect data then within his reach, a sound opinion as to the identity of the Jura limestone with the oolitic formations of Eng- land, an anticipation which he had afterwards the gratification, in conjunction with Dr. Buckland and Mr. Greenough, of verifying. The versatility of the genius of Dean Conybeare led him to examine and describe the lesser points connected with organic remains, as well as the greater; a circumstance in which he strongly resembled his friend and fellow-labourer Dr. Buckland. For an exemplification of this peculiarity of his mind, I shall refer to his paper published in the year 1814, in the second volume of the Transactions of the Society, and therefore one of his early contributions to Paleonto- logical Science. It was entitled, “On the Origin of a remarkable Class of Organic Impressions occurring in Nodules of Flint.” Mr. Parkinson had described them as “small round compressed bodies, not exceeding the eighth of an inch in their longest diameters, and horizontally disposed, connected by processes nearly of the fineness of a hair, which pass from different parts of each of these bodies, and are attached to the surrounding ones; the whole of these bodies being thus held in connexion.” Mr. Parkinson considered that _ these bodies were the works of polypes, and he therefore classed them with corals of some unknown genera; and Dr. Buckland, who had directed his attention to them simultaneously with Mr. Conybeare, considered that the moulds in which the siliceous casts had been formed were the work of parasitic insects, the thin hair-like appendages having been the passages of entry first made by the in- sects, and the larger flattened bodies the cavities afterwards excavated, the object of the excavation having of course been to obtain nourish- ment from the body thus eaten into, whether a shell or any other. This observation of Dr. Buckland was communicated to Mr. Cony- beare, but not until he had completed his own researches, and arrived at the same virtual conclusion,—namely, that “these cellules were the works of animalcules preying on shells and on the vermes in- habiting them.” In arriving at this conclusion, Mr. Conybeare was guided by the examination of various fragments of shells, still pre- served in contact with the siliceous matter which had subsequently been infiltrated into the cavities produced by the boring animal. ‘These appear to have been portions of shells distinguished by a striated texture, and were stated by Mr. Conybeare to resemble in structure the recent Pinna marina, as the genus Inoceramus does; but in addition to these, Mr. Conybeare found them connected with other shells, and even with an Hchimus anda Belemnite. Though XXVlli PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Mr. Conybeare spoke with diffidence of his having brought before the Society a paper on such minute palontology, it cannot be doubted that the interest connected with the discovery of the existence and workings of minute marine animals at so remote an epoch is of a very high order. The flints and other siliceous deposits of the chalk and other geological epochs, have indeed been striking examples of the effect of judicious investigation in rendering the most obscure objects the means of throwing light upon natural phenomena. Mr. Conybeare was fully aware of the necessity of studying phy- sical as well as organic phenomena in connexion with geological science; and it is truly surprising how often the intimate connexion of the physical geography of remote epochs with their natural his- tory is overlooked. His description of the land-slip which occurred on the coast of Culverhole Point, near Axmouth, in December 1839, - was ably illustrated by a series of lithographic plates from the draw- ings of the present Lieut.-Colonel Dawson ; and the magnitude of the results was well expressed by the following words :—“ Although this convulsion can only be ascribed to the less dignified agency of the land-springs constantly undermining the sub-strata, yet, in the grandeur of the disturbances it has occasioned, it far exceeds the ravages of the earthquakes of Calabria, and almost rivals the vast volcanic fissures of the Val del Bove on the flanks of Aitna.” With- out doubt these phenomena are very striking and interesting in themselves; but they become still more so when we reflect, as Mr. Robert Mallet has taught us to do, that they ought not to De con- fined to the existing epoch alone, but should be sought for in the stony records of past ages.. The paper on the Hydrographical Basin of the Thames, written with a view to determine the causes which had operated in forming ,the Valleys of the Thames and its tribu- tary streams, is equally valuable as tending to maintain the value of attending to physical geography in geological investigations. His examination, also, of the Theory of Mountain-chains, then recently propounded by M. Elie de Beaumont, as well as his remarks on the phenomena of geology which most directly bear on theoretical specu- lations, are proofs of the truly philosophical and enlarged view he took of his favourite science. In noticing the works of Dr. Buckland, I have already detailed the importance of the paper which was compiled by him in conjunction with Mr. Conybeare, on the Bristol and South Welsh Coal-fields ; one, as I then observed, of those elaborate and comprehensive papers which were the fitting work of the first pioneers of geological science, and the difficulty of which can scarcely be appreciated in these times when the foundations of the science have been fairly laid, and geo- logists have only to improve or correct the details. His remarks on the sections of the Antrim and Derry coast were also a conjoint work, and of much interest. Another and equally remarkable work was that nadentaeeme in con- junction with the late Mr. William Phillips, namely, the ‘ Outlines of the Geology of England and Wales,’ as it may be considered the first systematic work on the subject ; and, though geology has been since ANNIVERSARY ADDRESS OF THE PRESIDENT. XX1X more specialized and studied in minuter detail, this work will always be regarded as a striking proof of the ability and knowledge of the authors. It was, however, in 1821 (April 6) that Mr. Conybeare commu- nicated to the Society that remarkable Paleontological paper which excited so much interest at the time, and established in the most satisfactory manner the propriety of establishing a new genus of Rep- tila, forming an intermediate link between the Ichthyosawrus and Crocodile, to which Mr. Conybeare gave the name of Plesiosaurus. The discovery of immense vertebree of oviparous quadrupeds in the Lias near Bristol had attracted the attention of Mr. Conybeare, who quickly recognized the difference between those belonging to the Ichthyosaurus and others, which evidently, in his opinion, were por- tions of a different animal. With a singular acumen and rare sa- gacity, he placed the detached vertebree in their proper position, and finally established his new genus, for which he adopted the name Plesiosaurus, as expressing its near approach to the order Lacerta. For the whole group of animals which approximate, on the one hand, to the Crocodiles in general organization, and yet have been provided with such specific organs as were necessary to enable them to live, at least principally, m the sea, Mr. Conybeare proposed the name Enalio-sauri, as a classic appellation for the whole order; and he observes of the genera composing it, that even the Jchthyosaurus, which recedes most widely from the forms of the Lizard family, and approaches nearest to those of fishes, exhibits in its osteology a beau- tiful series of analogies with that of the Crocodile, and which widely remove it from fishes. - In this paper he then described in the minutest detail the osteology of the Ichthyosaurus, and exhibited a knowledge of anatomy which excited the admiration of every one. He then examined with equal care the relics of the new genus, which, although at that time not complete, were sufficient to enable Mr. Conybeare to conclude that the vertebral column recedes from that of the Jchthyosaurus in all the points in which the latter approaches to the fishy structure, and that the invertebral substance must have been disposed much as in Cetacea; and that, from the locking together of the articulating pro- cesses, 1t must have had much less flexibility than in the Jchthyo- saurus or in fishes. In examining also such portions of the paddles as could be arranged in order, he comes to a similar conclusion in another direction, namely, that the paddles of the Plesiosaurus are intermediate in character between those of the Ichthyosaurus and the © Sea-turtles ; and thus in every respect he laid a sound foundation for his new genus. It is to be remarked that this paper was given as the joint pro- duction of Mr. Conybeare and Sir Henry Delabeche, to whom Mr. Conybeare most liberally ascribed a full share of the merit of the discovery; but, allowing Sir Henry every praise for his assistance in that discovery and in all the geological details, I believe the sa- gacity and skill exhibited in the osteological details and reasonings have always been ascribed to Mr. Conybeare. XXX PROCEEDINGS OF THE GEOLOGICAL SOCIETY. In a second paper, read May 3, 1822, Mr. Conybeare was enabled to describe much more fully all the relations of the genera Ichthyo- saurus and Plesiosaurus, from the discovery of other remains, both of the Ichthyosaurus and Plestosaurus, by his coadjutor Sir Henry Delabeche. A very minute examination of the teeth, especially, enabled him to point out that those of the Ichthyosaurus were more intimately related to the teeth of the Crocodile than to those of other Lacerte (an opinion then at variance with the opinions of some ana- tomists), whilst at the same time, in other respects, the analogy was in the other direction, for Conybeare observes, ‘‘in pursuing, how- ever, the history of the teeth of the Ichthyosaurus to the last stage, we quit these analogies with the Crocodile, and arrive at another point wherein the Jchthyosaurus resembles the other Lacertw, in com- mon with many of the Mammalia : this is, the gradual obliteration of the interior cavity in old age, by the ossification of the pulpy nucleus.” In conjunction with Sir H. Delabeche he brought up the number of species to four, determined from the teeth ; and in his further con- sideration of the genus it is right to notice the following remarks, proceeding from him after noticing a difference in one character of the fossil Crocodile, when compared with the recent, as stated by Cuvier :—‘‘I am persuaded, from every circumstance, that a much nearer approximation to the structure of the older lacertian genera will be found in the fossil than in the recent Crocodiles ; interesting links in the chain of Saurian animals will be thus supplied, and it will probably be found that many of the points in which the Jch- thyosaurus differs from the recent type are only instances of its agreement with the fossil.” The researches of Sir H. Delabeche had not at this time led to the discovery of a complete skeleton of thenew genus Plesiosaurus; but additional portions of it were found, including a very perfect dental bone of the lower jaw, whilst a tolerably perfect head was discovered by Mr. Thomas Clarke in the Lias of Street, near Glastonbury. The investigation of these new relics of the Plesiosawrus led Mr. Conybeare to the following conclusion: ‘‘On the whole then, the manner in which the ribs of the Plesiosaurus articulate throughout, by a single head, to the extremity of the transverse processes of the vertebree only, the structure of the humero-sternal parts, and the characters derived from the head, approximate this animal most nearly to the Lacerte. By its teeth, on the other hand, it is allied to the Crocodile ; while its small nostrils and multarticulate paddles are features in which it resembles the Ichthyosaurus.” This able paper he concluded with words characteristic of his natural modesty, after pointing out the difficulty of rendering anatomical details at once sci- entifically accurate and yet attractive to a general audience: “ I need not add how much these difficulties will be increased in the hands of a writer who must acknowledge that, while intruding on the pro- vince of the comparative anatomist, he stands on foreign ground, and, using almost a foreign language, is frequently driven to adopt an awkward periphrasis, where a single word from the i of a master would probably have been sufficient.” . ~_ ANNIVERSARY ADDRESS OF THE PRESIDENT. XXxi However some may at the time have been inclined to throw doubts upon the deductions of Conybeare, the ability and accurate discrimi- nation of the author were publicly recognized by the great Cuvier, who hastened to advocate his admission to the French Academy as a Corresponding Member for the Science of Geology; and I am sure that all living paleontologists will follow the example of the late well-known, and at that time so highly respected, Mr. Clift, in recog- nizing the great merits of Dean Conybeare, and considering him one of the principal founders of the science in this country. At the present moment it would be tedious and unnecessary to pass in review the whole of the long series of Mr. Conybeare’s geological works, nineteen in number ; and I shall point your attention therefore solely to that able “‘ Report on the Progress, Actual State, and Ulterior Prospects of Geological Science,’ which he presented to the British Association in 1832, at its meeting in Oxford, in which he treats the subject with the combined powers of the scholar and man of science, pointing out the remarkable analogy in the views of Leibnitz to those of many modern speculators on physical geology; the opinions of Hooke in respect to the hypothesis of the elevation of our continents by voleanic agency; the masterly observations of Smith, first made known in 1799, which, although not the first to originate the doctrine of a regular distribution of organic remains, yet reduced to certainty and order what had been before vague and conjectural; the gradual rise of the Tertiary Geology from its foundation in the admirable ‘ Memoir on the Basin of Paris,’ by Cuvier and Brongniart, published in 1811 ; the establishment of the Geological Society in 1808, and the labours of all the great men connected with it, including, amongst many others, Greenough, Buckland, Sedgwick, Fitton, Murchison, Dela- beche, Phillips, Scrope, Daubeny, and Lyell, together with those of foreign geologists, including the great Von Buch and Boué. That Report alone is sufficient to prove his masterly acquaintance with the history of his favourite science, and with all its bearings, whilst it marks the liberal spirit with which he entered into all geological inquiries. The advance of geology since that Report has been enormous ; and, if a period of twenty years from the publica- tion of Cuvier and Brongniart. had done so much in raising Tertiary Geology to a high position, may we not say that the result of the next twenty-five years has been still more remarkable, and has richly rewarded the continued and judicious researches of some of our most distinguished geologists, such as Lyell, Forbes, Prestwich, and Austen, whilst the elevation to which the Silurian system has arrived by the persevering exertions of Murchison is a monument of progress which we can scarcely hope will be equalled in that peculiar branch of geology in future times. The zeal of Dean Conybeare for geology never forsook him; and when obliged to visit Madeira on account of the health of his young- est son, he visited the Peak of Teneriffe, and studied the other vol- canic phenomena of the neighbouring islands. How deeply must we regret that his last days were embittered by sorrow for the death of another son, from whose funeral he was returning at the time of his XXXll PROCEEDINGS OF THE GEOLOGICAL SOCIETY. death! But so excellent a man, prepared for death by the strict per- formance of every christian duty during life; requires not the com- miseration of those who survive him; although all who recollect his air of gravity and of sincerity, which always made his words effective in commanding attention and respect, and in bringing home conyic- tion to the minds of his hearers, must feel how heavy a loss we have experienced. The next person whom I shall notice, though unquestionably not possessed of the same extensive range of intellectual acquirements as the illustrious individual of whom I have just spoken, was yet a most active, intelligent, and valuable member of our Society. Mr. JosHua Tromer was the eldest son of Joshua Kirby Trimmer (who was the eldest son of Mrs. Trimmer the well-known authoress), and was born at North Cray in Kent, on the 11th of July, 1795. When he was about four years old his parents removed to Brentford, Middlesex, in order to be near the authoress, who resided in that parish. Under the roof of that venerable and widowed relative, much of the early childhood of the subject of this memoir was passed. The attention of the authoress was first particularly drawn to this grandchild by accidentally hearing him explain to a younger member of his family, rules of christian conduct to be observed through life—rules which, being entirely approved of by Mrs. Trimmer, were scrupulously fol- lowed out by himself in his own life. His docile disposition and inquiring mind gained her especial notice and affection, and he was held up by her to her various juvenile descendants as one whom they would do well to endeavour to resemble. It was indeed recorded of him, in the published life of Mrs. Trimmer, “‘ that Sunday was to him a day of perfect felicity ; and whether he sat with his book under a tree, or examined with his venerable grandmother the beau- ties of the plants and flowers, his countenance shone with delight ; and in the winter, when such pleasures could not be recurred to, the day was still one of enjoyment, and never wearied him.” : His taste for the science of geology was innate: his aged mother, who survives to mourn his loss, well remembers that at a very early age, when he used to accompany her and the authoress in their walks, his chief delight was to ramble to the side of a river or of a canal in search of shells, which he would bring to the authoress that she might name them; and frequently when at home he would invite his mother’s attention to the organic formations on oyster-shells, expressing the strongest desire to learn their natural history. Though the favourite study of his life appears to have ori- ginated with himself, his daily converse with the venerable Mrs. Trimmer, who was emphatically “the child’s friend,” confirmed his early tastes, and assisted in training his mind for that keen observa- tion and searching inquiry which so characterized his subsequent geological pursuits ; and it is worthy of remark, that these two rela- tives in their separate writings, directed as they were to widely dif-. ferent subjects, arrived at the same inductive conclusion with refer- ence to eternal truth. The authoress, in a little publication entitled ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXII “The Knowledge of Nature, for the instruction of Children,” has this remark: “It is evident from the construction of every part of nature, from the noblest to the most insignificant, that they are all most ad- mirably formed ; they must therefore have been the work of some wise, powerful Being, infinitely our superior ;’’ whilst the closing words of her grandson, in his work on “ Practical Geology and Mine- ralogy,” are, ‘‘The structure of the earth, as well as the mechanism of the heavens, proclaims the Divinity of the Hand which made them. The one tells of power and wisdom displayed through the immensity of space, the other tells of the same attributes displayed through the immensity of time ; and thus every bone and shell and leaf disinterred from the dust of the earth leads our thoughts towards eternity and the world of spirits, and tells us that, though all things visible are subject to change, they are the work of one invisible and eternal Being, ‘ the same yesterday, today, and for ever.’ ” About the year 1806, young Trimmer was placed as a pupil with the Rev. William Davison, at that time Curate of New Brentford. Under that highly talented preceptor, he pursued his classical and mathematical studies with such diligence as to gain the esteem of his preceptor, which he retained until his decease in the year 1852. When about nineteen years of age, he superimtended for his. father some copper-mines in North Wales; whilst thus employed, he gained a practical knowledge of mineralogy. After several yéars he undertook for his father the management of a farm in Middlesex; and, being thus engaged for some years, he acquired during that period a portion of that knowledge of soils which in after-life he so prominently connected with geology. During this period of his life he continued to reside with his parents, and his evenings were not unfrequently spent in Scriptural study. When engaged in other reading, the poet Spenser was his especial favourite ; and his intimate acquaintance with every page of the “‘ Faérie Queene” may have fur- nished him in part with that great command of language, so frequently evident in his writings. In prose-writing his model was Addison, the elegance of whose periods he admired: not unlike that author, he wrote with the greatest facility, never pausing for ideas or for lan- guage to express them; and it was not his habit to reconstruct any sentence he had once written: he composed also with ease in poetry, and gave expression to his thoughts in flowing and harmonious verse, _ and at an early age translated from the Italian a considerable portion of Tasso’s “ Jerusalem delivered.” In the year 1825 he was again in North Wales, working for his father some slate-quarries, one of them situate at Bangor, and the other two between Snowdon and Caernarvon. At the latter town he established, by means of public subscriptions, a museum, to which he © gave many valuable organic remains, some of which he had met with when occasionally visiting Ireland, but the greater part he had long been engaged in collecting from the ossiferous deposits at Brentford. Whilst working these quarries, at which employment he continued for some years, he resided chiefly in the Vale of Nantlle, where he was occasionally visited by his friend the late Dr. Buckland, whom XXXIV PROCEEDINGS OF THE GEOLOGICAL SOCIETY. he would at such times guide with enthusiastic ardour over the Snow- donian range, pointing out to him from time to time the erratic blocks and marine shells on which he founded his opinion that they were not deposited, as had been supposed, by melting icebergs on the floor of a:sea, which after long submergence had been converted into dry land by movements of elevation, but that they were spread by marine currents of extraordinary energy and short duration over the surface of pre-existing land, and over land covered with ice. This opinion, however, he subsequently modified by accepting coast-ice as being probably an efficient agent im these circumstances. About the year 1840 he ceased to reside in Wales, and was for some time afterwards employed in the Government Geological Survey of England. He then returned to reside in his native county, Kent, in which he continued until the time of his decease. The last few years of his life were entirely devoted to writing on agricultural sub- jects in connexion with geology, more especially on the drainage of lands, in which he insisted on the following points :— in The important influence exercised by the superficial deposits on the distribution of soils. 2. The division of those deposits into erratic tertiaries, or Northern drift, and warp-drift. 3. The division of the erratic tertiaries again into lower and upper erratics,—the lower erratics consisting of boulder-clay, possessing pe- culiar characters found in no other marine strata ; the upper erraties composed of rolled gravel and sand, approaching more the characters of ordinary tertiary strata, but distinguished from them by certain marked peculiarities. 4, The distinctness of the warp-drift, a deposit which generally forms the surface-soil, and its subsequent origin to that of the erratic tertiaries ; its presence in those districts where the erratic tertiaries are absent, and its diffusion over their denuded surface where they are present. 5. The indented surface of the beds, whether of the erratic ter- tiaries or of the older strata, on which the warp-drift rests, present- ing a series of irregular ridges and furrows. 6. The suggestion that the contradictory statements which abound respecting the superior efficacy of deep or shallow drains, of drains at wide or narrow intervals, of drains following the fall of the ground, or crossing it, might perhaps, in many cases, be reconciled by ob- serving whether the drains were parallel or transverse to these natural furrows and ridges. Among the numerous publications of Mr. Trimmer may be men- tioned the following, which strongly mark the bent of his mind, and the practical objects he more especially had in view :— 1. On the Diluvial or Northern Drift of the Eastern and Western sides of the Cambrian Chain, and on its connexion with a similar Deposit on the Eastern side of Ireland, at Bray, Howth, and Glenis- maule. 2. On the Origin of the Soils which cover the Chalk of Kent. In two parts. 3. Practical Geology and Mineralogy, with an Intro- ductory Discourse on the Nature, Tendency, and Advantages of Geo- ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXV logical Pursuits. 8vo, with two hundred illustrations. 4. Practical Chemistry for Farmers and Landowners. 5. Proposals for a Geolo- gical Survey, specially directed to Agricultural Objects. 6. On the Geology of Norfolk, as Illustrating the Laws of the Distribution of Soils. 7. An Attempt to estimate the Effects of Protecting Duties on the Profits of Agriculture. 8. Supplement to the same. 9. On the Agricultural Geology of England and Wales. Prize Essay. 10. Notes on the Geology of the New Forest, in relation to its capa- bilities for the growth of Oak, and for cultivation. 11. On the Agri- cultural Relations of the Western Portion of the Hampshire Tertiary District, and on the Agricultural Importance of the Marls of the New Forest. 12. On the Southern Termination of the Erratic Tertiaries, and on the Remains of a Bed of Gravel on the Summit of Clevedon Down, Somersetshire. 13. On the Erratic Tertiaries bordering on the Penine Chain. In two parts. 14. The Keythorpe System of Land Drainage ; its Principles, Efficiency, Economy, and Opponents. 15, On the Geology of the Keythorpe Kstate. He was in the midst of preparing another work for the press, to have been entitled ‘ Soils, Subsoils, and Substrata; or, The Geology of Agriculture,’ when, whilst walking in London, he was seized with an illness which after a few days terminated fatally, on the 16th of September, 1857. The catalogue of Mr. Trimmer’s works is sufficient to show that he was a most zealous, active, and practically useful geologist. When first I had the pleasure of becoming acquainted with him, he was distinguished as an enthusiastic advocate of the diluvian theory of the drift, considering that great waves had been lifted up and carried over the pre-existing dry land, scooping out channels and depositing marine debris; but this advocacy of a peculiar theory in no way in- terfered with his examinations, which were always made with care, and detailed with honesty. In June 1831 and January 1832, he com- municated two short notices to our Society, on diluvial pheno- mena, as he then considered them, noticing the discovery of marine shells in diluvial sand on the summit of Moel Tryfane, near Caernar- von, 1000 feet above the level of the sea, and again, on a visit to Runcorn, the discovery of marine shells ina singular deposit, forming part of the banks of the Mersey. It consists of a series of beds :— Ist. Yellowsand, with some Bi but no shells, 3 to 6 feet thick; 2nd. Decayed vegetable matter, $ to 3 inches thick ; ord. A bed 14 feet thick, to Sel Soke mark, containing frag- ments of new red sandstone and erratic pebbles of various crystalline and other rocks, associated with a few blocks, of great weight, up to a quarter of a ton; and in this bed he found portions of shells be- longing to Cardium, Turritella, and Buccinum, and he ascribed this phenomenon to an irruption of the sea. In 1838, at the meeting of the British Association at Newcastle, he pointed ‘out the occurrence of marine shells covering the vestiges of terrestrial phenomena in Cefn Cave in Denbighshire, and again alluded to his former discovery, having also communicated the re- sults of both discoveries to the Geological Society of Dublin,—a body XXXVI PROCEEDINGS OF THE GEOLOGICAL SOCIETY. to which he was much attached, and by whom he was much respected. Perhaps no one ever laboured with more zeal and with more ability to discover all the phenomena connected with drift-deposits, or to reduce them to a diluvial origin; but, as time went on, he appears to have fallen into the more general views entertained on the subject, and, though he probably greatly modified his original opinions, many of his discoveries were of great use to other geologists, and have been noticed with respect by them, as, for example, by Mr. Conybeare, in his Report on Geology. In 1841, he published his work entitled ‘ Prac- tical Geology and Mineralogy,’ a work of very considerable merit, and especially remarkable for the sound and liberal views which he sets forth on that long-disputed subject, the description of creation in Genesis. ‘The assailants of revelation,” he observes, “ usually as- sume, and too many of its defenders argue on the assumption, that we have reason to expect a system of physical science in the sacred writings; but the slightest consideration of the purpose for which they were given must convince us that such a revelation would have been quite at variance with their professed object. That object was to make man acquainted with his relations to his Creator, with his original state, his present condition, his future hopes.” Would that those who still keep up the argument, whether friends or enemies of science, would adhere to this view of the object of Scripture, and neither embitter the minds of their opponents by acrimonious dis- putations, nor endanger the cause of true religion by injudicious assertions ! . Our late friend, for I must emphatically call him so, was fre- quently engaged of late in discussing the origin of the sand-pipes of the chalk ; and his papers are so recent that all must recollect how steadily he maintained their production by the wearing action of the sea, in opposition to that by the eroding action of water charged with carbonic acid. In this, as in most other geological phenomena, every form of sand-pipe cannot perhaps be explained by any one cause; and it would therefore be unwise to reject in toto any reasonable cause, - correct in principle, because incapable of explaiming every effect. The wisest plan is to adopt a give-and-take principle, and to ascribe each separate effect to its own natural and efficient cause. The very useful manner in which Mr. Trimmer had latterly applied his extensive knowledge of drift-formations to practical draining, obtained for him the patronage of Lord Berners of Keythorpe as a large and scientific agriculturist, and must cause him to be deeply regretted by that important and valuable class of society, the prac- tical farmers: it had, indeed, been his principal object through life to make science an instrument in promoting the welfare of mankind ; and his own predilection for the theory of currents, whether passing over the surface of dry land, or at the bottom of a sea, producing a furrowed surface, led him to resort to such furrows as a natural system of drains. We shall long remember him as an enthusiastic yet unprejudiced geologist, and as a simple-minded, frank, and honourable man, the worthy descendant of the friend of some of our childish days, Mrs, Trimmer, ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXVI As a man of very high intellectual acquirements, and as one who filled the office of Secretary of our Society in 1837, Dr. Rory de- serves to be long remembered with respect and affection by us all. It has always been the pride of our Society to know that its officers were distinguished for their high position amongst men of science ; and it is not necessary now to enforce the great truth that mental superiority in any one branch of natural science cannot fail to exer- cise a beneficial influence on the cultivators of every other great collateral branch. But though Dr. Royle has fully merited our warmest encomiums for his botanical researches alone, he deserves them also for the aid he has given towards the advancement of a knowledge of the geology of India, although he does not appear to have professed himself exclusively a geologist. As a proof of this I may cite a memoir on the geological features of the Himalaya Mountains, which forms part of his great work “Illustrations,” to be hereafter mentioned. This memoir was accompanied by some ex- tensive sections,—namely, one across the Himalaya Mountains; one from Saharunpore to the Source of the Jumna; one through the Great Coal-field of Bengal; and the last through the Central Range of India; so that this essay was a most valuable attempt to reduce to order, under the correcting influence of his own personal obser- vation, the many scattered observations which had been previously made, on the structure of the Himalaya Mountains and Bengal Coal-field, but which, like the Report of Captain Herbert, having been buried in the official archives of Bengal, had been almost for- gotten. As might have been expected, Dr. Royle did not neglect Fossil Botany, and he figured in the “Illustrations” the two new genera from the Coal-field of Bengal, Vertebraria and Trizygia, the former of which is still very obscure in respect to its affinities. Connected also with his brief memoir of the Sewalik Hills, he figured some of the most interesting of their mammalian remains; and being Secretary of our Society whilst the well-known investigations into the curious fauna of that district were in progress, which have since redounded so much to the honour of Dr. Falconer and Sir Proby Cautley, he was most enthu- siastic in his efforts to encourage his friends in their labour by rapidly bringing the results under the notice of men of science throughout Europe, thus performing an office which Dr. Falconer has himself so lately imitated in respect to Mr. Beckles and the Purbeck Fossils. Dr. Royle also published figures of some of the fossil mammalia from the elevated plateau of Thibet, behind the Snowy Mountains,— a matter so important in respect to the determination of the geo- logical age of the Himalaya Chain, that it deserves the attention of every one who shall hereafter endeavour to perfect the geological examination of this magnificent and interesting region. I am sure the Society will appreciate my feelings when I say that I have freely availed myself of the materials afforded me by Dr. Falconer (who succeeded Dr. Royle in the charge of the Botanic Garden, and was his most attached friend), not only in placing before you his geological claims, but also the following general sketch of VOL, XIV, d XXXVI PROCEEDINGS OF THE GEOLOGICAL SOCIETY. his truly valuable life; for who can be considered a better judge upon such subjects? John Forbes Royle, M.D., F.R.S. & L.8., Officer of the Legion of Honour, and a Vice-President of the Royal Society, was the son of an officer in the Royal army, who had served in India. He was born in that country and educated for the medical profession in Kdinburgh, where he obtained the diploma of Surgeon. He received soon afterwards an appointment as Assistant Surgeon in the E.I1.C. Service, and in 1819 proceeded to Calcutta on the Medical Staff of the Bengal Army, being first attached to the Artillery at Dum-Dum. | For two or three years afterwards he was moved from station to station in Bengal and the North-Western Provinces, and whilst dis- charging the medical duties, which the exigencies of the service demanded from him, he availed himself of every opportunity afforded by frequert change of locality to acquire a oe of the natural productions of the country ; among which, Indian plants engrossed the first place in his attention, and drew him into correspondence with Dr, Wallich, the eminent Danish botanist, at that time Superin- tendent of the Honourable Company’s Botanical Gardens at Calcutta. A vacancy having occurred in the charge of the Botanical Gardens at Saharunpore, Dr. Royle was, fortunately for science, selected by Government as the best-qualified candidate, and appointed Superin= tendent in 1823. No station in India is more happily situated than Saharunpore for the cultivation of the natural sciences. HKastward of Delhi, elevated 1000 feet above the level of the sea, near the ex- treme northern limit of that part of the great plain of India which is included in the valley of the Ganges, within a few miles of the Sewalik Hills, and within easy range of the great chain of the Hima- layas, the position commands alike the tropical flora and fauna of the plains of India, and the temperate climate of the Snowy range, and every variety between the two. Dr. Royle possessed the acquire- ments proceeding from education and self-culture,—the energy of character and the ardent love of science, which at once impelled and enabled him to avail himself to the utmost of these advantages. The Public Garden, supported by a native endowment, and laid out, after the simple native plan, with abundance of fruit-trees and common flowering plants, was entirely remodelled by the new Super- intendent, after the most approved plan of English landscape-gar- dening; a large addition was made to the number of species grown, whether indigenous or exotic; a scientific arrangement was adopted. A conservatory was erected, an ample stream of running water was introduced, which fell into an artificial lake; in short, by many refined alterations a tame oriental garden was speedily converted into a beautifully planned and useful scientific establishment, the whole having been the creation of Dr. Royle. To compensate as much as possible for the restriction imposed upon his time by the medical duties he was obliged to perform, he despatched par- ties of plant-collectors in successive years to the various mountain- provinces in the neighbourhood, across the Snowy Range over the Thibetian boundary, and as far westward as the valley of Cash- ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXIX meer. By these means he amassed a rich and valuable herba- rium; but his natural bent was most strongly exhibited in the in- vestigation of the properties of plants and their application to the wants of men; and for a considerable time he supplied the hospitals of Bengal with indigenous drugs, as substitutes for the expensive articles imported from Europe. He devoted himself with great success to the identification of the articles in the bazaars of the Kast with the medicines familiar to the Greeks, as described by Dioseorides and Theophrastus. He investigated the agricultural resources of the plains of India, with a view to the improved cul- ture and introduction of various grains and of plants yielding fibres and other useful products; and he endeavoured to direct attention to the capabilities of the valleys and slopes of the Himalaya for the erowth of tea, which has since been so successfully carried out. Dr. Royle’s principal work, “‘ The Illustrations of the Botany of the ‘Himalaya Mountains,” is a storehouse of valuable facts and infor- mation, bearing on these and other allied subjects. The favourable situation of Saharunpore provided other tempting fields of natural investigation, which his ardent zeal would not per- mit him to neglect. Single-handed he undertook the, for a tropical climate, severe task of taking hourly observations of the thermometer and hygrometer, and of the barometer on a single day in each month throughout the year, besides the regular ordinary observations twice a day; and by these means obtained excellent data for determining the meteorological conditions of the climate, and fixing one of the standard stations by which the range of mean temperature over the continent of India has been ascertained. He made collections of the mammalia, birds, reptiles, and insects of the northern plains and mountains of India, in themselves so valuable and extensive, that they furnished materials for two important and distinct memoirs by ‘eminent British naturalists, upon the fauna of India, contained in “The Illustrations.” During the various journeys through the Himalaya mountains, he carefully collected specimens of all the rocks he met with, marked the direction, and measured the inclina- tion of the strata,—ascertained the elevation of the successive ridges, and the depressions of the intervening valleys, by barometrical mea- surement, and recorded the whole of the observations with such care, that, gleaning materials from other sources, and aided by Sir ‘Henry Delabeche, he was enabled to produce a very respectable approximative geological section across the chain of the Himalayas, from the plains of Hindostan to the Snowy Range, which was ‘brought out in his ‘ Illustrations.’ All these varied and extensive ‘researches were condensed within the comparatively short period of eight years. Gifted by nature with a strong frame, and a healthy constitution that never failed him, and which sickness never touched, he toiled from first to last as an earnest and ardent investigator of coat natural object which came before him. _ India has not always escaped that political reaction which hurries ‘men in authority from reckless expenditure into sordid parsimony. -It.was thus that the first Burmese and other wars had thrown the xl PROCEEDINGS OF THE GEOLOGICAL SOCIETY. finances of India into such embarrassment, that Lord William Ben- tinck was called upon to push retrenchment to the utmost possible limit. So urgent indeed was the demand upon him, that it is said he meditated the abolition of the Botanic Garden of Saharunpore ; but such was the display of honest sterling work performed, and of most useful results obtaimed, which Dr. Royle placed before the eyes of the Governor-General, that Lord William Bentinck was spared the reproach of committing what would have been considered an act of Vandalism, and this most valuable institution was preserved,— a service for which his memory will always be regarded with grati- tude by Indian naturalists. Whilst this peril seemed to hang over one of the most cherished objects of his scientific hfe, Dr. Royle meditated a retirement from the service, as he could not have borne to remain in India after science had been so degraded; but as his energy, and, let it be added, the speaking testimony of his scientific labours, had averted the dan- ger, he bore with resignation those reductions of pay and emolu- ments which affected him in common with other medical men, and remained in India till 1832, when he returned to Europe with a large and valuable natural-history collection. From that time to 1840 he devoted himself with characteristic energy to the investiga- tion of the materials he had collected, and to the preparation for publication of his great work, the ‘ Illustrations of the Botany and other branches of the Natural History of the Himalaya Mountains ;’ a work which is distinguished equally by the large amount of original information it contains, and by the accurate research and comprehen- sive views it exhibits. On his return he became a member of all the great chartered scientific societies of London, and was named a Vice-President of the Royal Society, and latterly for several years he was Secretary of the Horticultural Society, for the welfare of which institution he felt a lively interest. The well-known ability with which he had investigated the medical botany of India, led to his appointment to the chair of Materia Medica and Therapeutics at King’s College on its first foundation ; and, as a member of the Royal Asiatic Sodiety, he, with his habitual energy, soon introduced to the notice of that learned body a new branch of inquiry, in consequence of which a committee was formed to investigate the productive re- sources of India. The ‘ Transactions’ of the Society, which had been before devoted chiefly to essays onthe Languages, History, Mytho- logy, Archeology, and Numismatics of the East, were thus enriched by a series of valuable papers on interesting commercial subjects by Dr. Royle. The interest which was now awakened in the manufac- turing districts respecting the raw products of India led to so many in- quiries for information, that the Directors of the East India Company” were induced to establish a special department for the express purpose of spreading knowledge upon such subjects ; and Dr. Royle, who had previously resigned his post as surgeon without any pension or other reward, having most wisely been placed at its head, he entered at once upon an enlarged sphere of public usefulness, suited to his great .talents and vast stock of acquired information, He was instrumental ANNIVERSARY ADDRESS OF THE PRESIDENT. xli in leading to the formation of a museum at the India House, for the reception of the most important portion of the immense collections of Indian products, both raw and manufactured, which had been im- ported for exhibition at the great Expositions, of London in 1851, and Paris in 1855, by which the benefit and instruction to be derived from their examination will be perpetuated. To perfect this noble design Dr. Royle devoted his utmost energies, and the very day before his death, though still labouring under sickness, he attended at the Museum to urge on the work; but, alas! it was his last effort, and, suddenly cut off on the next day, the 2nd of January, 1858, in the 59th year of his age, the East India Company lost one who, whether at home or abroad, had done more than most of its servants to pro- mote its true interests, by rendering them essentially coincident with those of mankind. Besides the works so often alluded to, Dr. Royle published many other essays, either separately or in the Journals of learned societies, principally botanical and bearing on the medical and commercial products of plants; and it may well be said that he was eminently a scientific philanthropist. Besides his general connection with so many of the most important Scientific Societies of London, he was a Member of several Foreign Natural History Societies, amongst which may be named the Academia Cesarea Nature Curiosorum ; and for his exertions in rendering the Indian Collection at the Paris Exhibition in 1855 as perfect as possible, he was honoured by a first-class Jury Medal, and by the insignia of an officer of the Legion of Honour. In reflecting on the last years of so distinguished a man, it must be a great comfort to know that he was most happy in having mar- ried a lady of highly cultivated mind, who, in the bitterness of her sorrow at the loss of her husband, has the consolation of feeling that she was the source of his greatest happiness, and a participator in his intellectual labours. He has left, besides his widow, two sons and a daughter to mourn his loss and venerate his memory; and let me add, that their feelings will be shared by the numerous friends to whom he was endeared by kindred feelings and by moral worth. Of several of our lost members little information of any material importance can be obtained, though they have all exhibited at some period of their lives a strong desire to advance the progress of science. Mr. Lavrrack for example, while an undergraduate at Cambridge, placed himself within the circle of attraction of Professor Sedgwick’s Lectures, and manifested a taste for geology by his close attendance at the Woodwardian Museum, then being put into order; but it is not known that he had any opportunity in after life of undertaking original investigation. Mr. G. H. Saunpers likewise exhibited an early taste for geology, and is known to the Society as having contributed a Sketch Map intended to illustrate the position of a bed of fossil shells exposed to ‘View in a cutting of the Panama Railway; the specimens he had xl PROCEEDINGS OF THE GEOLOGICAL SOCIETY, forwarded to the Society, and they were found by Mr. Moore to pos- sess much interest in regard to the distribution of tertiary fossils over the Central American area, Mr. Froresr was a native of Sardinia, and ranked in his own — country amongst the nobility, beg Marquis d’Arcaes; but, as an Italian refugee, he only made use of his family name. For some time he was manager of a portion of the Mexican mines, which were worked under the direction of Mr. John Taylor; and he was on his way to Central America to report on mines in the Province of Gua- temala, when he was attacked with fever at Panama, and died, to the great regret of his employers, by whom he was considered a most amiable and upright man. His son has since taken charge of some Mexican mines which belong to a different body of proprietors. Mr. Wittram Batp was an eminent Civil Engineer and Surveyor, He was born in Burnt Island, Fifeshire, and was educated at the parish school there until he arrived at his twelfth year, when he was removed to a school at Edinburgh. After completing his ordinary education, he was apprenticed e Mr, Ainslie, C.E., of Edinburgh. He commenced his professional career in this ‘Tine in 1803, and he had much experience in making railways, and in the improvement of rivers and harbours. His abilities, being fully recognized, led to his employment in Ireland, where he was directing engineer in im- proving the navigation of the River Boyne and in forming quays at Drogheda; and was engaged to carry bills through Parliament for the improvement of the navigation of the River Suir, and of the River Moy, both in that country. It was during the time of his resi- dence in Ireland, that he was employed in 1811, by a Royal Commis- sion appointed to ascertain the situation and extent of the great bogs of Ireland and the practicability of draining and improving them, and to survey and report on the extensive bogs ‘of the county of Mayo, His reports on their situation, extent, and improvement formed part of those valuable public documents, ‘The Bog Reports,’ which were presented to Parliament, and printed in the years 1811, 1812, 1813. The very interesting information which these Reports contain on the peculiar condition, circumstances, and origin of the large accu- mulations of bog, which are so remarkable in Ireland as to constitute what may be almost considered a distinct geological formation, has caused them to be consulted by every one desirous of studying the history of bogs; and when the curious phenomena connected with them, such as the occurrence of two or three layers of tree-stumps, the ‘‘escars” or long ridges of gravel, the beds of marl, and the numerous relics of the great fossil Deer, the Megaceros Hibernicus, are considered, it cannot be doubted that the authors of these Reports have laid before naturalists, and especially geologists, ample materials for re- flection. This was not the only great Irish work in which Mr. Bald was engaged, as he was employed about the year 1810, by the grand jury of the county of Mayo, to make a territorial survey of that county, which he afterwards completed in a most accurate and satis- ANNIVERSARY ADDRESS OF THE PRESIDENT. xiii factory manner. This map was laid down and drawn on a seale of 4 inches to a mile; and I remember well my visit to the Court-house of Castlebar, some thirty years ago, to look at the map, which was then, as now, suspended in a large room, and justly considered a topographical work of the very highest order. That the triumph it then achieved was well-merited, may be judged from the honour- able testimony which that able judge, Sir Richard Griffith, Bart., known to us all as one of our oldest and most able members, has recently borne to its excellence in the following words addressed to me on the subject :—‘‘ Though slightly faded, the mountain-ranges, hills, and other, even very minor, features of the country have been so carefully and faithfully represented by drawing and shading, as to © present one of the most striking and effective maps I have ever seen on so large a scale, and in pictorial effect little inferior to the mag- nificent map of the mountains of North Wales, long since executed by Mr. Dawson, father to the present Colonel Dawson, R,H,” This warm and frank expression of approbation, bestowed by a Civil Engineer of such eminence as Sir Richard Griffith, himself the author of the highly-yalued Geological Map of Ireland which will long be an object of emulation to the Government Geological surveyors, to his former associate and acquaintance, seems peculiarly appropriate, as it is not too much to say that the map of Mr, Bald was in its time a fitting object of emulation to the Government National Surveyors, whether Engineer Officers and men, or Artillery Officers for some time associated with them, or Civilians who formed so large a por- tion of their hard-working staff, although it is much to be feared they shared more in the labours than in the honours and advantages of their military comrades. Independently of the merits of his map of Mayo, Mr, Bald deserves to be remembered with respect by the Officers of the Ordnance, or, as it should now be called, the National Survey, for the manly and frank manner in which he gave his evidence in their favour, when the propriety of confiding the charge of the Irish Survey to the Ordnance was under discussion before a Committee of the House of Commons. The opinions of Civil Engineers and Surveyors were much divided; but Mr. Bald allowed no private interests to blind him te the advantage of a uniform system, carried on with the regu- larity and precision which military discipline enforces and ensures: but, while I say this in justice to the liberality of Mr. Bald, let it not be supposed that I am the advocate of monopoly or exclusion in any department of the public service. When Mr. Bald left Ireland, he was employed for a time as a draftsman at the Admiralty, and then, by the Corporation of Glasgow, as Engineer for the improvement of the navigation of the Clyde by the erection of embanking-walls to circumscribe its channel, and by dredging to deepen it—reports of which operations were drawn up by him and printed. He was in this manner the recognized Resident Engineer to the Trustees of the River Clyde from 1839 to 1845, in the summer of which year he was engaged by the Chamber of Com- merce to examine the River Seine in France, from Havre-de-Grace xliv PROCEEDINGS OF THE GEOLOGICAL SOCIETY. to Rouen, I have been unable to learn anything of the last years of Mr. Bald’s life, and I must therefore here close my remarks upon a man, whose talents, which reflected so much credit upon his profession, were employed on objects both useful and interesting to geologists. The very eminent Mineralogist and Crystallographer, Hznry JAMES Brooxe, was born at Exeter on the 25th May, 1771, his relatives being engaged in the manufacture of broad-cloth; and after having received an ordinary scholastic education, he studied for the Bar, but was induced from the favourable prospects which appeared before him, to abandon that profession and to engage in the Spanish wool-trade in London, for which object he spent nearly two years in Spain: it is, however, justly asserted that the active study of the law had, like that of mathematics, the effect of framing his mind to precise habits of thought and expression, the effects of which became apparent in all his subsequent acts and observations. In the year 1812, soon after he had become a resident of London, he turned his attention to the subjects of Mineralogy, Geology, and Botany, but more especially to the two former sciences, for which he had a peculiar predilection. He was elected a Fellow of the Geological Society in 1815, of the Linnean in 1818, and of the Royal in 1819, on the Council of which Society he served in 1842-44. Though devoting his leisure hours to scientific pursuits, Mr. Brooke did not neglect his ordinary duties, and assisted the late Mr. Henry Hase, Cashier of the Bank of En- gland, in establishing the London Life Assurance Association; and, as the Spanish wool--trade began to decline, Mr. Brooke sought a pur- suit more congenial to his taste in the establishment of companies to work tne mines of South America; but, as these undertakings were too often marred in their prospects of success by difficulties abroad, he accepted the office of Secretary of the London Life Asso- ciation, in forming which he had assisted; and after several years’ service, such was the appreciation of the advantages he had con- ferred on that body, that on his retirement a liberal annuity was granted to him by the society. Though interrupted for some time in the pursuit of his favourite sciences, by the consequences of a serious accident he experienced by being knocked down by a horse suddenly turning a corner near his residence, Mr. Brooke was not a man to be satisfied with idleness, and for recreation’s sake he formed a large collection of shells, which he afterwards presented to the University of Cambridge. Not think- ing the study of the simple envelopes of organic bodies sufficiently intellectual, he then took to the collection of engravings, haying himself early in life made considerable progress as an amateur artist ; and some specimens of rare excellence were presented by him to the national collection in the British Museum. This interruption of his scientific labours was only of short duration, and being usually blessed with excellent health, he continued to pursue his favourite studies with unabated activity until a short time before his death on the 26th June, 1857, at the good old age of 86 years, ANNIVERSARY ADDRESS OF THE PRESIDENT. xlv Of his works, the ‘ Familiar Introduction to Crystallography’ was the first systematic treatise which in this country brought that de- lightful branch of science into notice: it was based on the system of Haiiy, and adopted therefore an unnecessarily large number of pri- mary forms: but at the same time the relations of the various ex- isting plane surfaces of crystals were traced out with a clearness which was a great improvement on preceding systems. In the subsequent Treatise on Crystallography, published in the ‘ Ency- clopeedia Metropolitana,’ Mr. Brooke simplified the former one, and reduced the number of primary forms to six, which correspond with the six systems adopted by Continental Crystallographers. Mr. Brooke discovered and described thirteen new mineral species. Mr. Brooke applied the reflective goniometer to the determination of the crystalline forms of artificial salts, and in the ‘ Annals of Phi- losophy’ for 1823 described no less than fifty-five laboratory-crystals thus determined. He was the author of the article ‘“ Mineralogy” in the ‘ Encyclopedia Metropolitana,’ and was associated with Professor _ W. H. Miller in the reproduction of the well-known treatise of the late Mr. Phillips. His last work was on the general relations and geometrical similarity of all crystals belonging to the same system ; it formed the subject of a paper read before the Royal Society, and was in the press at the time of his decease. With a liberality equally characteristic both of Mr. Brooke the elder and the younger, the valuable and almost unique collection made by the father during half a century, has been presented by the son to the University -of Cambridge,—a generosity which has wisely adopted the most efficient method of perpetuating the memory of a man who had so successfully endeavoured to simplify the study of that branch of Mi- neralogy which of all others is most full of interest; for assuredly crystallization seems to afford a sort of link between organic and in- organic nature, by showing that not only in composition, but also in external form, lifeless and inert matter has been subjected to definite laws by creative Intelligence and Power. Francis, Kart or Exiesmerr, a Knight of the Garter, Lord- Lieutenant of Lancashire, and during the year 1854-5 President of our sister Society, the Geographical, was one of those eminent individuals who in our day have shed lustre over the high order of nobility to which they belong, by their literary and scientific acquire- ments, just as their ancestors, in olden time, did by martial qualities. It is indeed a characteristic of the present age, which is principally due to the establishment of societies devoted to special branches of scientific inquiry, that men of the highest social position do not dis- dain to emulate men of a lower grade in the endeavour to obtain the first places in the ranks of science. Lord Ellesmere was the second son of the first Duke of Sutherland, and of that gifted lady the Duchess Countess*of Sutheriand. He was born in 1800, and died on the 18th February, 1857, being therefore cut short in his distin- guished career at the comparatively early age of 57. As a geogra- pher of a high order, Lord Ellesmere has received an affectionate and xlvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY; eloquent tribute from the pen of our own Sir Roderick Murchison, the President of the Geographical Society, in his Annual Address to that most useful and prosperous Society ; and I can do no better than glean from him what is necessary to justify the high estimation in which we, have always held that estimable Nobleman. For a large portion of his writings, Lord Ellesmere adopted the Quarterly Review as the medium of communication to the public, It appears that between the years 1834 and 1854, he was the contri- butor of no less than fifteen articles, many of which were directed to geographical research, others to the fine arts of which he was an able connoisseur, and some to biography, or to military exploits, as the spirit of chivalry was as alive in him as in the breasts of his warlike ancestry, His accounts of the works of the Dutch authors Meiglan, Fischer, and Doeff, and especially his vivid picture of the manners and usages of the Japanese, have been justly praised as having thrown a charm over geographical science, and rendered even its minute details attractive. The lively interest he displayed in the romantic expedition of Sir James Brooke, his analysis of Arctic and Antarctic researches, and his account of the travels of Castron among the Lapps not only prove the pleasure he derived from perusing the narratives of voyagers and travellers, but also his ability in estimating the value of their results. Many must remember the stately figure, and the courtly yet courteous manners, of this type of the true Eng- lish nobleman, when, opening the halls of the palace of his family for the reception of the leading men of science, he collected, as it were, the living gems of intellect within a frame-work enriched by those of past ages as displayed in his rich collection of the works of the eveat masters of art; as well as the dignified manner in which he presided over the Geographical Society: he exhibited indeed every quality which is calculated to adorn a nobleman of such high social position, and to render him a fitting leader of his fellow men. The versatility of his talents has been already noticed; but it may be added that he possessed the soul of a poet; for who but a-poet could attempt to transfuse the spirit of a Goethe and Schiller into the English language ?—-and unquestionably the soul of a soldier, as, in addition to the papers in the Quarterly Review, he translated ‘ Clau- sewitz’s Campaigns in Russia,’ the ‘ Sieges of Vienna by the Turks,’ and the ‘ Last Military Events in Italy.’ This latter aspect of his character was strikingly marked by the strong attachment and respect he always manifested for the great Duke of Wellington; and his singular ability for military science may be judged from the sound judgment he has exhibited in his Preface, or, as it may be called, Introduction to Clausewitz’s ‘‘ Campaign of 1812,” His thorough knowledge of the fine arts is well known; and his goneral acquaintance with science, as well as his earnest desire to apply it to the practical amelioration of the condition of his fellow ereatures, was publicly manifested by his address to the British Association, over which body, at its meeting in 1842, at Manchester, he presided as President, being then Lord Francis Egerton. His generous support of men of genius, and his domestic virtues, flowed ANNIVERSARY ADDRESS OF THE PRESIDENT. xiv from the highest qualities of the human heart; and I need do no more than quote the expressive words of one of his intimate friends, as given by Sir Roderick Murchison :—‘ His calm exterior and tran~ quil manner covered a deep-seated enthusiasm for the honour of his country, for the progress and amelioration of his species, and for all that is grand and noble in sentiment or in action,” Rear-Apmrrat Sie Francis Beavrort, K.C,B., D.C.L., F.R.S., F.R.G.S., Corr. Inst. France, was one of those remarkable men who in these days have afforded to the world a most powerful illustration of the fact, that the highest cultivation of the intellect is quite com- patible with the nautical knowledge and habits which enter into the composition of a first-rate seaman and an able navigator. If indeed the example of Lord Ellesmere has shown how much the highest order of nobility may be adorned and elevated by scientific and literary tasies, we may also affirm that much of the dignity which has been associated with the names of Beaufort and of Graves, and with those of Admiral Smyth and Captain Spratt, fortunately still living, and of many other illustrious seamen and navigators, is due to the happy combination in their characters of high scientific attainments and of great practical skill. Francis Beaufort was born in 1774, and was an Irishman of French extraction. His father, the Rev. Daniel Augustus Beaufort, was Vicar of Collon, in the county of Louth, and was directly descended from an ancient and noble French family. Francis was the second son, and the heir of some of the talents and tastes of his father, who numbered amongst his good deeds the best map of Ireland, previous to the Ordnance Survey, and an able Memoir on Ireland; but it may be added that those who have read the able essay upon the Round Towers of Ireland by one Miss Beaufort, and the kind-hearted and cheerful books written for the benefit of chil- dren by the Misses Beaufort, who are so well known and so highly appreciated in Dublin, must further acknowledge that the tastes and virtues of a whole family were embodied in the Admiral, Though only thirteen when he went to sea, Francis had already many of the requisites of an able officer. On his first voyage, which was with Captain Lestock Wilson, in the ‘ Vansittart,’ East India- man, as a “ guinea-pig’’—that is, in virtue of the payment of a hundred guineas,—he was remarkable for his skill in observation, and the amount of his nautical knowledge ; ; so that he afforded valuable assistance to his commander in surveying the Strait of Gaspar, in the Sea of Java. His perilous adventures began thus early. The survey was just completed when the ‘ Vansittart’ struck upon a rock off the Island of Banca (not very far from the spot where the ‘Transit’ went down last autumn), and through the hole stove in her bottom daylight and sea poured in alternately. An effort was - made to keep the ship afloat until the flat shore of Sumatra could be reached; but even the hope of a landing on Banca was presently given up, and she was run aground on an island seven miles from Banca. The crew escaped in the boats, and, with the loss of six xvii PROCEEDINGS OF THE GEOLOGICAL SOCIETY. lives and one boat, reached two English ships after five days’ rowing, with great suffering, on the open sea, close to the line. This ad- venture happened in August 1789. His name had already been for two years on the books of His Majesty’s. ship ‘Colossus’; but on his return from the East he joined the ‘ Latona,’ Captain Albemarle Bertie, and afterwards the ‘Aquilon,’ in which he was engaged in the memorable action off Brest, of the Ist of June 1794, during which ten of the enemy’s ships were dismasted and seven taken, and after which Lord Howe brought into Portsmouth six French ships of the line, which the King and Royal family came to inspect at the end of the month. They went on board the ‘ Aquilon’ to sail round the fleet, and thus young Beau- fort made, probably, his first acquaintance with royalty. He was for some years the sole surviving officer of that great battle. He fol- lowed his captain, the Hon. Robert Stopford, to the ‘ Phaeton,’ in which ship he was serving when Vice-Admiral Cornwallis made his eclebrated retreat from the French fleet on the 17th of June 1795, In this ship, afterwards commanded by Captain James Nicholl Morris, he assisted at the capture and destruction of many of the enemy’s ships, and of nine privateers and other vessels. It was in May 1796 that he obtained his rank of Lieutenant, and in October 1800 that his first great opportunity of distinguishing himself occurred. While cruising off the coast of Malaga his commander observed that a Spanish polacca, the ‘San Josef,’ and a French privateer brig, had taken refuge under the fortress of Fuengirola; and at night the young lieutenant was sent in command of the ‘ Phaeton’s’ boats to board the ‘San Josef.’ The French brig intercepted the launch ; but the other crews did their work without its aid. The resistance they encountered was desperate; but they obtained their prize, with the loss of one man to thirteen of the enemy, Beaufort, however, receiving no less than nineteen wounds. This made him a commander, with a small pension. The two next years were spent on shore, but not in idleness. Miss Edgeworth tells us that they were “ devoted, with unremitting zealous exertion,” to establishing a line of telegraphs from Dublin to Galway, an object of great importance as long as the west of Ireland was perpetually liable to invasion from continental enemies. He received the thanks of Government for his efforts, declining any other acknowledgment. Once more at sea, he was heard of from the East first, and then the West. As commander of the ‘ Woolwich,’ 44, he convoyed from India sixteen Indiamen in 1806. In 1807 he was surveying the River La Plata; and he afterwards went to the Cape and the Medi- terranean. In 1809 he was hovering about the enemy’s merchant- men on the coast of Spain and at Quebec, being in command of the sloop-of-war ‘Blossom.’ In 1810 he obtained his post rank, and the command of the ‘ Fredericksteen’ frigate; but before he joined he was employed in protecting the outward-bound trade to Portugal, Cadiz, and Gibraltar, in accompanying two Spanish line-of-battle ships to Minorca, and in acting for some months as captain to the ANNIVERSARY ADDRESS OF THE PRESIDENT. xlix ‘Ville de Paris,’ a first-rate, in the fleet off Toulon, commanded by Sir Edward Pellew. It does not appear to be on record in which year of his life it was that he so nearly perished by drowning, and underwent the remark- able experience of the intellectual condition under such a crisis, which he afterwards recorded in a letter, at the request of Dr. Wollaston. He described himself as “a youngster, at Portsmouth, in one of the King’s ships.” He was not himself impressed as others were by the remarkable character of his sensations; but he saw the importance of every such record, and made it accordingly. Interesting in itself, the story is extremely valuable as coming from one as singularly truthful in recording experience as skilled in detailing it. One of his most striking accomplishments was the power of expressing what he meant. The effect of this power was seen wherever he went, in the harmony he seemed to establish by the clearness of his ideas, and the graphic manner in which he expressed them. All the disputings and perplexities which accompany the rule of men of confused mind and speech were extinguished by Beaufort’s mere presence; and he at once made every one aware of their own, as well as of his views and objects, This power of rendering the most abstruse subject easy of com- prehension, a power possessed by very few, was strikingly exemplified in the letter to Wollaston, published in Sir John Barrow’s Autobio- graphy, which describes that peculiar psychological condition of the human frame at times when it hovers, as it were, between life and death, or is on the point of yielding up the united existence of body and soul, and assuming that alone of the soul. Few have doubtless experienced this condition under the same circumstances as Admiral Beaufort, by being snatched from drowning at the very moment when the soul was about to assume its undisputed empire; but many have passed through a corresponding state at times when, fever having reduced the powers of the body to a menemum, and elevated those of the soul to an unnatural and unbalanced sway, sleep is dispelled from the weary eyelids of the body, and the phantoms of past words, thoughts, and acts come rushing unbidden, and too often unwelcome, upon the mind’s eye. At such moments the past is reflected upon with pain or with pleasure, in proportion to its relation to evil or to good, and doubtless in reference to its bearing upon the future; and hence the natural reflection of Admiral Beaufort,— «May not all this be some indication of the almost infinite power of memory with which we may awaken in another world, and thus be compelled to contemplate our past lives? or might it not in some degree warrant the inference that death is only a change or modification of our existence, in which there is no real pause or interruption? But, however that may be, one circumstance was highly remarkable—that the innumerable ideas which flashed into my mind were all retrospective. Yet I had been religiously brought up, my hopes and fears of the next world had lost nothing of their early strength, and at any other period intense interest and awful anxiety would have been excited by the mere probability that I was floating | PROCEEDINGS OF THE GEOLOGICAL SOCIETY. on the threshold of eternity ; yet at that inexplicable moment, when’ I had a full conviction that I had already crossed.that threshold, not a single thought wandered into the future, I was wrapt entirely in the past.” In several passages of the deeply interesting statement of Admiral Beaufort will be observed an idea which was afterwards powerfully elaborated by Mr. Babbage in the Ninth Bridgewater Treatise. When he took the command of the ‘ Fredericksteen,’ in 1811, he was on the road to fame as an author. Sir. J. Barrow tells us that Beaufort was selected out of the whole Mediterranean fleet to survey an unknown portion of the coast of Syria. The result of this errand was, not only a capital survey, but a historical review of the country, as illustrated by its remains of antiquity. Beaufort’s ‘ Karamania’ was, as a book of travels, sound, substantial, and learned (thanks to the good classical education his father had given him), and full of interest at once for the man of science and the scholar. It was this book, with its discoveries and verifications of ancient sites, which had prepared the way for the researches of Fellows, Spratt, and Forbes, and more recently of Charles Newton, in Asia Minor, the result of which has been that the Halicarnassian Marbles have become part of the treasures of the British Museum. After much hazardous service against the pirates in the Greek waters, Captain Beaufort went to work on the survey of Syria, in the course of which he underwent extreme danger. In June 1812, his party were surrounded by armed Turks led by a crazy dervish, and he was wounded in the hip-joint so seriously that the wonder was that he ever walked again. It was a severe struggle for life itself; and when his ship was paid off, in the next October, he was still undergoing much pain from the exfoliation of the bone. He solaced his enforced leisure by work, preparing for the Admiralty such a set of charts of the coasts of Asia Minor, the Archipelago, the Black Sea, and Africa, as had never before been seen at the Admiralty. They were so drawn, finished, and arranged as to be fit for transference to the copper without any aid from the hydrographer or his assistants. Such is the testimony of Sir John Barrow, who recommended him to Lord Melville for the post of Hydrographer. | This was in 1829. In 1823 Captain Hurd had died, and Captain Parry was requested by Lord Melville to fill the post temporarily, which he did twice, if not three times. After the resignation of the Duke of Clarence as Lord High Admiral, Lord Melville again became First Lord, and one of his objects was to fill the office of Hydro- erapher with the best man that could be found, who should hold it permanently. There were many applicants ; but by 1829 two names only remained for choice—and one of them was not an applicant, Captain Peter Heywood. Lord Melville therefore requested Sir John Barrow and Mr. Croker to advise him. Sir John Barrow had, as we have seen, selected Beaufort out of the whole Mediterranean fleet for the survey in Asia Minor; and that survey having been so ably completed, he naturally named for the office of Hydrographer the accomplished officer who had so much. distinguished himself, ANNIVERSARY ADDRESS OF THE PRESIDENT. li For twenty-six years Beaufort was at the Admiralty as Hydro- erapher; and very early in that period he had made his office the model on which Copenhagen and St. Petersburg constructed theirs. Everywhere hydrography took a new form and existence, through the life which he put into his work. There is not a geographical discoverer, nor a zealous professional student in any naval service in the civilized world, who does not feel under direct obligation to Beau- fort for his scientifi¢ assistance given through his works, or more special encouragement by his personal aid and counsel: those, indced, who remember the enthusiasm with which Commander Wilkes, of the United States Exploring Expedition, used to speak of the friendly assistance afforded by Captain Beaufort, in preparing for that im- portant enterprise, cannot doubt of the appreciation in which he was held by his professional brethren of all nations. It has been no small benefit to the world that the most accom- plished hydrographer of his own or any time was at our Admiralty for six-and-twenty years, always ready to avail himself of any chance of increasing general knowledge, and ever genial and gencrous in assisting every man of any nation who devoted himself to geographi- cal discovery or the verification of glimpses already obtained. His name is attached to several stations in newly-discovered lands and seas; for instance, it will be uttered in all future times by voyagers passing up either the eastern or western shores of the American con- tinent to the Polar Sea; but even when not expressed, it is invisibly connected with almost every other modern enterprise of geographical discovery ; for he gave a helping hand to every scientific adventurer who applied to him, and no one thought of instituting scientific ad- venture without applying to him. When he entered the Admiralty, nearly thirty years ago, he found his own department a mere map-office. His friends well remember what a place it was—small, cheerless, out of the way, altogether unfit and inadequate. The fact is, nobody but the élite of the naval profession had any conception of the importance of the office—of the true functions of the hydrographer. Maritime surveying on an ex- tended scale was only beginning. We were not yet in possession of the full results of the labours of Flinders, Smyth, King, and Owen; and Sir Edward Parry’s view of his office was, that it made him the Director of a Chart Depot for the Admiralty, and the sup- porter, rather than the guide or originator, of maritime surveys. Becoming conscious that the times were requiring something more than he could give, he wisely resigned. The manner in which Cap- tain Beaufort was appointed, without solicitation on his own part, and simply because the best judges considered him the fittest man, encouraged him to lay large plans, and to indulge high hopes. He began a great series of works, in which he intended to comprise, gradually and systematically, all the maritime surveys of the world, = our own coasts, still shamefully obscure, being destined for a thorough exploration in the first place. He designed and began what Lieutenant Maury has since achieved, His instructions to surveying officers show how extensive were his purposes as to deep- li PROCEEDINGS OF THE GEOLOGICAL SOCIETY. sea soundings so long ago as 1831; and the object was never lost sight of, though he was baffled in the pursuit of it. Whatever de- pended on his own energy was done, throughout his whole term of office ; but he had to endure the affliction, often experienced by highly qualified servants of the Government, of not being able to excite a sympathy in his views amongst those in power, or amongst those who, keeping watch over the public purse, sometimes arrest the pro- eress of what would conduce to the public interest. It is indeed no small mortification to compare our Hydrographical Establishment with that at Paris, where the Dépot de la Marine might be taken for the office of the greatest maritime power in Europe; or with those at St. Petersburg, Copenhagen, and Washington; but the annual amount of shipwrecks, and the number of lives lost through want of that knowledge which Beaufort would have established a quarter of a century ago, gave rise to a severer grief, which weighed heavily on his heart, and was probably the most painful experience of his life. The universal spread of education, and the more scientific tone which it has assumed, will, it is hoped, rectify this evil, by satisfymg the Members of Government, as well as our Legislators, that expenditure on such objects can never be money thrown away; and we trust therefore that the able successor of Beaufort, Captain Washington, to whom I am indebted for most of the materials of this memoir, will be secured from the anxieties and mortifications which his predecessor experienced. Captain Beaufort was so restricted in his office that he had no subordinate who could be a comrade in his labours ; and all that he had at heart was done by his own hand. Disappointed in some of his hopes, and pinched in his official expenditure, he applied the full forces of his strong will to make the best of the hard circumstances of the case. His industry, of constitutional origin, and sustained by principle, appeared something miraculous under this stress. Day by - day for a quarter of a century he might be seen entering the Admi- ralty as the clock struck; and for eight hours he worked in a way which few men even understand: for many years he rose at five, and worked for three hours before his official day began. The anecdote of his connexion with the maps of the Society for the Diffusion of Useful Knowledge has recently gone the round of the newspapers ; and all the world knows that, in order to get these maps sold at sixpence instead of a shilling, he offered to superintend their pre- paration. Asif he had not enough to do in his own function, he gave the world that set of maps, so valuable that no ship in the United States navy is allowed to sail without them ; and it is his doing, that they are in a thousand houses which they would never have entered but for their cheapness. This is one of his innumerable charities. There was no sort of charity in which he was not just as liberal and as wise. There was no pedantry in his industry, any more than in his knowledge. He never seemed in a hurry. While too seriously engaged for gossip, he had minutes or hours to bestow where they could really do good; he had conscientious thought to spare for other people’s affairs, and — ANNIVERSARY ADDRESS OF THE PRESIDENT. lili modest sympathy in their interests, and intrepid advice when it was asked, and honest rebuke when it was deserved and might be effec- tual. His unobtrusiveness was perhaps the most striking quality of his manner, to observers who knew what was in him. His piety, reverent and heartfelt, was silent, as he preferred that that of others shouldbe. His domestic affections were unconcealable; but spoken sentiment was quite out of his way. His happy marriage (with the daughter of his first commander, Captain Lestock Wilson) ended in a mingling of pain and privilege which touched the hearts of all wit- nesses. Never was so much understood with so little said. She died of a lingering and most painful disease, making light of it to others as long as possible, though the full truth was known to both; she kept her young children about her, with their mirth wholly unchecked, to the latest possible day ; and the few who looked in on that sacred scene saw that it was indeed true that, as she said, she had never been happier than during that painful decline. As for him, there was not the slightest remission of public duty, while his domestic vigilance so powerfully assisted in smoothing her passage to the grave. Now that both are gone, it is right to present this feature in the character of the man so long before known as hero and as savant. He came out from the long trial so much changed that it seemed doubtful whether he would ever regain his health and buoyant cheer- fulness. He lived, however, to see his children fulfilling, each his own career of labour and honour: one son in the church, another as Legal Remembrancer (Attorney-General) in Calcutta, and a third as a judge in Bengal. By his second marriage, with a sister of Maria Edgeworth, he secured a friend to himself and his daughters for many of the latter years of his life. Among his public labours were those of the successive offices of Commissioner of Pilotage, entered upon in 1835, and of Member of the Royal Commission to examine into the state of the Tidal Har- bours in the United Kingdom, in 1845. In 1846 he became Rear- Admiral on the retired list rather than surrender his office; but he never liked his “ yellow flag,” and the mortification of his retirement was but slightly solaced by the honour of the Knighthood of the Bath, conferred in 1848. The sudden expansion of railway-projects so increased his work that his health began to fail, but not till he had reached an age at which few men think of work at all. arly in 1855 he was obliged to retire and go home to a sick bed to suffer with fortitude the pangs of a painful and incurable disease. He was the same man to the last,—active and clear in mind, benevolent and affectionate at heart, and benign in manners. His activity never interfered with his profound quietude and peace; and his quietude and peace deepened, as his mind brightened, to the last. He was short in stature; but none of those who were personally acquainted with him will forget his countenance, which could no- where pass without notice. Its astute intelligence, shining honesty, and genial kindliness revealed the man so truly that, though he never lauded himself, few were so correctly estimated, and so highly valued. He was attended in his last hours by his adoring nae and died VOL. XIV. liv PROCEEDINGS OF THE GEOLOGICAL SOCIETY. in the midst of them on the 17th of December, 1857. Whilst de~ ploring his loss, society should be thankful that such a man was spared so long for the benefit of mankind. Although most of the preceding record is but the echo of the tribute already paid to this great man, by one of his most distinguished friends, I have thought it due to the members of this Society to preserve it that they all may be able to dwell on the character and merits of one who has shed so much lustre on this and other scientific societies. May the officers both of army and navy be encouraged to imitate so bright an example, and not be. deterred from doing so by the senseless dread of becoming too learned ! Tomas Brst Jervis, Lieut.-Colonel E.I.C. Engineers, F.R.S., F. Geol. 8., F. Ast. 8., F.LS., F.A.S., F. Geog. 8., M.I.C. Eng., Cor, M.N.H.S. Boston, Soc. Ethnogr. Paris, &c. &c., was the second son of John Jervis, Esq., civil servant of the E.1.C., who, having for some time held a high post at Madras, was transferred to Jaffnapatam, on the north of the island of Ceylon, where Thomas Best Jervis was born, August 2, 1796. Lieut.-Col. Jervis throughout life valued himself less upon his ancestry, although his family is most ancient and respect- able, than on the fact that several of his relatives had been eminent for their patriotism, learning,and integrity. The head of the family, James Jervys, Esq., possessed the property of Chatkyll,in Staffordshire,in the fifteenth century ; and Colonel Jervis would recount with satisfaction the fact of King Charles having been protected and hidden after his retreat to the oak, by Miss Lane, one of the staunch royalist mem- bers of the family. In later times the celebrated divine, Bishop Hooker, and the Earl of St. Vincent (Sir J. Jervis), have nobly main- tained the honour of the family. On his mother’s side Colonel Jervis was descended from a Polish family of the name of Ritzo, who had been for generations in the royal household of the Georges, whom they accompanied from Hanover. Baron Grimm’s family still reside in Prussia, where the present Dr. Grimm is physician to the king of Prussia, and one of the principal medical officers of that country. George, Thomas, and John, the three sons of Mr. John Jervis, were sent home to England at a very tender age, in accordance with the necessity imposed by the tropical climate, for their education, and were consigned to the care of their uncle Chief-Justice Thomas Jervis, of the Chester circuit. Thomas was first transferred to a maiden aunt, Miss Jervis, at Lichfield, an excellent Christian person, from whose watchful care he acquired that deeply-rooted principle which was. always one of his most marked characteristics. The first school he went to was kept by a Dame ; and, being there taught along with little girls, he was thoroughly grounded in English grammar, and other sub= jects too often neglected or omitted at boys’ schools. Fron hence he probably derived an habitual gentleness of disposition, so that he had an uncommon tenderness of feeling, even towards the brute creation, never liking to inflict pain even on aninsect. From Lichfield he was _ placed at a school at Rugely (Staffordshire),and subsequently sent up to town to Judge Jervis, whose wife, having children of her own, always ANNIVERSARY ADDRESS OF THE PRESIDENT. lv treated the three “‘ India boys” with comparatively little ceremony. Thomas was sent to Mr. Delafosse’s excellent classical school at Rich- mond, and, having to trust entirely to his own exertions for getting en in life, early showed an eager thirst for knowledge ; so that, instead of wasting his youth in play, he studied with the greatest attention, and was soon one of the most proficient in the school for his clas- sical knowledge, taking great delight in Greek and Latin poetry. He now became very desirous of acquiring a knowledge of other subjects then so much neglected at classical schools, as is still too frequently the case in great seminaries: he procured some books on elementary mathematics, and studied them diligently, making himself by his zeal a favourite with the principal. During the holidays, which he spent with his uncle, he still pursued his studies by himself, and spent his allowance of pocket-money in procuring little French books, a pencil, or something similar, exhibiting an energy in the pursuit of knowledge uncommon in a lad of his age, though shared in a measure by his two elder brothers. He now persuaded his cousins to teach him a little French and drawing, and he always remembered with gratitude the simple lessons of one of them who thus assisted him. Hence he was sent to Addiscombe College to study for the Kast India Company’s service, in which for several generations his family and relatives had passed the best years of their life. He had here a better opportunity of studying the languages, French, Hindustani, &c., and under the able professors of that establishment he mastered the elements of mathematics, becoming, as he advanced in knowledge, enraptured with the subject, which he followed up to the day of his death with unwearied delight. After having remained the requisite time, he passed a most honourable examination for the Engineers, being one of the foremost of the cadets of the year (and there was no lack of talent among the candidates for the Engineer service) ; and he was sent to Worcestershire, under Colonel Mudge, R.A., to work on the Ordnance Survey of England: the part he surveyed was the town and neighbourhood of Bromsgrove, since engraved on the 1-inch scale. . He now embarked in the fleet which was despatched to convoy the merchantmen sailing for Bombay, and he arrived at that port in May 1814. Immediately after his arrival he entered on the responsible duties of his profession, and had the control of large sums of money, £28,000 having been spent by him in erecting civil and military buildings; and at one time he had five thousand natives under his orders, whom he had to instruct in bricklayers’ and masons’ work. To make up for the scarcity of limestone, he examined the _ beach, and, finding that there was a considerable bed of recent shells in the neighbourhood, he persuaded old women and children and infirm villagers, by liberal offers, to collect them in baskets; and so great was the quantity obtained, that the kilns were filled and the building rapidly erected. He was appointed interpreter to Major- General Keir, in Guzerat, in December 1817 ; temporary Assistant to the Superintending Engineer at the Presidency in February 1819; and Executive Engineer, Southern Concan, in September 1819. In 1820 he requested to be appointed. to survey the Southern e2 lvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Conean. The Chief Engineer considered ‘ the offer creditable to the activity of the officer ;” and Lieut.-Colonel Kennedy recommended that he should be permitted to commence on the proposed under- taking, as being in all respects highly qualified for executing such a work; and the Governor in Council authorized his bemg employed in making the survey whenever he could be spared from his other duties as Executive Engineer. He was thanked by letter on the 5th December 1820, by Mr. Pelly, the Collector and Magistrate in the Southern Concan, for the admirable internal organization of his department, and was then placed at the disposal of the Commander-in- Chief, to be employed on an expedition against the pirates in Arabia. His Report on Weights and Measures was noticed as “highly creditable to his talents and philosophical. researches,” and obtaimed a special acknowledgment from the Government, dated July 1822, which expressed their approbation of the ability and research it displayed. In 1824 Lieut.-Colonel Sutherland, Deputy Surveyor-General, bore testimony to the value of Lieut. Jervis’s services as a Trigono- metrical Surveyor, and in the same year the Government expressed its approbation of the “ zeal and diligence he had displayed in the preparation of certain Revenue and Statistical papers ;” and in June 1826, noticed in terms of approbation his ‘able and intelligent Report on the State of Education in the Concan.” In 1829 the Commander-in—-Chief (Sir Thomas Bradford) sub- mitted to Government, Captain Jervis’s application to be appointed Deputy Surveyor-General of India, on the death of the Surveyor- General, with his Excellency’s warmest and most unqualified re- commendation that it should be complied with. ‘Captain Jervis,” his Excellency adds, “‘ was employed under the late General Mudge, from whom he has the highest testimonials, in the grand, Trigono- metrical Survey of England in 1812. His Excellency conceives him to be the most qualified person that could possibly be selected for the situation to which he aspires.” He was appointed Inspecting Engineer of the Surat division in De- cember 1829; Superintending Engineer at the Presidency in 1830 ; in the same year Acting Inspecting Engineer in Guzerat; afterwards Executive Engineer in Ahmednuggur, and Acting Executive En- gineer in Belgaum, in March 1831. The Government expressed their satisfaction at the zeal and energy he had displayed in prosecuting his researches, and for information he had afforded respecting slate-quarries discovered in the Southern Mahratta country. In 1833 theichurch built by him at Belgaum was stated to reflect great credit :on his taste; and the following extract from a letter addressed to Captain Jervis, dated 8th August, 1831, will show the high estimation he had then acquired :—* The Governor in Council, highly appreciating the value of your labours, and desirous of securing to the Government and the public all the benefits that can be derived from them, accepts your offer to prepare a copy of your Statistical. Memoir of the Concan in a complete state and form for publication;” ——— ANNIVERSARY ADDRESS OF THE PRESIDENT. lvii In February 1835 the Government reported that Captain Jervis had completed his statistical reports and memoir on the revenue-sys- tem of the Concan, and had furnished a volume of beautifully executed maps and plans, ‘‘ which reflect great credit on him.” In 1835 also the acknowledgments of Government were conveyed to him for his ‘‘ curious and interesting volume on Weights and Measures ;” and the Governor in Council stated that he considered Captain Jervis deserved great credit for having devoted his spare time and distinguished talents to the illustration of so difficult a question. He was appointed Superintending Engineer at the Presidency in ~May 1835; and member of a committee to take into consideration the best plan for the construction of a causeway between Bombay and Colaba in October 1835 ; and the Government subscribed for fifty copies of his Statistical and Descriptive Memoir of the Western Coast of India. On his quitting India on furlough to Europe in 1836, Government expressed “ the high sense which they entertained of his character, professional skill, and talents. Before his departure he drew up a code of instructions, at the request of Sir Thomas Bradford, the Commander-in-Chief, in three languages,—English, Hindustani, and Mahratta. In 1837 the Court of Directors awarded him a donation of 10,000 rupees as a testimony of the high sense which the Court entertained of the value of his labours in conducting the geographical and statistical surveys in the Concan. In 1838 the Court expressed their approbation of ‘the zeal evinced by him for the advancement of the objects of the Survey of India by making himself fully ac- quainted with the details of the system which is pursued upon the Irish Survey ;” and about the same time he was appointed to super- intend a series of tide-observations to be made upon a uniform prin- ciple at various points of the coast of India. He returned to his duty in October 1839, and was appointed Superintending Engineer, Northern Provinces, in March and May 1840. On his retirement from the service in December 1841, the Governor in Council stated that “‘ he will have much satisfaction in bringing to the notice of the Court of Directors the services of Major Jervis in the several branches of his particular profession, and also as an officer eminent for his general science and research ;” and the testi- mony borne to his services by the Bombay Government was creditable to him and most satisfactory to the Court of Directors. In 1830 Captain Jervis married Miss A. 8. Paget, daughter of William Paget, Esq., M.D., 48th Regiment; and this lady, having been the intimate friend and coadjutor of Mrs. Ibbetson the botanist, was an able assistant to Captain Jervis in his description of the in- digenous flora of the Concan, as she made water-colour drawings of almost all the flowering plants and trees of the Province: the work he then projected has not however been published. Whilst in London, Major Jervis drew up a statement of the scientific researches which he deemed to be desirable in Shedda; and this comprehensive report was considered so valuable and so im- portant, that a memorial was addressed to the East India Company lvili PROCEEDINGS OF THE GEOLOGICAL SOCIETY. on the 14th of July 1838, signed by His Royal Highness the Duke of Sussex, as President of the Royal Society, and many of the most illustrious members of that and other Societies, urging that the Government in India might be directed to forward in every possible way his views ; and no one expressed himself with more characteristic and generous warmth in his favour than Sir Roderick Murchison. About this time Major Jervis had been appointed Surveyor-General of India in succession to the present Colonel Everest; but, finding after his return to India that that officer had no intention to retire so soon, he gave up his hopes of being ever able to carry out his favourite project, and retired, as has been stated, from the service, in January 1842. Whilst in India his discovery, and application to useful purposes, of lithographic stone, and his examination and description of the slate-quarries he had first discovered in the Western Ghats, and his report to Lord Clare and the Governor-General of India on the geological structure of that portion of Western India which les be- tween the 15th and 19th degrees of north latitude, were all important scientific services ; and on his return home the activity of his mind did not relax, and he spent his time in educating his own family, seeking to find some congenial employment that might keep his faculties in full exercise. In 1843 he began to set up with his private funds a lithographic press, for the purpose of promoting the education of the natives of India, whom he loved to his dying hour, and wished to see enlight- ened. The productions of his press were all of a useful character ; _ and the first thing he did was to prepare forms for the E.I.C. for the collection of revenues, the management of the marine engines of the navy, and a variety of other forms, which he furnished, by the highly scientific processes he adopted, at a very moderate charge. Among the various papers which Major Jervis proposed to the Indian Government is one which is of great importance, as it urged the adoption of properly lithographed post-office-orders in India. In writing to Lord Hardinge, March 24, 1845, Major Jervis says: «« A Government post-office-order and letter of advice, in the opinion of General Morrison, formerly in the Supreme Council, several of the most eminent judicial authorities lately in India, and many of the members of the Court of Directors, would go further to suppress murders, crimes, and misrule consequent on the transmission of money by private hands than any other thing.” The few maps and papers printed by Major Jervis at his private press were equal to the best of the day, according to the testi- mony of many able geographers; and Mr. Greenough thus writes, «‘ Your map of the Duskrooe Purgunnah is admirable both in design and execution: would that the whole of India were laid down on your model!” (December 6, 1844); Sir G. Rennie says, “I could not have conceived the perfection to which the lithographic art had arrived till I saw these specimens, although we have have had much experience in our dealings with the trade for railway and other maps” (January 21, 1845); while with regard to the maps of ANNIVERSARY ADDRESS OF THE PRESIDENT. lix India in the vernacular languages, which Major Jervis was desirous of making for the missionary-schools, had funds permitted, Mr. Davis, the best Chinese scholar of all Europe, speaking of the Plan of Pekin, was pleased to say that it was the Jinest specimen of Chinese writing he had ever seen, and he would compare it with the native Chinese. Nor was the encouragement of native female education a trifling object aimed at by Major Jervis, who felt how important the example of mothers must be in after life to the rising generation. At the commencement of the Russian war, Colonel Jervis examined the materials forthcoming to enable the allies to gain a knowledge of that country, and early fixed upon the magnificent map of the Crimea which had been prepared by General Mukhin and the Russian staff. He obtained permission to trace it himself at a Continental library, and, having completed it and translated the names into English, brought it to England to lay it before the Duke of New- castle, along with other rare documents not to be procured in Eng- land. After urging the subject long and frequently, and impressing upon the Government the absolute necessity of having geographical information for the troops, his Grace permitted him to furnish two or three copies of each of these documents, officially, to commence with. In ten days—less time than he could have sent to Vienna for another copy of the Austrian map of Turkey—he produced, entire in twenty-one sheets, two hundred copies at the service of the Govern- ment! The map of the Crimea was also ready before the army left Varna; and by it Lord Raglan mentions that he made his flank movement by MacKenzie’s farm. Soon after, the Government sent copies of these maps to the general-officers ; and in alluding to this subject, Colonel Jervis wrote thus to the Duke of Newcastle :—(1854.) “I believe it is not generally known that the present is the first war in which the British forces have been supplied with the most needful help to success, correct and suitable land-maps. To your Grace and Lord Raglan’s acceptance of my services is ascribable, as well as to the exertions of the Hydrographer at the Admiralty, Admiral Sir F, Beaufort, and his coadjutor Capt. Washington, R.N., that the army has been furnished with the earliest and best information of the distant countries in which they are now engaged. ‘This service as regards the army has been honourably recognized by the principal Staff- Officers, the Commander-in-Chief, and many distinguished personages in France and England ; nor least by her most gracious Majesty the Queen, the Emperor of the French, and the Ministers of War and Marine.” In an unknown country, on a conflict so momentous, geo- graphical information must be inestimably valuable. Much of this important service was carried out at his own cost and by his own and his son’s labour ; and he pressed upon the Government in very emphatic terms the advantage which would be derived from the establishment of an office in connexion with the army, similar to that of the Hydrographical Office connected with the navy. After some months, Colonel Jervis procured from the French Go- vernment 1476 maps of the choicest kind, and offered these as a nucleus for the new office. Soon after, he was appointed, March 1855, lx PROCEEDINGS OF THE GEOLOGICAL SOCIETY: to be the Director of the Topographical and Statistical Depot of the War Department, with one assistant to attend to the details of work- ing, &c., and, to act as his deputy in his absence, his son, Mr. W. P. Jervis, all other assistants bemg merely hired by the week. This was almost the last work of the Duke of Newcastle, and will doubt- less be remembered as one of the greatest improvements in the orga- nization of our army, for the first step taken by Colonel Jervis was to impress the Minister with the importance of attaching to his office a set of intelligent officers who should form a topographical corps, and accompany the troops in the Crimea, Asia Minor, and indeed in every campaign. The first corps sent out under Colonel Jervis, and equipped with instruments, &c., went to Erzerum, where they surveyed the whole sources of the Kuphrates on a large scale, and the plain and town of Erzerum, sketching in the hills, &.: this survey was afterwards employed in connexion with the frontier-survey from © Ararat to the coast. Lord Panmure did not sanction a topographic.l corps for the troops at Sevastopol, though the Engineers of the Turkish Contingent were regularly supphed with instruments and materials from the Topographical Depot, and sent home some valuable maps. It may however be observed that the propriety of attaching a scientific corps to the Crimean army had been submitted to Lord Raglan by a different person, and that the project would have been carried out had not insurmountable difficulties appeared in the way. Lieut.-Colonel Jervis had the merit of originating the important establishment of a Topographical Office in the War Department, and he did much with limited means; we must not however condemn the higher authorities for not at once raising such an establish- ment to its utmost elevation, as no men in power can neglect the necessary economy of public money. It cannot be doubted that the Topographical Office will go on improving in excellence and importance, and that the remembrance of its first head will be long associated with it. The works of Lieut.—Colonel Jervis on geo- graphical and other scientific subjects were very numerous; and I may mention especially, as proofs of his labour or ingenuity, his model of Sevastopol, which is in the War Department (it is 14 feet by 10, on a scale of ten inches to a mile, with true altitudes, and was coloured skilfully by the kindness of Mrs. Colonel Jervis), and a new system of projection for maps, called by him “ cycloidal,” and which has been employed in his official maps of the Caucasus (two sheets) and the 8. W. of Asia, Circassia, the Caspian, &c.; of these, nine sheets are more or less completely engraved and issued. Lieut.-Colonel Jervis is now gone; but we may fairly say that the East India Company has seldom possessed an officer of more energy and ability, that his services at home were very valuable, and that in every respect he was a most kind and estimable man, fulfilling all his duties, as a loyal subject, a faithful husband, and an affectionate father, in the most exemplary manner. Grorcr Wearr Brackenriner, F.S.A., was born on the 4th of January, 1775, in Hanover County, Virginia, at that time still sub- ANNIVERSARY ADDRESS OF THE PRESIDENT. xi. ject to the British crown. He was the eldest son of George Brack- enridge of Winash, Brislington, who was a Scotchman by descent, though born at Bristol, where his family had recently settled, and of Sarah, youngest daughter of Francis Jerdone, Esq., of Louisa County, Virginia, and formerly of Jedburgh, N.B. The father of Mr. Brackenridge had settled in America as a planter and merchant ; but, entertaining conscientious scruples on the principles and pro- priety of the American revolution, he returned to England, and placed his son at the school of Dr. Estlin, at Bristol, where he was initiated in the mysteries of commercial pursuits, and became ulti- mately the senior partner in a leading and long-established West India firm. As a man of business he was characterized by high principles of honour and integrity, and by habits of accuracy and. punctuality. He exhibited at an early age a taste for science and literature, and in spite of the demands of commerce upon his time, Geendered more absorbing by the distractions of the revolutionary war, he found leisure for inquiries into medizeval antiquity and more than one branch of natural history. He formed a good collection of the Coleoptera; and his cabinet of organic remains, which in the early days of geological science was of much repute, is still of value for its specimens of fossils connected with the strata of the West of England, He was very accurate in his examination of fossils, and brought under the notice of Mr. Sowerby a specimen of Ammonite, remarkable for the striking and peculiar form of the lip, which was found at Dundry, near Bristol. Before arriving at his fiftieth year, Mr. Brack- enridge abandoned his commercial pursuits, and purchased the resi- dence of Brislington. He had before, ike many of our leading men of science, found it possible to exercise the faculties of his mind during many a leisure moment on objects of more stirring interest than the dry details of business ; but he now gave himself up. to the full gratification of his refined tastes, collecting much more largely than he had done before, fittmmg up his library in the Tudor style, and enriching it with richly-cut furniture, and with fine specimens of stained glass. As an antiquary, he devoted much attention to the investigation of the architectural features of Bristol, that picturesque old city, where he had passed so much of his early life, and to the preservation of many of its ancient relics. He assisted most liberally in procuring the best illustrations for ‘ Collinson’s History of Somersetshire,’ which work must therefore be looked upon as bearing testimony to his love of topographical research. Having for the last twenty years of his life spent the summer and autumn at Clevedon on the Bristol Channel, he liberally promoted the building of a new church on Clevedon Hill, contributing the greater portion of the building-fund, and adding a permanent endow- ment: his son was appointed its first minister in 1839, when the church was consecrated. Though, from his retired and domestic habits, he was not generally known in his neighbourhood, he was valued by those who did know him for the kindliness of his dispo- sition, his great powers of conversation, and the many sterling qualities of his character. He married, Nov. 11, 1800, Mary, young- est daughter of Robert Burt, Hsq., of Bristol, and of Tracy Park, Ixii PROCEEDINGS OF THE GEOLOGICAL SOCIETY. near Bath, who died March 20, 1855. He was not long left behind her, as he died February 11, 1856, at his house at Brislington, near Bristol, aged 81. Cuartes Wittram Wentworts Frrzwittiam, fifth Earl Frrzwm- tram, K.G., was best known to the world as an enlightened liberal politician, but his claim on our respect is founded upon his desire to promote the intellectual advancement of his fellow men, as manifested by the fact that since the year 1833 he filled the office of President of the Yorkshire Philosophical Society. He has been succeeded by the Earl of Carlisle, but the services of twenty-eight years’ presi- dency are not likely to be forgotten by the members of the Yorkshire Philosophical Society. Asa soldier myself, I cannot pass by the name of Colonel W. G. Error in silence, though I have been unable to obtain any specific notice of his life. The officers of our military and of our naval pro- fession should be encouraged to enter upon a study which is so ¢a- pable of being made valuable in practice ; and the very fact of joining our Society proves that regard for science which it is our object to inculcate and to cherish. _ [ have now to notice the distinguished foreign members whom it has been our misfortune to lose during the past year, and I shall begin with M. Awpr& Husert Dumont, who was so well known to many of our leading members, and whose career, though short, was productive of great results. He was born in 1809: and such was his earnest pursuit of his favourite science, that at the age of twenty (in 1829), he produced his first geological essay on the “ Geological Constitution of the Province of Liege,’ and addressed it to the Royal Academy of Belgium. by which body it was crowned with honour. Ten years afterwards the merits of this work obtained for M. Dumont the award of the Wollaston Medal from our Society. In 1834 (April 5) he was chosen a corresponding member of the Bel- gian Academy, and in 1886 (Dec. 15) he was admitted a regular member. About the same time, at the recommendation of the Dean of the Academy, and of the late M. Cauchy, also a member of the Academy, M. Dumont was named, by the Government, Professor of Mineralogy and Geology to the University of Liege, and was requested to undertake the difficult and important task of drawing up a geolo- gical map of Belgium; and it is much to be feared that, honourable as that work must be considered to his native country and to him- self, the labour and anxiety counected with its preparation were fatal to his health. In 1852 his Memoir on the Rhenish and Ardennes Formations, in- eluding the Ardennes, Brabant, Condroz and the Rhine, shared with De Koninck and Van Beneden the first great quinquennial prize in the natural sciences decreed by a jury selected from the Academy. In January 1855 the Academy selected him as its director for the year 1856, and he had only completed his year of office two months when he was snatched away by death; and it may be considered a touching ANNIVERSARY ADDRESS OF THE PRESIDENT, dx incident, that the only survivor of those members who assisted at the foundation of the Academy, M. D’Omalius d’Halloy, came to Belgium to bid adieu to Dumont, whose early progress he had encouraged, whom he loved as a son, and by whom he was revered as a parent. For twenty years his life was devoted to the preparation of the geo- logical map, during which time he shrank from no labour either of body or mind, exploring every spot in Belgium, and not allowing a single geological fact of importance to escape his attention, so that his inquiries extended from the primary to the tertiary formations inclusive. The merit of the map cannot be disputed, even though doubts may be entertained as to the nomenclature made use of ; and we may adopt the following words of one of his eulogists without re- serve: “ Though he was, perhaps from a natural disdain for ordinary means of success, too careless about popularizing his ideas beyond the class he taught, his maps will retain their value, even though it may be necessary to change his nomenclature ; and they are so manifestly stamped with the character of exactness and reality, that it may be expected that the divisions which he has adopted will be hereafter taken as general types of formations: indeed they have already been adopted in Germany for many formations, so that they have already obtained a place in geological science.” The failure of his health forced M. Dumont to travel; and he discovered on the shores of the Bosphorus, and on the mountains of Spain, formations equivalent to those he had recognized on the plains of the Ardennes and of Con- droz; and it was then that he conceived the idea of forming a geo- logical map of Europe, a map which has appeared, and must be looked upon as one of the first serious attempts to establish on a large scale the geological correlation of the various countries of Europe. | . Like our late friend Mr. D. Sharpe, to whom he was well known, he was snatched away in the very prime of life, and at a moment when still greater advances in geological science might have been reason- ably expected from him. The University and the Government of his country had however done much in that brief time to testify their estimation of him. Many of his academical honours have been al- ready noticed; but it may be mentioned that he was a Commander of the Order of Leopold, a Knight of the Order of Conception of Villa- Vicosa of Portugal, and of the Polar Star of Sweden, whilst he was a member and one of the founders of the Royal Society of Sciences of Liege, Member of the Society of Sciences, Arts and Belles Lettres of Hainault, Honorary Member of the Central Society of Agriculture of Belgium, of the Association of Engineers, formed on the model of the School of Mines, and of the Society of Emulation, Member of the Academies of Naples and Turin, formerly President of the Geological Society of France, Member of the Imperial Society of St. Petersburg, of the Society of Naturalists of Moscow, Corresponding Member of the Society of Physical, Chemical, and Agricultural Sciences of France, and since 1841 a Foreign Member of our Society, the loss of whom will be deeply regretted by many of our members, and by none more than Mr. Austen and Mr. Prestwich, both of ee were intimately ac- quainted with him personally and knew well his worth. _. The preceding observations are sufficient to prove how fully. M, lxiv PROCEEDINGS OF THE GEOLOGICAL SUCIETY. Dumont had earned the high character for unwearied zeal and energy in geological research, ascribed to him not merely by his own country- men, but by the geologists of all Kurope: some further remarks on his writings are, however, necessary to give a clear idea of his great and varied talents, as well as of that independence of mind which led him perhaps sometimes to an excessive dread of being shackled by systems. The Memoir on the Geological Constitution of the Pro- vince of Liege was his first great work, and gained the prize offered by the Academy of Brussels for the essay which should best fulfil the following conditions : ‘‘ describe the Geology of the Province of Liege ; point out the mineral species and accidental fossils which are there found, the localities where they occur, and the synonyms of all sub- stances already known and which have been before described.” There were two other competitors for this prize; and the epigraphs attached to the papers of Dumont and of his next ablest opponent, who gained a silver medal, are as follows: that of the second com- petitor was a passage from Baillet to this effect,— & weno 4 vie ary dae. meh SAgri iy 3 . ‘ at ce Set ‘ 4 iy 3 , a! my ite * d reset: 6 Ue as Se 5 Ly * er See sg ee fF jay Rees: tov THE QUARTERLY JOURNAL OF THE GEOLOGICAL SOCIETY OF LONDON. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. AprRIL 22, 1857 (continued*). 3. On the Grotocy of Strats, Sxye. By A. Gerxis, Ksq., of the Geological Survey of Great Britain. With Descriptions of some Fossiis from Skye ; by T. Wrigut, M.D., F.R.S.E. [Communicated by Professor Ramsay, F.G.S.] [Puate L+] ConTENTS. Introduction. Limestone-breccia. I. Character and sequence of the Lias- Igneous rocks—syenite and trap- sic beds of Strath. dykes. II. Geological structure of the Strath Metamorphism. Valley. Faults. Coast-sections. Conclusion. Interior. Introduction.—The first notice of the district described in the present paper was that published in 1800 by the late Professor Jameson in his ‘ Mineralogy of the Scottish Isles.” It is exceedingly meagre, having been compiled from the notes of a brief excursion in bad weather, and contains only a list of minerals found in the ascent of Beinn na Cailleaich, with the mention of numerous basalt-veins * See vol. xiii. pp. 360 e¢ seq. t+ The Sections figured on this Plate have been selected from the series of sketches communicated by the author as illustrative of the Geology of Strath, and now in the Society’s Library. The unfigured Sections will be referred to in the paper. VOL. XIV.—PART I. B 2 PROCEEDINGS OF THE GEOLOGICAL sociETy. [April 22, that traverse the limestone in every direction*. Eighteen years later Dr. Macculloch published his ‘ Description of the Western Islands,’ wherein he pointed out the existence in Skye of secondary strata—the equivalents of the lias and oolite of England, extending in broken and irregular series up to what has since been determimed to be the equivalent of the Oxford Clay+. He also described with considerable minuteness some of the more remarkable features m the geology of Strath. Yet of the structure of the district he seems to have had but a vague general idea—not a few of its most important features having escaped his notice, while of some of the facts which he mentions he has failed to perceive the true bearing. I shall even have occasion to show that, notwithstanding the minuteness of his description, he can only have examined a limited portion of the di- strict, and that too but superficially. Several years later Sir Roderick Murchison examined the eastern coast-line of Skye, and, from a comparison of fossils, ascertained the existence and limits of strata belongmg to the lias, and the lower and middle oolitet ; and I am not aware that, since the date of this paper, any further observations have been made upon the south- eastern part of the island. | That portion of Skye of which I offer a description to the Society comprises nearly the whole of the parish of Strath. It may be re- garded as an irregular belt from three to six miles in breadth, extend- ing from sea to sea where the island narrows most. Its physical features are those of a wide undulating valley between two elevated ranges—the red sandstone and gneiss hills of Sleat to the south, and the syenitic mountains of Beinn na Cailleaich and Bein Dhearg to the north. This district—embracing an area of nearly thirty square miles—includes the largest development of the lasin Scotland ; and, indeed, as that formation in its lower and middle divisions reaches here a thickness of not less than 1500 feet, it may be regarded as no unfair representative of that of England. The geological structure of Strath—so intricate and confused—gives to these liassic beds an additional and peculiar interest. Along the shores the strata form low reefs and skerries, brown with alge, and extend in regular se- quence throughout their series. Yet no sooner do they strike into the interior than, in many localities, all seems to be involved in hope- less confusion ; regularly stratified limestones become crystalline amorphous marbles; shales assume the appearance of metamorphic clay-slate or burnt pottery; great outbursts of syenite cut through the beds, dislocating, contorting, or overspreading them ; trap-dykes in countless numbers traverse the glens and the hill-sides ; while, by the agency of faults, higher members of the group are thrown down among the lower, and long tracts of red sandstone are brought into the heart of the lias. Before attempting to detail these complicated appearances, I shall describe the character and order of the beds from their base upwards. * Jameson’s ‘ Mineralogy of the Scottish Isles,’ vol. ii. p. 91. t+ Forbes, Quart. Journ. Geol. Soc. vol. vii. p. 104. } Trans. Geol. Soc. 2nd series, pp. 293, 353. 1857. ] GEIKIE—SKYE. 3 I. Character and sequence of the Liassic beds of Strath. It is a somewhat remarkable fact that in Scotland the Lias invari- ably rests on a paleeozoic or metamorphic base—usually Old Red Sandstone. And it is equally striking that the formation is confined to the northern counties, among the hypogene and older paleozoic districts ; none being found to the south of the great granitic barrier. These facts are of importance in investigating the physical history of the country. The lias of Skye rests sometimes conformably and often unconformably upon red sandstone or purplish-grey quartz- rock. ‘These underlymg beds have never yet yielded any organic remains, so that it is uncertain whether they should be regarded as Old Red, Silurian, or some of the later portions of the gneissic series of central Scotland. ‘They graduate southwards, according to Mac- culloch, into a series of gneiss- and mica-schists; but considerable doubt rests upon their stratigraphical relations, and it does not seem probable that the difficulty can be cleared away without a careful and somewhat extended examination, not merely of the rocks in Skye, but of their prolongations into the mainland*. The boundary-line of the lias and red sandstone commences on the north-eastern shore at the village of Lussay, whence it proceeds in a south-westerly direction for three miles to a point about half a mile south of the village of Sculamus, from which it runs nearly due south to the hamlets of Heast on Loch Hishort. See Map, Pl. I. fig. 1. This is a well-marked line; for the observer may not un- frequently stand at the same moment upon lias and red sandstone. The only part on which there hangs a shade of uncertainty is at the turning of the beds near Sculamus, where, owing to the thick cover- ing of peat and the swampy nature of the ground, the two rocks cannot be approximated quite so closely as along other parts of the Ime. Yet this and similar obscurities could be shown only on a map of a very large scale. I have been not a little surprised by the manner in which this Ime is mapped and described by Dr. Macculloch. He commences it at the head of the long narrow creek of Obe Breakish, instead of at. the village of Lussay, thus colourmg as red sandstone a space of fully two miles in length, which is actually lias. After quitting the shore his line is undefined, the formations being shaded into each other, indicative of a very uncertain boundary. Beyond this a large mass of syenite is introduced, breaking through the line, and for about three miles separating the two rocks. They are re- presented as meeting again to the south of the syenite, whence they run south-west to the shore of Loch Eishort, near the farm of Borereg—an error of considerably more than a mile. His lines are thus frequently set down at random, great tracts of red sandstone are altogether omitted both im map and memoir, the existence of faults is ignored, long tracts of syenite are inserted where none exist * Since this paper was written, Professor Nicol’s Memoir “On the Red Sand- stone, Quartzite, &c. of N.W. Scotland” has appeared in the Quart. Journ. Geol. Soc. vol. xiii. p. 17. Bee 4 PROCEEDINGS OF THE GEOLOGICAL society. [April 22, in nature, and false dips are given, by which the very lowest beds are made continuous with the highest parts of the series. It pains one therefore to find such statements as the following :—“ Fortunately a rigid topographical detail is but of little moment ;” “and there is the less reason therefore to dwell on those minutie, though they have been examined in the most scrupulous manner ;”’ “‘ commencing from the lowermost beds, it must be remarked, that it is impossible to trace their common boundary with the red sandstone*.” And there are many other passages where, by a similar bold assertion or by a certain vagueness and ambiguity, the author leads his readers to take for granted what he affirms, and to give him credit for having observed a great deal which he has not thought it necessary to narrate. These remarks are made with much diffidence and reluctanee. It is a delicate task to criticise the labours of one of the earliest culti- vators of geological science, especially one of his works which has ever ranked among the standard treatises on British geology. And when I reflect that his account of this limited area is one of the fullest and most elaborate parts of his “‘ description,’ embracing about twenty-five pages of letter-press, I am sensible that my remarks tend to throw a shade of discredit over other portions of his work on the Western Islands. But it was impossible to pass over the subject in silence. The lowest bed of the lias (PI. I. fig. 2) is a sandy conglomerate, averaging 2 or 3 feet in thickness, and traceable from near Lussay at intervals along the boundary-line to Heast. It is formed of well- rounded pebbles of red sandstone and white quartz—the waste of the surrounding knolls that formed reefs and skerries when the Scot- tish lias began to be thrown down. To this succeed, at Lussay, beds of white and greenish chloritic sandstone, varying from 3 or 4 to fully 15 feet in depth. Next follows a seam of dark-blue com- pact limestone about a foot thick, surmounted by a stratum, irre- gularly 2 feet deep, of massive Isastree enveloped in a dark sandy clay. This remarkable bed escaped the notice of Dr. Macculloch : it was first observed by Sir Roderick Murchison; and afterwards examined and described+ by one who has scarcely left a district of his country unvisited, or unrecorded by his classic pen—the late lamented Hugh Miller. I have not succeeded in detecting the coral-bed in the interior of the island ; it probably thins out at no great distance from the shore. Above the corals there are 7 or 8 feet of a calcareous grit, which shades off into aseries of dark blue limestones with occasional courses of shale. The calcareous beds are not peculiarly fossiliferous, show- ing however on the weathered surface mouldering casts of Ammonites and Gryphee, and on a fresh fracture the minute joints of Penéa- * Description &c. vol. i. pp. 316, 317. + In a paper read before the Royal Physical Society of Edinburgh, 21st April, 1852. This coral was mentioned at the Cheltenham Meeting of the British Association by the Rev. P. B. Brodie, to whom I sent a specimen. See also Edinb. New Phil. Journ. April 1857, p. 263. 1857. | GEIKIE—SKYE. 5 erinites. The shales too, when contrasted with those higher up in the series, are remarkably barren in fossils. The long narrow peninsula at Obe Breakish consists, on its south- eastern side, of beds of white sandstone, and along its north-western shore of a thick deposit of dark sandy micaceous shale abounding in Gryphee. Above these shales there occurs in the interior a stratum of brecciated conglomerate formed of lias-limestone and red sandstone fragments. From Breakish to Broadford the shore is occupied by low shelving reefs of dark blue limestone with alternating courses of shale. As the rocks approach Corry, beds of calcareous grit often charged with Gryphee begin to appear. The series described up to this point corresponds in position to the lower lias of England. Beyond Corry and on the opposite island of Pabba there begins a series of dark micaceous and sandy shales abounding in fossils*, and answering to the lower horizon of the English middle lias. The syenite of Beinn Bhuidhe descends to the shore north of Corry ; but the shale can still be traced along it as far as the entrance of the Sound of Scalpa, where the last beds visible are of sandstone, greatly disturbed by syenite and trap-dykes. The series is, however, pro- longed on the coast of Scalpa Island near Scalpa House, where a series of calcareous shales rest unconformably on the red sandstone, which has herea south-easterly dip. The organisms of these shales are in a wretched state of keeping, but some of the better-preserved Pectens suggest a comparison with the marlstone of England. The continuation of the series through the upper lias will doubt- less be made out along the eastern coast-line of Skye and Raasay, but my explorations have not hitherto extended further north than Scalpa. The sequence of the beds described will be at once perceived from the subjoined Table. Table of the Lias of Strath. Dark calcareous shales (with Pectens, &c.).......... Scalpa. Middle Lias. « Dark-grey or brown, sandy, micaceous shales (with UHC LOUSSLOSSIIS) Wie cwedcdesewaaarce-ahdadestsemcnsece Pabba. Calcareous grits (with Gryph@@).........0e0..s.ee0e Peete na Nie in Cote bands... 2. e.-.. ERIE Calcareous brecciated conglomerate..............2+0. (Inland.) Dark brownish-grey sandy shale (with Gryphee). \ Ohe Breach: Wikiite SamG@siQMe, - sone soccc tea temnemeseae «ecescsgese=s Hip eaias 4 Limestone and occasional seams ) (with Ammo- | ep OU SWAG. os ercn a. maw asnesie coe nites, Gryphites, | Calcareous grit ; 7 to 8 feet ... } and Pectens). Coral-bed ; 2 feet ([sastraa) ........++eseeccccseessess > Lussay. THESTOR Es BU TODI oy. eecceee dec Sacte sone ccee =< deces. cs Green and yellow sandstone; 3 to 15 feet ......... | Fine conglomerate; 2 to 3 feet............--eeeeseeeee J Red sandstone and quartz-rock. The dip of these beds from their base at Lussay to their top at Scalpa House (fig. 2) is pretty uniformly 5°-8° to the north-west ; * For a description of the fossils collected in Strath I am indebted to the kindness of Dr. Wright. See APPENDIX. 6 PROCEEDINGS OF THE GEOLOGICAL society. [April 22, and, as the distance is nearly four miles, their entire thickness must be at least fully 1500 feet. II. Geological Structure of the Strath Valley. Coast-sections.—The previous enumeration of the liassic strata of Strath is in reality a description of the beds seen in section along the north-eastern shore (Pl. I. fig. 2). They follow each other regularly, from the sandstones and coral-bed of Lussay up to the Scalpa shales, with no material disturbance from faults or igneous rocks. The struc- ture of the south-western coast-line is somewhat more complex. At the head of Loch Slapin (fig. 4), among the roots of Bein Chro and Beinn Dhearg Mor, there occurs a set of limestones and shales occupying the same horizon as those of Breakish. In the bed of the stream that descends between these two mountains a few yards of altered limestone abut against the syenite of the hills ; this is followed by a series of indurated shales with occasional fragments of Belem- nites; and further down the water-course, a hard bluish-grey and streaked metamorphic limestone becomes the prevailing rock. The dip of these beds is S. by W. at angles of from 25° to 60°. They are capped on the shore at Torrin by a small patch of shale, seen only at low-water, which may possibly represent the under portion of the Pabba series. Following the eastern shore of Loch Slapin, we find the dip turning round to the north-west, and the same series of altered limestones again presenting itself. The bedded structure of the rock is nearly obliterated ; but, where the angle of dip can be observed, it _ increases southwards beyond the Torrin promontory, until the shore is covered by a great protrusion of syenite, which stretches eastwards for three miles, forming the long ridge of Beinn an Dubhaich. It extends along the shore for about half a mile, and, at the promon- tory south of Camus Smalaig, is succeeded by the limestone as before. South of this junction the beds dip 8.W. at 15°-25°, where the bedded structure begins to reappear. They gradually lose their metamorphic aspect, till at the mouth of the stream which descends from Glen Kilbride, they pass into a coarse shelly limestone abound- ing in Gryphee. ‘The grits and limestones, which for a short space succeed, are the equivalents of similar beds between Broadford and Corry ; and, as in that locality, so also here, they are surmounted by a thick set of dark micaceous shales, identical in character and fossils with those of Pabba. They stretch into the interior for upwards of a mile, whence they deflect to the south, and reach the shore of Loch Eishort at Borereg,—thus occupying the tongue of land which separates the two lochs. At Suishnish Point they are covered by a patch of yellow calcareous sandstone, which, at one part, displays a rude grotto with pendent stalactites, like not a few other caves formed by the decomposition of trap-dykes along ‘‘ Slapin’s caverned shore.” This lip of sandstone is succeeded by the same series of shales dipping N.W. at 3°-5°. Half a mile from Suishnish they are inter- rupted by a large mass of augitic greenstone, which has broken through and overflowed them atop. The headland of Carn Nathrach is formed by this protrusion of greenstone surmounted by another of 1837. | GEIKIE—SKYE. 7 fine-grained syenite. At Borereg the shales strike inland, as already mentioned, and are succeeded by a set of limestones and thin shales —the representatives of the limestones of Broadford and Torrin*. The Sketch No. 1. illustrates this locality. The occurrence of quartz-beds in the limestones at this locality is interesting, Inasmuch as it proves that pure white crystalline quartz- ite is not necessarily a product of igneous influence. The syenite of Bein na Chara, it is true, is only ashort way distant ; that it could not, however, have had any material effect upon the quartzite is abun- dantly evident from the unaltered character of the interstratified limestones ; and if further proof were needed, it would be found in the occurrence of a precisely similar quartzite among the limestones of the interior, on the ridge to the south of Glen Kilbride. There it rests on an elevated belt of red sandstone, and is overlaid by a lime- stone-breccia, and a series of unaltered limestones. The nearest syenite is that of Beinn an Dubhaich on the other side of the Glen, but a large fault intervenes between them. There is, indeed, a small basalt-dyke traversing the lias-beds at this point, but it is of much too trifling extent to have produced the supposed metamorphism ; while I shall take occasion to show that the trap-dykes of the district generally have not exercised any marked influence upon the texture of its rocks. Of the quartz-beds on Loch Kishort, the upper, as ex- posed on the beach, is much jointed and fractured; and, as far as I could penetrate into its substance, it seemed to be a nearly transparent crystalline quartzite, with an occasional tendency to be dull and subgranular. The under bed is also a good deal fractured, owing, perhaps, at least in part, to the proximity of a fault. It forms a tall cliff, remarkable for its brilliant whiteness, and for the large snowy blocks that cumber the beach around its base. A fresh fracture shows that this peculiar brilliancy is chiefly owing to a thin crust, from }th to ;4,th of an inch in thickness, consisting of minute aggre- gated granules or crystals of quartz. Further from the surface the rock assumes the character of a very fine quartzose grit. The shore of Loch Eishort is now occupied by a great tract of red sandstone, extending inland as far as the north-eastern corner of Beinn na Charn. Its western boundary is formed by a fault, which throws out fully 400 feet of the lower lias, and brings down the Sculamus and Broadford limestones against the paleeozoic beds. The dip of the sandstone is generally westerly, at angles varying from 20° to 50°. Its eastern edge has likewise been produced by a fault that extends from near the north-east corner of Beimn na Charn to the village of Heast. This latter dislocation has thrown out a still larger portion of the lower lias ; and the effect of the two movements together has been to cut a rude scalene triangle out of the lias lime- stones and shales, inserting in their stead a corresponding area of red sandstone. ‘The Heast fault can be well observed in the channel of the stream, where the fractured ends of the limestones, shales, and breccia distinctly abut against those of the older strata. Beyond * With the above description of this coast-section, for the accuracy of which I can vouch, compare that by Macculloch ; Description, vol. i. p. 328. 8 PROCEEDINGS OF THE GEOLOGICAL socieTy. [April 22, the cultivated patches of Heast the coast-line is fringed with sombre, lichen-clothed crags of red sandstone and quartz-rock, stretching away to north-east over a bleak moorland region, and swelling southwards into the grey wrinkled mountains that form the long peninsula of Sleat. Interior.—I have now gone over the coast-sections of the district, whence a good idea may be gained of the general arrangement of the rocks in the interior. To describe that arrangement regularly in detail would be not a little tedious, and, from the want of local refer- ences, would be attended with inconvenience and difficulty. I have accordingly drawn several sections through the more remarkable parts of Strath, whereby much is shown at a glance that could not be so well understood even from the clearest description. These sections, with the accompanying map, will, I trust, convey a fair idea of the structure of the district. They show the Liassic region of Strath to be a great synclinal trough bounded on the north-west . by syenite, and on the south-east and east by red sandstone, and ridged up along its centre by an anticlinal axis. Notwithstanding this seemingly simple structure, there is not a little complexity when we descend to details. Thus, we should ex- pect that along the outer edges of the synclinal hollow, the lowest beds would be always those visible, but this is not strictly true. The most northerly of the sections, Pl. I. fig. 2, exhibits no sign of any bending of the beds: these follow each other in regular sequence from the lower conglomerate and coral-bed up to what is probably the marlstone. Section III., MS., and fig. 5 display the full swell of the anticlinal axis, and likewise the effects of denudation in partly baring the sandstone-ridge of its mantle of limestone. The lower beds seen at the eastern end of the line do not rise against the syenite at the western ; those visible along the flanks of Bein na Cailleaich belong to a higher part of the series. The shales and limestones at the foot of Ben Chro are not the bottom beds, nor do these occur at the other edge of the trough on the shore of Loch Eishort, for there, as shown above, the fault cuts off all the strata below the white quartzite. And thus, though the general structure of the district is that of a synclinal hollow, its regularity has been assailed by syenite and faults. Nor is there greater regularitv in the occurrence of the central anticlinal ridge. Eastwards it is produced by a broad undulation of the red sandstone and superincumbent lias without visible igneous rock ; westwards it is caused by a long protrusion of syenite, while midway there is a confused coalescing of the two axes. Moreover, throughout nearly the whole extent of this central area, the lime- stones have been so altered that it is no easy task to ascertain their true dip. They are ploughed up on all sides by trap-dykes ; faults have dislocated their connexion; great protrusions of syenite have ridged them up, and long tracts of red sandstone are found running through their centre. Instead, therefore, of attempting to describe this confused district, I must refer to the map and sections alluded to for the general dis- position and relations of the rock-masses, and content myself with 1857. | GEIKIE—SKYE. 9 describing under three or four subdivisions those appearances that seem most worthy of consideration in the geology of Strath. The first subject to which I shall advert is the long sandstone-ridge and its accompanying breccia. Limestone-breccia.—In detailing the sequence of beds along the north-eastern shore, reference has been made to a bed of limestone- -breccia which, though not visible on the coast, can be seen at many places in the interior. This rock and its attendant circumstances appear to have escaped the notice of Macculloch * ; yet it is a point of not a little interest, and throws some important light upon the physical history of the district. Its horizon lies a short way above the thick shale that occurs in the lower portion of the series at Breakish ; and this position it probably always retains. It varies in thickness from 3 or 4 feet to 10 or 12, and is made up of rounded and subangular fragments of quartz-rock, red sandstone, and lias-limestone. Its line is accurately defined by the eastern edge of a long belt of red sandstone (similar to that whereon the lowest lias-beds re- pose), around which it seems moulded. This narrow strip of sand- stone is bounded on the west by a fault that runs through the valleys of Glen Kilbride, Loch Lonachan, and Glen Shuardail, and is well exposed in the channel of the Shuardail Water, where it gradually dies out before reaching Sculamus. The other edge of the sandstone- belt is fringed by the breccia. Except at one spot on the southern ridge of Glen Kilbride, where, for a short way, there intervenes the lenticular mass of white quartz-rock already noticed, and also on the western slope of Beinn Shuardail, where the breccia is overlapped by limestone, the sandstone is always found to have a capping of breccia ; and, I make no doubt, were the anticlinal ridge of Beinn Shuardail stripped of the limestone by which it is enveloped, the sandstone below would be found girdled by a zone of breccia. The only locality where I have detected the latter rock away from the sandstone is in the bed of the stream that descends from the Black Lochs to Heast. The following sections will explain the structure . of that part of Strath. The Section through the northern end of Beinn Shuardail (fig. 5) crosses the anticlinal of red sandstone with the flanking breccia and limestones. The breccia probably thins out over the older limestone and shales as here delineated. Had it been continuous, we should have found it at 6' above the Breakish-shales. These lower beds must abut against the bottom of the breccia in the manner shown in the section ; for that they cannot pass above the breccia, is proved by the position which it occupies at Heast, and by the limestone- fragments with which it abounds. Assuredly it cannot be on the © same. horizon with the lower conglomerate found resting on the red sandstone from Lussay to Heast (fig. 4). The Section between Beinn na Charn and Hill of Harripool (fig. 6) passes south of the gap in the syenite-range of Beinn na Charn and * He does, indeed, mention a calcareous conglomerate next the syenite, but adds that ‘its connexions cannot be traced.’’—Description, vol.i. p. 325. 10 PROCEEDINGS OF THE GEOLOGICAL society. [April 22, Hill of Harripool. It differs from the preceding in so far as it shows the effect of the fault along the eastern side of Beinn Shuar- dail, and the reappearance of the breccia in the Heast stream at 0’. In Section FV. MS. a small knob of red sandstone is seen projecting through the limestone on the west side of Beinn Shuardail. I think it highly probable that this and another similar patch half a mile north are prominences of the underlying rock from which the over- lying limestone has been torn away, so that the breccia, though in- visible, may flank their base, as shown in the section. As corrobo- rative of this conjecture, I may remark that at Sithean, where the sandstone, divested of its calcareous covering, descends almost to the level of the road, the breccia is found resting above it ; but where the limestones begin to creep up the hill-side to the south, the breccia gets covered over, together with the sandstone below. I am thus particular in the details of this sandstone-ridge and its casing of breccia, because the appearances described appear to me indisputably to prove that the period of the Lower Lias of Skye was marked by movements of upheaval and depression. Whilst limestones and shales were alternately accumulating at the bottom of the old liassic sea, a long low reef was thrown up, raising with it the calcareous and muddy deposits that had formed the ocean-bed. Exposed to the beating of the surf, these strata were broken up, their fragments dispersed along the slopes of the reef, and the red sand- stone once more laid bare. At length the ridge began to suffer a downward movement, and, as it slowly sank, fresh accumulations of limestone gathered around and over it, in a sea swarming with Ammonites, Pinne, and Pectines. There is another point of interest im this sandstone-ridge which I am unwilling to omit. The remarkable parallelism of the mountain- ranges and glens of Scotland long ago drew the attention of geolo- gists, and the progress of investigation has shown that what is so marked in the north can be no less distinctly traced in the general structure of the British Islands. The great faults traced on the maps . of the Geological Survey have generally a parallel strike from south- west to north-east, corresponding with the direction of the Highland glens and straths. With regard to the relative ages of these upheavals and depressions mere parallelism can prove nothing, for there is strong reason to believe that at least most of the great disturbing move- ments which have taken place within the area of the British Islands, from the earliest eras whereof we have any cognizance, have been along a north-east strike. Now, the sandstone-ridge of Strath pre- serves the same direction, and, though invaded by the syenite of Beinn an Dubhaich and shattered by the fault of Glen Kilchrist and Glen Shuardail, it is still tolerably perfect for nearly five miles. Of its age there can be no doubt; it was formed towards the close of the lower horizon of the Lower Lias, and had begun to sink when the limestones of the upper horizon of that division were deposited. Many a long year had rolled away, and its site was well nigh effaced, when the Pabba-shales, belonging to the lower and middle horizons 1857. ] GEIKIE—SKYE. ll of the Middle series, were thrown down, enveloping the remains of Ammonites Jamesoni, A. brevispina, and A. Davei. The circum- stance is interesting, therefore, in a twofold point of view: Ist, because it proves that the disturbing agencies which afterwards played such an important part in Hebridean geology had already begun to show themselves as early as the time of the Lower Lias ; and, 2ndly, because it clearly indicates that m the same ancient period the forces which produced the parallelism of the Scottish glens and mountain-chains acted in the prevailing north-easterly direction. Igneous Rocks.—The igneous rocks of Strath belong to two great classes, and assume three distinct modes of occurrence. There are, first, the various hills and mountain-chains of syenite—huge amor- phous masses breaking through and overlying the liassic beds ; and, secondly, the innumerable dykes of augitic trap that cut the strata at every angle, and not unfrequently spread out between them in a bedded form. The northern limit of the liassic region was described as formed by a boid eruption of syenite rising into an elevated chain of mountains (see Map, Pl. I. fig. 1). The summits of these hills, bleak and bare, rise out of a thick mantle of shattered blocks and broken debris, which, together with the scantiness of the vegetation, give them an air of ruin and desolation. Beinn na Cailleaich, the highest of the range, attains an elevation of over 2000 feet. In addition to this great syenitic tract, there are numerous minor isolated portions scattered throughout the district. Of these the largest is Bemn an Dubhaich, which stretches eastward from the shore of Loch Slapin for about three miles, with an average breadth of about a quarter of a mile. Another syenitic hill of considerable size is Beinn na Charn, rising abruptly above the hamlets and cultivated patches of Borereg. It is of an irregular form, thickest towards the west, and tapering to a point in the opposite direction. The Hill of Harripool may be re- garded as a continuation of Bein na Charn. It runs as a long sloping ridge in the direction of the village from which it derives its name. The rocky headland named Carn Nathrach, that forms the point of Suishnish, is likewise a syenitic protrusion, having an irregularly oval form, and bulging out a little towards the west, like the other detached eminences. ‘There is but one other portion of considerable size in the district,—the rounded hill, called Ben Bhuidhe, that rises over the western arm of Broadford Bay. In addition to these, however, there occur numerous smaller erup- tive masses in various parts of Strath. One juts over the rugged path along the cliffs of Loch Slapin, between Glen Kilbride and Glen Suishnish ; another projects into the breccia between Loch Lonachan and Beimn na Charn. I have observed several more, and it is pro- bable that others may have escaped my notice. Indeed, after a somewhat lengthened examination of the district, the conviction forced itself upon me that there might be large masses of syenite hidden at no great depth beneath the surface, especially in the more 12 PROCEEDINGS OF THE GEOLOGICAL society. [April 22, highly metamorphic regions, where the syenite at present exposed would seem imadequate to explain the amount of alteration which the lias-limestones have undergone. The syenite of Strath assumes two distinct and easily recognizable forms ;—one overlying the liassic strata without markedly disrupting them ; the other violently disrupting, but not overlying them. In the former case the junction of the two rocks is horizontal, or rather parallel with the plane of stratification, and the igneous rock con- sequently conforms to the dip and strike of the limestones and shales on which it rests. In the latter case the junction is vertical or nearly so, and the igneous rock breaks through the beds without reference — either to their inclination or direction. The one class of phenomena recalls the circumstances attendant on the eruptions of the trap- family, the other reminds one of the appearances that characterize the protrusions of the granites. To the latter class belongs that great expanse of syenite of which Beinn na Cailleaich, Beinn Dhearg, and Beinn na’a Cro are the . terminal heights on the south, and which, stretching north for eight or ten miles, occupies a large area in the centre of Skye. The only part of this extended district that I have examined is the southern edge abutting against the lias from the head of Loch Slapin to the Sound of Scalpa ; hence among the glens and hill-sides there may be isolated patches of the liassic limestones and shales, although the whole area is coloured and described by Macculloch as syenite. The rock of which Beinn na Cailleaich and Beinn Dhearg are com- posed is a granular admixture of brownish felspar and grey quartz with a little hornblende. Occasionally a few scales of mica are observable, so that the rock is fully entitled to rank among the granites. The felspar readily crumbles away, giving rise to long tracks of debris— whence the brownish tint and rounded outline of the hills. The line of junction of the lias-beds and syenite can be accurately traced for some distance along the western flanks of Beinn Dhearg. In the bed of the stream which flows.down the glen between that hill and Beinn na’a Cro, there occur the limestones and shales already described, dipping away from the hills at angles (decreasing as they retire) of from 50° and 60° to 20°. They cannot be seen in contact with the syenite, but that rock can be traced down to a few yards from them, well displayed in the channel of the stream. From this spot the line of demarcation strikes up the slope of Beinn Dhearg, and, though the exact point of junction always eluded me, the two rocks, judging from the contour of the ground and from the section cut by a stream between Beinn Dhearg Mor and Beinn Dhearg Beag, must have a very nearly vertical line of separation. If there be any inclination, it is probably that of the lias-beds dippmg away from and resting against the syenite, which along some parts of the line courses the hill-sides like a ruined wall, its base thickly strewn with prostrate blocks that obscure the line of contact. Oc- casionally, as on the flanks of Beinn na Cailleaich above the milestone on the Sligachan Road, there are large masses of limestone caught up by and resting on the syenite. They do not usually appear im- 1857. | GEIKIE—SKYE. Ns bedded in the igneous rock, but rather look as if lying upon it or sunk into it. The syenite can be seen at different points protruding among these detached masses of limestone, but in no instance did I observe it enveloping and overlying them. It is, moreover, equally void of all fragments of altered limestone or shale, such as one sees caught up in many greenstones, especially along the sides of dykes; nor, save in one or two doubtful instances, did I detect it sending out veins into the adjacent rock. I may remark, in passing, that these isolated masses of limestone, as well as the great body of that rock for some distance from the syenite, are highly altered, assuming, in fact, the aspect of a crystalline marble. To this remarkable meta- morphism I shall refer more at large after the igneous rocks have been described. The class of disrupting sperite includes, in addition to the hills above described, the long irregular ridge of Beinn an Dubhaich. This eminence exhibits along its northern boundary the same abrupt vertical junction with the limestone that is shown on the sides of the opposite hills. Its southern edge is more irregular, containing many isolated masses of limestone, like those referred to on Ben na Cailleaich, while the contiguous limestone in turn contains not a few protruding knobs of syenite. In short, it is a repetition on a smaller scale of the great syenitic zone that girdles in the Strath Valley to the north. But as its western extremity has been much wasted by the waves of Loch Slapin that come surging in from the Atlantic, a section has been cut across its breadth, and its contact with the limestone is accordingly well displayed on both sides. The following cliff-sections convey an idea of the appearances here presented. The South junction of Syenite and Marble on Loch Slapin (Sketch No. 4, MS.).—Here the marble has a vertical dip, and a few yards southwards it inclines to the south-west. The syenite is a coarse granular rock, meeting the marble vertically below and bending a little over above. A syenite-vein is seen extending into the marble horizontally for 2 or 3 feet from the main mass of syenite. It looks as if it had been squeezed into an open fissure. The North junction of Syenite and Marble on Loch Slapin (P1. I fig. 7) represents the junction at Camus Smalaig. The marble here is a pure white, almost saccharoid rock. It seems to have a rude dip to the north-west, but this may be deceptive. The syenite assumes a somewhat finer texture along the line of contact, and at the lower part of the visible junction is charged with green serpen- tine, which likewise discolours the contiguous marble. Neither in this junction, nor in the corresponding one, half a mile south, does the syenite overlie the limestone. At the southern locality it falls over atop, as above stated, but the appearance is probably caused by a sudden change in the strike of the lme of demarcation, whereby, in place of its edge, its plane is presented to view. The remaining masses of syenite belong, for the most part, to the second or overlying class, of which Bemn Bhuidhe may be taken as 14 PROCEEDINGS OF THE GEOLOGICAL society. [April 22, an illustrative example. This hill forms the elevated promontory between Broadford Bay and the Sound of Scalpa, and occupies an area of not much less than a square mile. The coast-line is fringed with low flat reefs of black shale, identical with that of Pabba; and as the waves have in many places cut a steep cliff that topples over the beach, the connexion of the igneous rock with the lias-beds can be accurately studied. Nothing could present a greater contrast to the junction of the syenite and marble along the flanks of Beinn Dhearg or. Beinn an Dubhaich, than the junction of syenite and shale along this sea-margin of Bemn Bhuidhe. Here we see no great tilting of the beds, no wide-spread metamorphism, no wall-like contact of the two rocks. On the contrary, the shales dip gently under the sea, showing in many places no evidence of their proximity to a large mass of igneous rock. They are unaltered except within a foot or there- abouts from the syenite, and at the contact show a flinty porcelain- like texture. The syenite has manifestly rolled over them, catching up fragments in its progress, insinuating itself, after the manner of the traps, into cracks and fissures, and conforming exactly to all the inequalities of the stratification. Fig. 8 shows the manner in which this junction is displayed along the cliff-section. The Junction of Syenite and Shale at Beinn Bhuidhe (fig. 8).— Here the syenite is a lighter-coloured, more felspathic, and finer- grained rock than that already described. At the point of contact it is very homogeneous and compact, and hand-specimens may easily be obtained showing the two rocks fused together—an appearance nowhere observable among the disruptive syenites. The headland of Carn Nathrach must be referred to the same overlying class with Beinn Bhuidhe. Its structure is represented in fig. 4. “The overlying nature of Beinn na Charn is well displayed along its eastern boundary, where the limestones and shales dip under it, unaltered save near the point of contact; and there, it may be remarked, they are not by any means so much changed as near the disruptive masses; nor is the limestone in any instance altered into a white crystalline marble, as it is along the northern hills. The Hill of Harripool is more complex in its structure, and not less manifestly a superjacent, intrusive mass (see fig. 3). At its northern extremity it subdivides, shales and limestones being found between the separated portions. In truth, it is identical in its mode of occurrence with an ordinary greenstone, which it further resembles in the limited amount of its attendant metamorphism. Such, then, being the marked differences between these two forms of syenite, I think the inference may be legitimately drawn, even were there no other evidence, that they are not probably the products of contemporaneous eruptions. At Beinn Bhuidhe they approach within a few hundred yards of each other, and it is incon- ceivable how at the one spot the rock should have tilted up, pierced, and greatly metamorphosed the strata, after the manner of the granite 1857.] GEIKIE—SKYE. 15 of Arran ; while at the other it in no way disturbed either their dip or their texture, save along the immediate line of contact, but in- sinuated itself between their planes, and conformed to every in- equality of the floor over which it rolled. There is usually, more- over, a marked difference between the mineralogical texture and even the composition of the two rocks. The disrupting class are coarse- grained, and of a brownish-yellow tint; the overlying and intrusive are of a finer texture and lighter shade, and generally considerably more felspathic. ‘There are indeed exceptions to this rule, as in Beinn na Charn, where the rock approaches more closely to the texture of the northern hills; but the distinction is in most cases sufficiently obvious. It seems impossible, therefore, to avoid the con- clusion that the one series of outbursts must be older than the other. But there is another source of evidence, of a somewhat negative kind, which not only corroborates this inference, but indicates, as ' far as merely negative evidence can do, to which of the two classes the higher antiquity should be assigned. For, as in no observed in- stance do they intersect each other, it is obvious that they do not of themselves furnish material: for a determination of their relative ages. Yet I believe an answer to the question may be gathered from a survey of the other igneous rocks of the district ; and to these I shall now refer. Trap-dykes.—Certainly one of the most remarkable features in the geology of Strath is the almost incredible number and variety of its trap-dykes. From their greater permanence they are visible at a considerable distance, now coursing up the hill-sides like ruined walls, now plunging deep amid the heather of the glens, now dam- ming up the channel of some mountain-torrent that pours over them its white cascades. They preserve a general north-westerly strike, but frequently intersect each other or unite, being seldom continuous for long distances. These features are well displayed along the eastern shore of Loch Slapin, where for upwards of two miles the waves have cut a vertical line of cliff. Along this cliff, and on the beach below, the dykes may be seen running parallel, uniting, again bifurcating, interlacing in labyrinthine confusion, now thickening, now thinning, terminating abruptly and commencing again, entangling masses of limestone, and sending out minor veins; at one time roll- ing in an undulating course, wholly irrespective of the dip or strike of the beds, at another running along the line of the natural joints ; now seeming to conform to the planes of bedding, now cutting through them like walls of masonry, and at length ending off in a point sometimes well nigh as fine as that of a pen. In truth there are few localities where the nature of trap-dykes could be better studied than along this coast-line, for there is both an admirable ground-plan of them along the beach, and, for a considerable part of the shore, they are exposed in section along the cliffs. (PI. I. fig. 9, and MS. Sketches Nos. 8 and 9, illustrate the trap-dykes on the shore of Loch Slapin.) The eastern margin of the island also exhibits the trap-dykes in 16 PROCEEDINGS OF THE GEOLOGICAL society. [April 22, abundance ; but they are there more regular, and generally keep parallel to each other in a north-west direction. On Pabba Island they are also numerous, running along the line of the natural joints, with the usual north-westerly strike. Here they show very unequal degrees of permanence, in some cases crumbling away as rapidly, or even more so, than the surrounding shale; in others jutting up like walls. Of the latter kind one very noticeable example occurs on the northern shore of the island. A dyke, from 3 to 4 feet thick, and, next the cliff-line, about 30 feet high, crosses the beach and runs out to sea (MS. Sketch No. 11). The shale has been washed away on all sides of it, and it blocks up the walk along the beach lke a wall of smoothly built ma- sonry. ‘These Pabba dykes are of interest in so far as they enable us to estimate the extent to which trap-rocks have altered the strata of the district ; for in Strath there is so much metamorphism and so many protrusions of syenite, that one is apt to miscalculate the amount of influence of the different igneous eruptions. Pabba, how- ever, is nearly two miles distant from the nearest point of syenite, so that this rock could not have had any effect upon the shales of the island. There is thus no conflicting agency to mar or heighten that of the trap-dykes ; and, as in Pabba they fully equal in number those in the most metamorphic regions of Strath, it follows that, if, either wholly or in part, they have produced the metamorphism of Strath, they must have caused a corresponding amount of alteration in Pabba ; but in that island there is no metamorphism beyond the mere hard- ening of the shales in immediate contact with the trap. At the di- stance of 2 feet they are generally as soft and fissile as when furthest removed from dykes. It is evident therefore that the remarkable metamorphism I have yet to describe cannot have been produced by the trap-dykes, startling as their number may seem. Their effect is limited to a few inches from their edges, and even this slight altera- tion becomes undiscernible in the interior, where it is lost in a far more extended and complete metamorphism. The trap-dykes, like the syenites, are divisible into two well-marked classes, differing from each other in mineralogical texture and in age. The one group comprises nearly all the dykes of the district, and is formed of a dark-grey or bluish-black basalt*, not columnar, but much jointed. The rock is exceedingly hard, and weathers with a greenish-brown crust. The dykes of the other class are not nume- rous, and consist of a dark crystalline augitic greenstone*, which sometimes approaches the basalt in texture. The annexed ground-plan (fig. 10) of the neighbourhood of the old Manse at Kilchrist shows the relation of these two classes to * These terms are here used, as they have, I think, always been in Scottish mi- neralogy, to signify two rocks differing from each other, not in composition, but in texture ; Jasalt being a compact black mixture of augite and felspar without visi- ble crystals, greenstone a lighter-coloured mixture of the same minerals, the cry- stals being easily recognizable. When hornblende replaces the augite, it is called a hornblendic greenstone. In Scotland, where so large a proportion of the traps are augitic, this distinction is a very useful one. 1857.] GEIKIE—SKYE. Ly; each other. The greenstone-dyke extends from the road at Loch Kilchrist in a south-easterly direction for fully half-a-mile, cutting through marble and syenite. Along both edges of the syenite- belt there are numerous smaller basalt-veins cut off abruptly, toge- ther with the marble which they intersect. Similar appearances are visible on the south front of Beinn na Cailleaich, where all the basalt-dykes of the Sithean valley are truncated by the syenite, while a large one of greenstone, traversing perpendicularly the bare slope of the mountain, forms a prominent dark scar. ‘These facts seem to me to show that the trap-dykes are of two ages; those of basalt beimg older than the disruptive syenites, those of greenstone later. The intrusive syenites are not traversed by basalt-veins, but they are intimately connected with the greenstones ; and this relation, when examined, throws important light upon the respective ages of the different igneous rocks of the district. Reference has been already made to the headland of Carn Nath- rach, that divides Lochs Slapin and Eishort (fig. 4). It is formed by a great sheet of augitic greenstone, surmounted by an irregular bed of fine-grained felspathic syenite. The greenstone, which re- sembles in texture and mode of occurrence the other rocks of the same kind in the district, forms a bed of considerable regularity, and is connected at its southern edge with a thick dyke that cuts verti- cally the nearly horizontal shales of Suishnish. The syenite, owing to its liability to decay, has a somewhat irregular surface; but it undoubtedly forms a bed, and is everywhere found resting on the greenstone. At the large loch on the top of the headland it has carried up a considerable fragment of the calcareous sandstone of Suishnish Point, and there can be no question that both greenstone and syenite are alike intrusive. Along the eastern base of Beinn na Charn there are also at several points indications of a substratum of greenstone. The same fact is observable in the Hill of Harripool: that emimence forms a long ridge extending southwards from the village of Harripool and merging into the northern projection of Beinn na Charn. At its seaward end it consists of limestones and shales belonging to the Breakish-series ; and, about two miles south from the sea, beds of syenite, probably manaieations of the main mass east of the Black Lochs, are found intercalated with the liassic strata: at several points the syenite has a distinct capping of greenstone, perhaps the result of a difference in cooling, but more probably the product of a different eruption. The connexion of these intrusive syenites with the greenstones is such as to leave no doubt that they are both later than the dis- ruptive masses ; that in truth they must be regarded as the latest of the igneous products of Strath. Thus the greenstones, whether regarded as merely the result of a difference in cooling, or as the _ products of distinct eruptions, confirm the conclusion that the syenites are of two ages, and indicate with tolerable distinctness to - which class the higher antiquity should be assigned. It may be well, ere passing on, briefly to sum up the evidence here VOL. XIV.—PART I. c 18 PROCEEDINGS OF THE GEOLOGICAL sociETy. [Apr. 22, collected as to the dates of the igneous eruptions of Strath. Ist, they are all posterior to the Middle Lias, being intrusive and not con- temporaneous ; 2ndly, the first period of igneous action gave rise to a great profusion of trap-dykes, which intersected every part of the district ; they did not, however, produce any marked alteration of the general stratification and texture of the rocks, but rather con- formed themselves to the natural jomts of the beds, and hence ac- quired a prevailing strike to north-west; 3rdly, subsequently vast tracts of syenite tilted up the liassic strata, in a manner analogous to that of the Arran granites, and produced in them an extensive and com- plete metamorphism ; 4thly, the last period of igneous action was characterized by the outburst of great hills of fine-grained syenite, that intruded itself among the beds without either tilting them or producing any considerable amount of alteration upon them ; at the same period sheets of greenstone were occasionally thrust among the syenites and limestones, or broke through them as massive dykes*. Metamorphism.— The general arrangement and effects of the igneous rocks having been pointed out, I shall proceed to describe the metamorphism so often alluded to. The metamorphic district, as may be conjectured, lies among the disruptive syenites. Its north- western limit is formed by the great syenitic chain of Beinn Dhearg and Beinn na Cailleaich ; the hillward slope of Bein Shuardail and the hollow of Glen Kilbride bound it on the south-east ; the shore of Loch Slapin, from Beinn na’a Cro to the mouth of Glen Kilbride, forms its south-western termination; while to the north-east it ap- proaches Beinn Bhuidhe and Broadford. Within this area the bedded limestones of Broadford Bay are altered into a crystalline mass; stratification is usually obliterated, along with all trace of fossils, and what was before’a dull blue limestone assumes all the sparkle and varied tints of a primary marble, mottled sometimes like that of Balahulish, or pure like that of Carrara. The action of atmospheric agents upon this rock has caused it to weather in a very singular manner. The eminences which it forms, in not a few instances, look as if a shower of oblong grey blocks had been shot into their soft peaty surfaces. In some places the marble assumes a finely cavernous exterior, pitted all over, like a sandy beach after rain. At other times the blocks are smooth as tomb- stones, and stand out in bold relief from the heath and furze that surround their base. No moss or lichen can cling to them, nor does the vegetation of the soil cluster up their sides, as it never fails to do round the mouldering dykes, so that the marble-hillocks arrest the eye at once, and can be distinguished at a considerable distance. This manner of weathering is not, however, peculiar to the marble. It may be seen, though in a much less marked manner, along the outcrop of unaltered limestone south of Sculamus. But the most * The geological era of these events has still to be fixed. Professor Edward Forbes was of opinion that the trap-hills of the north-east of the island were of Middle Oolite age, but admitted that the district would require a more extended investigation before the point could be made out with certainty. See Quart. Journ. Geol. Soc. vol. vii. p. 109. 1857. | GEIKIE—SKYE. 19 remarkable example of weathering is probably that on the beach south of Camus Smalaig, where, to the action of the atmosphere, there has been added that of the waves. The rock is there of a leaden-blue colour, and its surface bristles thickly with sharp rough irregular fragments, having a greenish hue and adhering to the marble often by the merest point. These small roughnesses are so angular as to wound the hand when it is passed even gently across them, and they render walking dangerous alike to boots and skin. I can compare them to nothing but what we might conceive would be the appearance presented by a shower of moist tea-leaves that had been thrown athwart a freezing pond and become hard and fixed in the ice. The texture and colour of the marble vary in different parts of the district. The whitest varieties are to be seen at the Kilchrist quarries, and in the vicinity of Kilbride. In each of these localities there is a large mass of syenite close at hand. Various shades of grey occur, in some instances (as on the shore south of Camus Sma- laig), in contact with the syenite,—the marble assuming a crystalline or saccharoid texture. Green streaks of serpentine mottle the rock where it is intersected by trap-dykes, and also, at Camus Smalaig, where it is cut through by syenite. Specimens may also be obtained prettily veined with blue and purple (rarely with red) even in the immediate vicinity of the purest crystalline varieties, as at the Kil- christ quarries. As the marble recedes from the syenite it darkens in colour, loses its metamorphic aspect, and gradually passes into an ordinary limestone. On the exposed marble-cliffs that frmge Loch Slapin, a little way north of Glen Kilbride, 1 have found what appears to be the frag- ment of a Pentacrinite. With this exception I have not succeeded in detecting in the altered limestone any trace of organic remains. There are, however, a number of rough nodular accretions of cherty carbonate of lime, of great hardness, that protrude, sometimes in considerable numbers, from the smooth surface of the marble. These may represent some of the organisms seen along the eastern shores, and I have sometimes fancied that my eye could detect what bore a remote resemblance to a Gryphite. If such irregular nodules do actually represent Ammonites, Gryphee, &c., these organisms must have undergone no little distortion and obliteration—Pentacrinite, Ammonite, and Pecten being jumbled together into rugged lumps of cherty limestone. The passage of the metamorphic into the unaltered limestone is a point of considerable interest, and may be studied to advantage on the shore of Loch Slapin at the mouth of Glen Kilbride (MS. Sketch No. 13). There the altered limestone is seen abutting against the syenite of Beinn an Dubhaich. As it approaches the sea it hecomes dark, compact, and dull in grain, with streaks of white, but devoid of fossils. Then occur seams of lighter-coloured limestone and hard shale with Gryphee, succeeded by a dark blue close-grained lime- stone with : Den ee oe Bennnalao. ——_ ech cH y piciass CG ee ote : Zi Sandstone: he: Carbonac Probable ~, ig 1857. | GEIKIE—SKYE. 23 later secondary or earlier tertiary epochs ; and I am much inclined to think that some of the later felspathic ashes and basalts which dot the mainland, together perhaps with not a few of the great parallel faults and dykes, may belong to this volcanic era. A thorough examination of these islands cannot fail, therefore, to elicit much truth as to some obscure points in the physical history of Scotland. Of the geology of Strath, however, there is one branch that seems to be complete in itself, whereon we can expect little light to be thrown from other districts. I allude to what is certainly its most characteristic feature—the metamorphism of the lias- ‘limestone. Strath may be surpassed by other localities among the Western Islands in the preservation and number of its organic re- mains ; but I despair of meeting with a more striking example of metamorphism. The igneous rocks of this parish, with their va- rieties of kind and form, and their effects on the surrounding strata, impart to it an interest all its own. Notes to the Map and Sections: Plate I. The accompanying Map has been taken partly from that of Dr. Macculloch, partly from the Charts of the Admiralty Survey, of which a tracing was kindly sent me by Captain Wood, R.N., Kyle, and partly from bearings with the azimuth-compass. It is far from being accurate; yet the errors are not probably so material as to affect to any considerable extent the general bearings of the geolo- gical lines. With regard to the geological part of the Map, there is but one re- mark needed here. The irregular bulging hill of Creag an fithick, south of Beinn Dhearg, is coloured (in the original) like the syenite, but of a fainter tint. The rock has puzzled me nota little. Sometimes it seemed like an earthy greenstone, sometimes like a felspathic por- phyry ; at some points it assumed many of the characteristics of an ash or tufa, with fragments of altered shale ; at others it approached in texture and general appearance the syenite of the contiguous hills. It is likely that there may be several kinds of igneous rock in the series of lumpy knolls from Kilbride north-eastward, but I was unable to separate them out, and I have coloured the whole as one mass. It is by no means easy to ascertain to what age these rocks belong; they seem to have come up in the rent formed by the dis- ruptive syenite of Beinn Dhearg, and to have flowed over atop. But it would be rash at present to hazard any conjecture regarding them. [The lines of sections, with roman numerals, on the Map, fig. 1, refer to the MS. Sections. ] The Sections are drawn on the scale of 1 inch to the mile, except with regard to the height above the sea-level, which in most cases has had to be exaggerated. [In fig. 8 the syenite has been lessened. in height.] The upper horizontal line in each of the Sections marks the sea-level, and the space between that line and the lower one re- presents a thousand feet of vertical depth. S77 oe Quart. Joonn Geon Soe Vou. XIVPL |, | ‘ Fig , Figs . Section through northern end ABcitty Sharda. GEOLOGICAL MAP of the { Scalpa House LIASSIC DISTRICT OF STRATH, i (Greenstone) Be pane we Gene acai 6. Breecia. c. Shales &L: ‘ from Brealish, wlLiexsay, d.Limestmes ot Sc : Ws would haveragpeared adit beavcontinuous, | Se = 5 Z Bsa (ote? E35 Miaale bias. EEEESD Rad Sandown: ES iipersthene. Eon De Syentte,. eee —Lines of fiat. Greenstone Basalt. ISLE of SKYE, é 7 Scale of Miles 5 a Fig. 6. Section between Beinnna. Charm and Fill of "Harripool . Tech Tonachan MW Li D | 7, ZL aa Red Sandstone, bBreecia.c.Timestones & Shales ¢ inFig.d, a Limestones &Shales; di Limestone of Beinn Shuardil approaching themeta morphicregion. f: Fault. Fig 7. North junction of SyateX Merble, Belin an Dulhaich. : SSS a. Cyuirlbben nperBlD. 6. Syante of Barnan Dubhaich. c Greenstone a. Syenite, b. Marble with arudedip to N \W, dyke, d.d. Basalt dykes. 2, i Fig3, Seetion from Bey na Cailleaich through Beinn Shuardail and Till of HarripooL ke Fig.2. Sechor from Scakpa through attire & Pabhba to the Road. beoween Brealish &Lussay. ; Cailleat B eaich. . Ry SES ser Slve s ; Beinn Shnardail HillofHarripool., Scalpa %% Guilkmon ObeBreakish Road Se Gen Shama, Tad of - SES Ke Broadtird Bay the Sea { Bo } = ! hades = == ose SY SS Se 5 B Sie EE ke Zz Tevel off Se Sms — a ae oy Z, bi Pe tingy, hqucrtz rock, rreuch jointed & cleerved, Z eae FAS Tee : wien ke, eg a ee te weet Syentte Indiirated Red, Sandstone and aS E and the Shall. % ie as Ae WE (Lig ayer rate bed, tele ete mm Sg oa thon | Fig A: Cliff— Section along the East side of Lock Slapin & the North side of Loc h Bishort. Blabhein : va tac erg £5 NS. : a HL —— ypevsthene Leva of Frobable Sandstone 24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 22, Notes on the Fosstus collected by Mr. Grtxie from the Lias of the Isuxs of Passa, Scaupa, and Sxye. By Tuomas Wraieut, M.D., F.R.S.E. . Ar the request of my friend Professor Ramsay I made an exami- nation of the fossils collected last summer by Mr. Geikie from the Lias of Pabba, Scalpa, and Strath ; first, for the purpose of deter- mining the species to which they belonged ; and, secondly, to assign the subdivisions of the formation which they characterized. Previous to laying before the Geological Society my notes on the different species contained in this interesting collection, it is neces- sary that I should premise a few remarks on the classification of the Lias, in order that I may rigorously define the portion of the for-— mation I include in the term middle ; so that the true stratigraphical position of the beds which yielded these organisms may be fixed with certainty. English authors in general divide the Lias into Upper Lias, Marl- stone, and Lower Lias ; but these subdivisions require additions and modifications in order to place our liassic beds in correlation with those of French and German authors. For on the Upper Lias clays are superimposed beds, which, previously to the publication of my memoir on the “Upper Lias Sands’’*, were grouped with the Inferior Oolite; and with the Lower Lias are placed several beds which, with the Marlstone, constitute the Middle Lias of the Con- tinental authors. Taking the Lias-beds as they occur in Gloucestershire, in descend- ing order, and naming each bed by the species of Ammonite which characterizes it, we find the series tabulated at p. 25, which is nearly the equivalent of the Lias-beds of Germany so well described by Dr. Oppel in his valuable work now passing through the press, ‘‘ Die Jura-Formation, &c.’’ In the following Table (p. 25) a comparative view is exhibited of the subdivisions of the Lias, according to Prof. Quenstedt, Dr. Oppel, the late A. d’Orbigny, and Sir Roderick Mur- chison. The following list contains the most characteristic species of Mol- lusca and Radiata of the Middle Lias of Gloucestershire, and is given for the purpose of indicating the age of the Pabba-shales, by a com- parison of the respective fossils. Belemnites paxillosus, Schloth. Ammonites Henleyi, Sow. elongatus, Miller. ibex, Quenst. (Boblayei, d’ Orb.) clavatus, Schloth. —— bipunctatus, Roem. (Valdani,d’ 0.) compressus, Stahl. Loscombi, Sow. longissimus, Miller. —— capricornus, Schloth. (maculatus, breviformis, Ziet. ¥: GB.) Nautilus intermedius, Sow. Ammonites spinatus, Brug. —— margaritatus, Monéf. Normanianus, d’ Ord. Taylori, Sow. — heterophyllus (amaltheus), Quenst. Centaurus, d’ Ord. —— fimbriatus, Sow. Chemnitzia undulata, d’ Ord. [Continued at p. 26.} Jamesoni, Sow. Daveei, Sow. Maugenesti, d’ Orb. * Quarterly Journal of the Geological Society, vol. xii. p. 292. Lier) N WRIGHT—LIAS FOSSILS FROM SKYE. 1857.] a *poq-ou0g eee eee ie Bodo LO Gt eocecoessoeee Pi UOTE Ra ea aa OSH) 0 TO EE LLOKS | eertooeseseoren StrT sop IOINETIOA ——$[—$—$S$—— Heetieerieseserreses DQq-qoasuy ee eee *“Avssn'yT POO rer eoeserteecereecssseseseeereee a et ee ee DOC ESIC MOE a ses ae: qj9qQ-Ssnyern uy ay]0UOY J, 77) puvoy "0 sery eral eR RRUONE ave 09] ae Gang ala RE ae OM NCE rapt apeuptiy screen gee “9U0JSOWIT vosessnes ch pa er sae coneesseerersreangg-snjOUsAXxO he IU0OY JINIUAN, J, ‘d Ser'y PUB SOTBYS SPL] LOMOT | J........++4+++ paq-snyejsoouey rreeseeseses qn gg-snqeysOoLiey | POeerearteeeeeeretene poq-tuosowmer weeeoeeseeereees p49 -TUOSOWI aye "eqqed POO e eevee seses Peover sheen sseuey Pee eerecccees esses ersece poq-x9q] ‘SVIT aTaaryy ee ye ea eal JAB LIUSIIDUSLULNNT SBlT [ Ceoeeeoeaesenesereeere poq-laoaeqg “WaIsDUT ooe ee Tava RE 5 eeeveesssene fa) S042 4TIV SIC . Md pa tS Selle otis JJOQ-Ssnyeqse IVT eee ° -edjvog ouoIseIN | fae ee oe nausstlinutde teererereeeereres gaggasngqvatdg \ aUOY;UadYZJVMp *Q SBI] ‘sery Jaddg |e" paq-stunurmi0g| ‘sviry adda |*77°°°*""**4y30q-aadtMoUOpIsog|*** vafazyasuaquopisod *9 Sev] "auT[0O IOWMIJU] jo aseqg eoceeeorevneer seers peq-sisuain "Uata 400 J, eeoeceeeseeeseserece 4yoq-sisuaine reveeeess 19H LIUSISUIANG 5) Ser'y ‘TANS GDC EE IGG PULLED “hubrg4O addQ “ppajsuang) ‘GUIHSUTLSTONOTH ‘AUIHSUTLSAONO1D ‘IONVUT ‘DUTANALLATA "VIEVMS i a a ‘ahyy pun ‘auyssagsaano) ) ‘hunusayy ‘aounig ue spag sovy ay} f0 U0IQDIALLOD ay? Buamoys 2790], F 26 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Continued from p. 24.] Trochus imbricatus, Sow. Pleurotomaria expansa, Sow. concava, Wright, n. sp. Anglica, Sow. Rotella compressa, Sow. polita, Bronn. Dentalium giganteum, Phil. Gryphea-cymbium, Lamhk. gigantea, Sow. Pholadomya ambigua, Sow. decorata, Hartm. Pleuromya unioides, Roemer. Panopeza elongata, Roemer. Mytilus (Cypricardia ?) hippocampus, Young & Bird. cuneatus, Sow. Cypricardia cucullata, Goldf. Cardinia attenuata, Stutchd. Cardium acutangulum, PAil. truncatum, Sow. Unicardium cardioides, Phil. (lanthe, d’ Orb.) Arca Buckmanni, Richard. truncata, Buckm. Pinna folium, Young & Bird. Lima Hermanni, Ziet. Limea acuticosta, Goldf. Avicula cygnipes, Young & Bird. inzquivalvis, Sow. longiaxis, Buckm. Inoceramus ventricosus, Sow. Pecten xquivalvis, Sow. — sublevis, Phil. [Apr. 22, Pecten corneus, Goldf. (non Sow.) velatus, Goldf. Plicatula spinosa, Sow. Gervillia levis, Buckm. Goniomya, 2 sp. Homomya, sp. Gresslya, 3 sp. Astarte, 2 sp. Leda complanata, Goldf. , ni. sp. allied to L. lachryma, Qu. Terebratula cornuta, Sow. — Edwardsi, Davids. —— resupinata, Sow. —— punctata, Sow. —— subpunctata, Davids. —— numismalis, Lamk. —— subovoides, Roemer. Spirifer rostratus, Schloth. Rhynchonella variabilis, Schloth. rimosa, V. Buch. —— tetrahedra, Sow. — acuta, Sow. Cidaris Edwardsii, Wright. Hemipedina Bowerbankii, Wright. Acrosalenia crinifera, Quenst. Ophioderma Gaveyi, Wright. Tropidaster pectinatus, Forbes. Uraster Gaveyi, Forbes. Pentacrinus robustus, Wright. basaltiformis, Miller. — punctiferus, Quenst. gracilis, Charlesw. In the above list I have only enumerated the most characteristic species, as there are many undescribed forms of Gasteropoda and Conchifera in the Middle Lias of Gloucestershire which cannot be cited in this paper. List of the Inassie Fossils collected by Mr. Geikie in Skye. Belemnites elongatus. Pabba. Lima Hermanni. Pabba. paxillosus. Pabba. Limea acuticosta. Pabba. breviformis. Pabba. Inoceramus ventricosus. Pabba. Ammonites Jamesoni. Pabba. Pecten zquivalvis. Pabba and Scalpa. —— brevispina. Pabba. ySDs Davei. Pabba. Plicatula spinosa. Pabba. Trochus imbricatus. Pabba. Gervillia Maccullochii, n.s. Pabba. Pholadomya ambigua. Pabba. Gryphza cymbium. Pabba. Pleuromya Scottica, n.s. Pabba. obliquata. Pabba. unioides. Pabba. Ostrzea arietis. Lussay. Cardinia concinna. Lussay. , sp. Lussay. Avicula, sp. Scalpa. Rhynchonella tetrahedra. Pabba. Unicardium cardioides. Pabba. Pentacrinus robustus, n.s. Pabba. Pinna folium. Pabba. gracilis. Pabba. Mytilus cuneatus. Pabba. Isastreea Murchisoni, n.s. Lussay. Lima gigantea. Pabba. to “I 1857.| WRIGHT—LIAS FOSSILS FROM SKYE. BELEMNITES ELONGATUS, Miller, 1823. Belemnites elongatus, Miller, Trans. Geol. Soc. 2nd Series, vol. ii. t. 7. f. 6-8 ; Sowerby, Mineral Conchology, t. 590. f. 1; De Blain- ville, Mémoire sur les Bélemnites, pl. 4. f. 6. Belemnites pazillosus, numismalis, Quenstedt, 1848, Cephalopoda, tego tl. 2), 22. This species is found in the Middle Lias at Charmouth from the bed with Ammonites Jamesoni, Sow., to that with Ammonites Daveei, Sow. It was collected in Crick Tunnel, near Daventry, and is also found in the lower beds of the Middle Lias, with Terebratula numis- malis, Lamk., at Cheltenham. Two specimens have been collected from the Pabba shales; although only 6 inches in length, they are good type-forms of this species. In France it is found in the Middle Lias in twelve different Departments, and in Wurtemberg it forms a characteristic fossil of the Lias y. of Quenstedt, and “der mittlere Lias”’ of Dr. Oppel. BELEMNITES PAXILLOsus, Schlotheim, 1820. Belemnites paxillosus, Schlotheim, die Petrefactenkunde, p. 46. Bruguierianus, d Orbigny, Pal. Frang. Terrains Jurassiques, pl 7. f. 1-5. paxillosus amalther, Quenstedt, Cephalopoda, t. 24. f. 4. Three specimens of this species were collected from the Middle Lias shales of Pabba, but the distinct horizon in which they occur has not been noted. In Gloucestershire it is found in the Marl- stone with Ammonites margaritatus, Montf., and in the same rock at South Petherton with that Ammonite. In France it has been collected from the same horizon; and in Southern Germany, Dr. Oppel says it is one of the most widely distributed species of the Margaritatus-bed. BELEMNITES BREVIFORMIS, Zieten, 1831. Belemnites breviformis, Zieten, die Versteinerungen Wiirttem- betes, t. 21. £7. breviformis amalthei, Quenstedt, Cephalopoda, t. 24. f. 21- 23, 1848. 7 There is only one specimen of this Belemnite im the collection. This species is found in the Marlstone of Gloucestershire, and in the Lias 6. of Quenstedt, with Ammonites spinatus, Brug. AMMONITES JAMESONI, Sow., 1827. Ammonites Jamesoni, Sowerby, Mineral Conchology, pl. 555. f. 1. Bronni, Romer, die Versteinerungen des Norddeutschen Ooliten-Gebirges, t. 12. f. 8, 1836. Regnardi, V Orbigny, Paléont. Francaise, Ter. Juras. t. 72. Jamesoni, angustus, Quenstedt, Cephalopoda, t. 4. f. 8, 1845. Jamesoni, latus, Quenstedt, Cephalopoda, t. 4. f. 1: Jamesoni, Quenstedt, der Jura, t. 15. f. 1-5 ; Oppel, Mittl. Lias Schwabens, p. 38 ; die Juraformation, p. 159. 28 PROCEEDINGS OF THE GEOLOGICAL society. [Apr. 22, The original type of this species was collected by Sir Roderick Murchison in the Isle of Mull. There are several fragments in the collection, one showing the inner and larger whorls, 7m situ, from which we learn that up to the third whorl the ribs are fine and nu- merous, about 56 in a whorl; in the fourth whorl they are further apart ; in the fifth whorl they become more prominent, are directed obliquely forwards, and as they pass over the dorsal surface they form an arch, the convexity of which is towards the mouth of the shell. This appears to be the most abundant species in the Pabba-shales, as there are several specimens of different ages in the collection ; the largest specimen measures 6 inches in diameter. Compared with Sowerby’s figure (Min. Conch. pl. 555. f. 1), the lateral ribs in the specimens from Pabba are less flexed, the second whorl is dispro- portionately small, and the ribs are closer together. Ammonites Jamesoni, Sow., is found in the Middle Lias near Charmouth, and in the grey shaly clays of the same zone at Robin Hood’s Bay, Yorkshire coast ; I have obtained only three specimens in the lower beds of the Middle Lias near Cheltenham. This Ammonite is found in the lower part of the Middle Lias of Swabia, in many localities, as at Pliensbach by Boll, at Sondel- fingen, Hechingen, Balingen, &c. The German specimens are mostly fragments. In France it is found in the same region of the Middle Lias at Saint Amand (Cher) and Evrecy (Calvados). As the rib- bing of the shell varies at different periods of its growth, such varieties have been supposed to constitute distinct species. The Ammonites Regnardi, VOrb., and the Ammonites Bronni, Roemer, are but dif- ferent states of this very characteristic Ammonite from the lower region of the Middle Lias. AMMONITES BREVISPINA, Sowerby, 1827. Ammonites brevispina, Sowerby, Mineral Conchology, t. 556. f. 2. natrix, Zieten, die Verstein. Wurttemb. t. 4. f. 5, 1830. natrix, rotundatus, Quenstedt, Cephalopoda, t. 4. f. 17, 1845. Sowerby’s text and the numbers of pl. 556 do not agree; this mistake will mislead the reader, unless he is acquainted with the two Ammonites figured in that plate. Figure 1 represents 4mm. brevi- spina, Sow., and Figure 2, dmm. laticostatus, Sow., as stated in the description. On comparing the fragment of this species from the Pabba-shales with 4. natriz, Zieten, from the Middle Lias of Balin- gen (Swabia), I find them to be identical ; the spines near the inner edge of the whorl are nearly obsolete, those towards the back are short well-developed processes, and are well characterized by the specific name brevispina. The type-specimen of this Ammonite was collected at Pabba by Sir Roderick Murchison, with which the fragment before me entirely agrees. It is found likewise in the lower shales (Middle Lias) of Robin Hood’s Bay with dmm. Jamesoni, Sow. 1857.] WRIGHT—LIAS FOSSILS FROM SKYE. 29 Ammonites Davai, Sowerby, 1822. Ammonites Daveei, Sowerby, Mineral Conchology, t. 350 ; d’Orb. Paléontol. Francaise, Terr. Jurassiques, t. 81, 1844; Quenstedt, Cephalopoda, t. 5. f. 6. The only specimen of this Ammonite contained in the collection has the shell tolerably well preserved ; the fine irregular layers of growth which impart a wrinkled appearance to the whorls, with the few distinct tubercles, from ten to twelve in a whorl, placed on its outer border, serve to distinguish this species from dmm. armatus, Sow., and Amm. subarmatus, Sow., with which it might be con- founded. Ammonites Daveei, Sow., is found at Charmouth in the upper region of the Middle Lias; in Gloucestershire I have a specimen collected from a bank of clay above the zone of Ammonites ibez, Quenst. (4. Boblayei, d Orb.) and Amm. bipunctatus, Roem. (4. Valdani, @Orb.). In Swabia Dr. Oppel found it in this horizon near Boll, at Fiizen andat Randen. D’Orbigny gives many localities for this species in France, where it is proper to the Middle Lias, “bien au-dessous de la Gryphea cymbium.”’ TROCHUS IMBRICATUS, Sowerby, 1819. Trochus imbricatus, Sow. Mineral Conchology, t. 272. f. 3, 4. The only examples of this species are two interior moulds, from which the shell is entirely denuded ; the whorls are rather more convex than the type-forms of this fossil from the Middle Lias Clays near Cheltenham, from whence Sowerby’s specimens were obtained. PHOLADOMYA AMBIGUA, Sowerby, 1819. Pholadomya ambigua, Sowerby, Mineral Conchology, t. 227. The two specimens of this shell are small, about 2 inches in length ; but they agree in the form of the mould, the number of the ribs, and the style of the lines of growth, with true forms of this species of the same size found in the Middle Lias, near Cheltenham, in com- pany with Ammonites Henleyi, Sow., Pleurotomaria expansa, Sow., Pecten equivalvis, Sow., and Modiola scalprum, Sow. PxLevromya Scortica, Wright, nov. sp. Shell oval, umbos large, prominent, and forming conspicuous re- curved projections, the points of which extend to the anterior border ; sides much inflated below the umbos, and marked with numerous longitudinal elevations and depressions; the moulds are so much distorted that neither their number nor the true form of the shell can be ascertained. This species resembles Pl. uniordes, Roem., in the longitudinal ele- vations on the shell, but differs from it in having the curvature of the umbos level with the anterior border, instead of at the anterior third, as in Pl. unioides. The forward position of the umbos like- wise distinguishes it from Pl. rostrata, Agass. : 30 PROCEEDINGS OF THE GEOLOGICAL SOcIETY. [Apr. 22, PLEUROMYA UNIOIDES, Roemer, 1836. Venus unioides, Roemer, Norddeutschen Oolit. t. 8. f. 6. p. 109. Pleuromya unioides, Agassiz, Etudes Critiques, Pleuromya, p. 236. t. 27. f. 9-13. The single specimen before me from the Pabba-shales so closely resembles the same species from the Capricornus-bed of the Middle Lias, and likewise from the Margaritatus-bed of the Marlstone, that there can be no doubt of their identity ; it appears to be rare at Pabba. AVICULA, sp. In a fragment from Scalpa, with a portion of Pecten equivalvis, there is the interior of one valve of an Avicula; but the species is indeterminable. CaRDINIA CONCINNA, Sowerby, 1819. Unio concinnus, Sowerby, Mineral Couchology, t. 223. Cardinia concinna, Agassiz, Etudes Critiques, Myes, t. 12. f. 21,22. Six valves of this shell lie on a thin slab of greenish sandstone, which came from beneath the coral-bed at Lussay; the Cardimie are mostly in the form of moulds, and on the under side of the slab are similar impressions of the same shells. The specimens from Lussay agree much better with Agassiz’s than with Sowerby’s figure. In Germany this species characterizes the lower beds of the Lower Lias, in Wurtemberg. In France it is found in the same strata in the Departments of Moselle and Cote d’Or. Unicarpium carpiorpeEs, Phillips, 1839. Corbula cardioides, Phillips, Geology of Yorkshire, t. 14. f. 12. The single valve of this species from the Pabba-shales agrees with the type-forms of this shell found in such abundance in the shales of the Middle Lias, beneath the Marlstone in Gloucestershire, and in the same horizon in Robin Hood’s Bay, Yorkshire. PINNA FOLIUM, Young and Bird, 1822. Pinna folium, Young and Bird, Geological Survey of the York- shire Coast, t. 10. f. 6. Pinna inflata, Chapuis et Dewalque, Fossiles Ter. Second. Luxem- bourg, t. 30. f. 1. Several specimens of this species, from the Pabba-shales, are in the collection, which entirely agree with the Gloucestershire examples of the same shell, and with those from Robin Hood’s Bay, Yorkshire. Myti.us cunEatTUvs, Sowerby, 1821. Modiola cuneata, Sowerby, Mineral Conchology, t. 248. f. 2. Modiola scalprum, Phillips, Geology of Yorkshire, t. 14. f. 2. The three specimens of this Mussel are from the Pabba-shales ; they are small imperfect examples of the species, but identical with 1857. | WRIGHT—LIAS FOSSILS FROM SKYE. 31 the Gloucestershire forms of the same size found in the shales of the Middle Lias, and in the Marlstone of that county. LIMA GIGANTEA, Sowerby, 1814. Plagiostoma giganteum, Sow. Mineral Conchology, t.77 ; Zieten, die Versteinerungen Wiirttembergs, t. 51. f. 1, 1830. Inma gigantea, Goldfuss, Petrefact. Germaniz, t. 101. f. 1, 1834. The specimen from Pabba agrees so well with the small smooth forms of this species found in the Lower Lias of Gloucestershire and Lyme Regis, that I have referred it to L. gigantea. As I believe that L. gigantea does not occur in the Middle Lias, I think it pro- bable that this specimen was obtained from some of the lower beds. Lima Hermannyt, Zieten, 1838. Lima Hermanni, Zieten, die Versten. Wirttemb. t. 51. f. 2. The specimen is a fragment, but the large ear, the flattened shell, the waved ribs with wide interspaces, and the distinct concentric layers of growth are sufficient to distinguish this fragment from its congeners. It was collected from the Pabba-shales. Limea acutTicosta, Goldfuss, 1836. Iimea acuticosta, Goldfuss, Petrefact. Germanie, t. 107. f. 8. Plagiostome. acuticosta, Quenstedt, der Jura, t. 18. f. 22-25. This species is catalogued in Murchison’s Geology of Cheltenham as Plagiostoma duplicatum ; it is found in the Marlstone and Middle Lias shales of Gloucestershire. It is collected likewise in the same zone at Robin Hood’s Bay, Yorkshire. In France it is found at Fontaine-Etoup-four, Calvados, in the Middle Lias. It is abundant in the Middle Lias of Swabia. The two characteristic specimens of this shell before me, contained in fossiliferous nodules, were collected from the Pabba-shales. INOCERAMUS VENTRICOSUS, Sowerby, 1823. Crenatula ventricosa, Sowerby, Mineral Conchology, t. 443. Inoceramus nobilis, Minster in Goldfuss, Petr. Germaniez, t. 109. f. 4. This species is very abundant in the Middle Lias near Cheltenham ; a solitary specimen from the Pabba-shales agrees entirely with our shells; the regular undulations on the sides, and the general con- tour of the mould, are identical with fossils of the same size from Hewlett’s Road near that town, where it occurs with Ammonites Henleyi, Sow. At Charmouth, Dorset, Dr. Oppel collected it with Ammonites Davai, Sow. PECTEN ZQUIVALVIS, Sowerby, 1818. Pecten equivalvis, Sowerby, Mineral Conchology, t. 136. f. 1. The specimens of this species from the Pabba-shales are small and mostly in the state of moulds. There is one large compressed shell 32 PROCEEDINGS OF THE GEOLOGICAL society. [Apr. 22, from Scalpa identical in size with the same species found in the Marlstone of Gloucestershire. The beds at Scalpa have been sup- posed to be Inferior Oolite ; but the presence of Pecten equivalvis, of large size, in them is against that opinion. The fewness of the specimens collected at Scalpa, added to the bad state of preservation of those found, make it a desideratum that these beds shonld be worked with the view of clearing away the doubt. Looking at Mr. Geikie’s sections, and comparing them with the section which ac- companies Sir Roderick Murchison’s paper on the Oolitic Rocks of Sutherland, Ross, and the Hebrides*, I am disposed to think that the geologist would be rewarded by the discovery of both Marlstone, Upper Lias, and Inferior Oolite in the Island of Scalpa. PECTEN, nov. sp. This specimen is distinct from all the other Middle Lias Pectines ; but, as it is only an imperfect mould, it is impossible to give a dia- gnosis of the species. PLICATULA SPINOSA, Sowerby. Plicatula spinosa, Sowerby, Mineral Conchology, t. 245. f. 1-4; Goldfuss, Petrefacta Germaniee, t. 107. f. 1. | This species is a very common shell in the Middle Lias of England, France, and Germany, and is found in the Pabba-shales. The spe- cimens from Pabba measure ;%,ths of an inch in height. GeRvILLIA Maccutiocui, Wright, nov. sp. Shell large, oblong, equivalved ; moderately thick anteriorly, and thin posteriorly ; umbos acute, extending to the extreme limit of the anterior border; hinge-margin straight, about 3 inches long; anterior auricle absent ; posterior long, wing-like, but imperfectly preserved ; folds of growth irregular, and strongly marked on the mould ; a prominent carina passes in an oblique direction, from the middle of the left valve towards the posterior border ; inferior border very convex, which gives an unusual height to the shell; anterior border oblique, but nearly straight. Dimensions. — Length 51 inches; height 2? inches; thickness 13 inch. This fine specimen, which is unfortunately broken, was collected from the Pabba-shales (Middle Lias). A portion of the posterior wing and of the convex lower border are absent, so that my mea- surements are only approximately true. The diagnosis, however, will enable palzeontologists to distinguish this Gervillia, which is the largest species yet found in the Lias; the height of the shell, the flatness of the valves, the straightness of the anterior border, the acuteness of the umbos, and the convexity of the inferior border di- stinguish it from G. lata, Phil. The size of the shell, the straight- ness of the hinge-margin, and the irregular marking of the lines of growth distinguish it from G. /evis, Buckm., which is found in the * Trans. Geol. Soc. 2nd series, vol. ii. p. 353. 1857. ] WRIGHT—LIAS FOSSILS FROM SKYE. 33 Middle Lias near Cheltenham ; with G. crassa, Buckm., from the Lower Lias, it has no affinities whatever. I dedicate this fine species to the memory of Dr. Macculloch, to whom we are indebted for much valuable information on the geology of the Western Islands of Scotland. I am the more desirous of con- necting that eminent geologist’s name with the Pabba-beds, seeing that the Gryphea dedicated to him proves to be a previously- described species. GrRYPH#A CyMBIUM, Lamarck, 1816. Gryphea cymbium, Lamarck, Animaux sans Vertébres, vol. vi. p. 198; Goldfuss, Petrefacta Germania, t. 84. f. 5; t. 85. Gryphea Maccullochit, Sowerby, Mineral Conchology, t. 547. ap eh This species has long been misunderstood by English paleeontolo- gists, as it is not an abundant shell in England ; I have collected it, with Ammonites Henleyi, Sow., at Charlton near Cheltenham, and I have received specimens from near South Petherton. The shells collected by Mr. Geikie from the Pabba-shales enable me to clear up a doubt which has long existed relative to Gryphea Maccullochit, Sow., being a variety of Gryphea obliquata, Sow. ; for these speci- mens, collected, like the types of Sowerby’s species, from the Lias at Pabba, enable me to state that Gryphea Maccullochi, Sow., from Pabba is the true Gryphea cymbium, Lamk. One of the Pabba specimens represents Goldfuss’ var. y, dilatata ; it is 33 inches in height by 3 inches in breadth; other examples nearly agree with Sowerby’s figures 2 and 3. t.547. In Gloucester- shire this Gryphea is found in general in the Middle Lias Clay ; but in Yorkshire it occurs in the Marlstone. In France it attains a very large size, and is collected in several Departments from the upper region of the Middle Lias with Ammo- nites margaritatus, Montfort. GRYPHZA OBLIQUATA, Sowerby, 1818. Gryphea obliquata, Sowerby, Mineral Conchology, t. 112. f. 3. obliqua, Goldfuss, Petrefacta Germanie, t. 85. f. 2. Although this shell is sometimes mistaken for Gryphea arcuata, Lamk., and sometimes for Gryphea Maccullochii, Sow., it 1s never- theless distinct from both. In Gloucestershire it is found in the Obtusus-bed of the Lower Lias, and ranges upwards to the base of the Middle Lias. It has a similar distribution at Lyme Regis, Dor- setshire, and at Robin Hood’s Bay, Yorkshire; and is found in the lower beds at Pabba. In Gloucestershire Gryphea arcuata, Lamk., is found in the lower beds of the Lower Lias; Gryphea obliquata, Sow., in the upper beds of the Lower Lias; Gryphea cymbium, Lamk., in the Middle Lias ; and Gryphea gigantea, Sow., in the Marlstone. VOL. XIV.—PART I. D 34 PROCEEDINGS OF THE GEOLOGICAL society. [Apr. 22, OsTR#HA ARIETIS, Quenstedt, 1856. Ostrea arietis, Quenst. der Jura, t. 10. f. 10. On two slabs of sandstone from Lussay, obtained from the Lower Lias beneath the coral-bed, there are a number of small plaited Oysters which resemble Quenstedt’s Ostrea arietis; they are not identical with the figure in his “ Jura,” but they resemble it more closely than any other described species I am acquainted with. PENTACRINUS ROBUSTUS, Wright. Pentacrinus Goldfussu, Wright, 1854, Annals and Mag. of Nat. Hist. 2nd series, vol. xiii. p. 380, pl. 13. f. 3. This Pentacrinite is a very characteristic Crinoid of the Middle Lias of Gloucestershire, where it has been collected with Ammonites capricornus, Schlotheim (A. maculatus, Young & Bird), at Chipping Campden, and at Hewletts near Cheltenham, im the same zone. The plates of the column are thin; each fourth or fifth plate is broader, and projects beyond the plate below and above it. The pelvis and primary and secondary arms are very robust, hence the specific name; I originally figured and described this species as Pentacrinus Goldfussii, Wr., before I was aware that Professor M‘Coy had previously given the same name to another species ; it will therefore be figured in my monograph on the Oolitic Echinodermata as Pentacrinus robustus. Mr. Geikie collected five fragments of the column of this species from the micaceous shales at Pabba. PENTACRINUS GRACILIS, Charlesworth, 1847. Pentacrinus gracilis, Charlesworth, London Geol. Journal, t. 9. The specimen is not in good preservation ; it consists of a portion of the calyx, with its primary and secondary arms; the bifurcation of the primaries, almost as soon as they branch from the calyx, and the long, simple, cylindrical, secondary arms, without pinnules, suf- ficiently distinguish this species from its congeners. It is contained in a highly micaceous fossiliferous slab of the Pabba-shales ; nearly the same horizon in the Lias as that from whence the original speci- men from Staithes, Yorkshire, in the York Museum, was collected. IsastRzA Murcuisoni, Wright, nov. sp. Corallum large, and very massive ; surface convex, and covered with numerous concave cells. Calices unequal in size and form; the larger ones occupy the upper surface, and the smaller ones are situated on the sides of the corallum. The calices are polygonal, deep, and concave ; their sides are of unequal length, and are termi- nated by a very thin mural edge; an ordinary-sized calyx contains thirty-six septa : in some of the smaller ones there are thirty, and in some of the larger ones forty or more septa. The septal systems appear to vary considerably ; but, as the calices are much covered 1857. | WRIGHT—LIAS FOSSILS FROM SKYE." 35 with a fine muddy matrix, it is difficult to count the numbers accu- rately. The septa are of unequal length, and they are thin, waved, and granulated on their upper surface; the columella is absent or rudimentary, and the point of convergence at the bottom of the calyx is always excentral. Dimensions.—Longest diameter of calyx ;4;ths of an inch; trans- verse diameter ;%,ths of an inch ; depth of the calyx =3,ths of an inch. These corals were noticed by Sir Roderick Murchison* as Poly- pifers of the genus Astrea, and compared to the coralline bodies found in the Lias at Ledbury near Bridgewater. The coral-bed was found by Mr. Geikie at Lussay underlying calcareous grit and sand- stone of the Lower Lias; it was irregularly about 3 feet thick, and the corals are enveloped in a fine dark mudstone: the coral-bed rests on a thin band of hard blue limestone, beneath which is a stratum of greenish micaceous nodular sandstone containing Cardinia concinna, Agassiz. Isastrea Murchisoni closely resembles another species of the same genus found in the Lower Lias near Evesham, Warwickshire, Is. Haimett, Wright; but it is distinguished from that species by having the calices larger, the mural edge narrower, the septa thinner and more waved; the columella more excentral. The two corals require a careful comparison to detect their diagnostic characters. I dedicate this species to Sir Roderick Murchison, to whose re- searches we are indebted for much valuable information on the geo- logy of the Hebrides. Having thus critically examined each of the species contained in this collection of Lias fossils from the Isle of Skye, the following conclusions may be inferred from their study :— Ist. That the Lower Lias is represented at Lussay by greenish micaceous sandstone, overlaid by hard blue limestone, on which rests a bed of corals (Isastrea Murchisoni, Wr.) wrapped in a dark mud- stone, the coral very closely resembling a species found in the Lower Lias of Warwickshire ; the coral-bed, 3 feet in thickness, is over- laid by calcareous sandstone and compact blue limestones. Un- fortunately no Ammonite has been found in these beds, so that their precise age cannot be determined ; still, however, the presence of Cardinia concinna, Zieten, is, per se, good evidence that the greenish micaceous sandstones with Cardinie belong to the Lower Lias; for that shell is found only in the lower beds im France and Germany, its true position in Wurtemberg having been ascertained to be below the Bucklandi-bed, where it is associated with Ammo- nites angulatus, Schloth. 2nd. The “‘ Pabba-shales ”’ belong unquestionably to the Middle Lias, as defined in the beginning of this paper; they appertain to their lower division, which includes the Jamesoni-bed, the Ibex-bed, and Davcei-bed ; a comparison of the species collected by Mr. Geikie with the list of the Middle Lias species inserted at pages 24 & 26 is conclusive as to the age of the Pabba-shales. The number of leading * Trans. of the Geol. Soc. 2nd series, vol. ii. p. 368. D 2 36 PROCEEDINGS OF THE GEOLOGICAL socreTy. [May 6, species collected by our author, during his short visit to Pabba, makes it highly probable that, were the shales worked diligently, nearly all the species of the Middle Lias of England would be found therein. 3rd. The ‘shells from the Lias of Scalpa are very meagre and in bad preservation ; they consist of Pecten equivalvis, Sow., Gervillia inequivalvis?, Sow., and a Pleuromya. The ‘position of the beds which yielded these shells, as shown by the section (PI. I. fig. 2) from Scalpa, through Guillimon and Pabba, to the road between Breakish and Lussay, indicates that they may be the equivalent of the Marlstone, and represent the Margaritatus-bed and Spinatus-bed of the table at page 25; the size and form of the large Pecten like- wise favours this opinion. Much good work might be done if these beds and those imme- diately above them were carefully examined, as the species enume- rated are not sufficient to prove that the beds are ‘ Marlstonie,”’ inasmuch as Pecten equivalvis, Sow., is common to the clays below the Marlstone, as well as to that rock itself. It is probable that the Upper Lias and Inferior Oolite will also be found in the neighbourhood, for it has been already proved that the lower division of the Inferior Oolite, characterized by Ammonites Murchisone, Sow., exists in Skye, as the type-example of that most important fossil was found by Lady Murchison, in a nodule of mica- ceous sandstone, at the base of a cliff east of Holme near Portree ; so that doubtless the intermediate strata exist between Holme (Skye) and Scalpa. May 6, 1857. Arthur R. Abbott, Esq., Hitchin, Herts, Lieut.-Gen. John Briggs, Clayton, Sussex, and Capt. G. Harker Saxton, of the 38th Regt. M.N.I., were elected Fellows. Dr. H. R. Goeppert, Professor of Botany &c. in the University at Breslau, was elected a Foreign Member. The following communication was read :— Tue Siturian Rocks and Fossits of Norway, as described by M. Toeopor Kserutr, those of the Batic PROVINCES OF Russia, by Professor Scumipt, and both compared with their BritisH EquivaLents. By Sir R. I. Murcuison, V.P.G.S., F.R.S.,D.C.L., Pres. R. Geogr. S., &c. Introduction.—My former brief sketches of the Silurian rocks of Norway * have recently been much improved and enriched by the la- bours of M. Theodor Kjerulf, who has published an excellent memoir, entitled “ The Silurian Basin of Christianiat.’’ He has also addressed * Proc. Geol. Soc. vol. iv. p. 601; Quart. Journ. Geol. Soc. vol. i. p. 467 ; ibid. vol. iii. p. 1; ibid. vol. xii. p. Gis ‘Geol. Russia in Europe,’ &c.; ¢ Sinria? p. 319, &e. + Das Christiania-Silurbecken, chemisch-geognostisch untersucht. 4to, 1855. 1857.] MURCHISON—SILURIAN ROCKS OF SCANDINAVIA. 37 to me descriptive letters, with illustrative diagrams, exactly defining the relations and dimensions of the different rock-masses, as well as the organic remains of each stratum; the most characteristic specimens of the latter having been transmitted to England for comparison*. The same zealous author has published a work in which he clas- sifies the two great-sedimentary deposits of South Norway, the one exhibiting a vast development of unfossiliferous rocks, to which he applies the name of Cambrian,—the other being the overlying Silu- rian rocks, of which he describes each stratum with its respective fossils from the Alum Shales upwards. My able coadjutor in the work on Russia and the Ural Moun- tains, Count A. von Keyserling, had previously translated and sent to me a memoir, by Prof. Schmidt, on the succession of the Silurian rocks of the Russian province of Esthonia, and the adjacent isles, which portrays the distinctions of the various members composing the Silurian system with much greater precision and clearness than had ever before been applied to that region. I now lay an outline of these documents before my associates, in order to show them how independent observers in other tracts have come to the conclusion, that the Silurian system, as defined by them, as well as by myself, forms a natural-history group, whether we look to its geological relations, or its zoological contents. In the sequel I will revert to my own comparison, and point out how the Silurian rocks of Scandinavia and Russia agree with those of our own country, from the lowest to the highest beds inclusive. Norway.—To begin with Norway, M. Kjerulf divides the whole Silurian series of his country inte three physical groups, which he severally names in ascending order from the tract where it is best exhibited ; viz. Oslo, Oscarskal, and Malm6, and in these he recog- nizes fourteen subdivisions. A. The Oslo group consists of a base of sandstone and conglome- rate, which, though not exposed near Christiania, occur at Langé, Mjosen, and other places. This bottom rock (1), which is unfossili- ferous, is followed by alum-schists and bituminous limestone (2) ; Lower graptolite-schists (3); Orthoceratite-limestone (4); and Upper graptolite-schist (5). B. The second or Oscarskal group is composed of calcareous and argillaceous flags (6 & 7); with intermediate orthoceratite-limestone with encrinite-schists and calcareous sandstone (8). C. The Malmo or upper group exhibits at its base argillaceous schists (9*) with calcareous flags (9°), and Pentamerus-limestone (9°) ; Coral-limestone, often concretionary (10); Encrinite-shale (11); Upper orthoceratite-limestone (12); Upper graptolite-schist (13) ; Upper Malmo limestone and schist (14). The following Table and the annexed general section, fig. 1, explain this order. * These are now placed in the Museum of Practical Geology. *sqstyos [eunoug waddy ‘[{ "OpIZITLNY "TL “sqstyos-oz[cjdeay soddq °c *dUOJSpULS SNOITRITeD *g *9U0JSOUII[-991}8.199 "S}SIYOS-UUN[Y *Z *sqSIYOS [VUILOU "S}SIOS SNODOV][IZIV IOMOT "0G -OYJIO Joddy 10 -owyeyy AAMO'T “ZT “sqstyos-oq1jojdeiy IaMOoT ° JOMO'T PUL JUOJSIWIT]-9IVIIDOYWAG °9 ‘QUOJSIMUT[-SNAIWIEUIT “96 ‘systyos-oqtjoydery soddy “eq *9UOJSIUIT]-9}TJVAIOOYJAQ JOMO'T "fF "SOUOISSEP SHODILT[ISAV pie SNODTVOTeD *7Z *QUOJSIWT|-[CIOD “OT ‘quojsomly owe iaddq ‘FT ol 96 6 G6 01 il ot g1 ZL Tt OL g1 ULE Wr Ge 46 L 9 eer er 5 = S zy EEE” = ee ag GSE EN 5S 2 z5 Ui ZAP SS S wee, OSES) “Ny 54 *(J29J OST-OST) QUITL IAT ‘QUITO "M -oupnyy fO Syooyy Noppmy ay, 07 QULICQ fo syooy (aopnung) uniunpig LaMoT ay? Wolf U01QI09 —"¢ od I a = ‘Ud[Ly U0SIg “A'S'S "ANN ‘o-spunvbapury fo und v fo uo19ag@—'Z ‘BIg ‘hnndony ur syooy unrinjyy ay7 fo uoiqIIg JOLIVaH— | “Sy MURCHISON—-SILURIAN ROCKS OF SCANDINAVIA. 39 Thickness in feet. Local Subdivisions. Local Groups. __ British equivalents. 180 { 14. Upper Malmo limestone . { Upper Silurian. 13. Graptolite-schists . . . .» Upper Malmé{ (Woolhope, 12. Orthoceratite-limestone . . Wenlock, & og9 J 11. Upper encrinal schists . . | | Ludlow Rocks.) 10. Coralline and encrinal lime- | Sbonete” 0): - . > Lower Malmo. Llandovery 370 b. Pentamerus-limestone bel Rocks. a. Argillaceous schists . . J 8. Calcareous sandstone. . .) Lower Silurian. 7. | Calcareous and argillaceous 7005 & flags (Orthoceratites an | Oscarskal . . Caradoc. Encrinal schists) 160 5. Graptolite-schists . F 30 to 40 4. Orthoceratite-limestone . 50 3. Graptolite-schists . ; TBO%G TAOS SAH -sShisia it Lower Oslo. . Stiper Stones. Total 1930 1. Quartzite and mfossiliferous rocks. “| Upper Oslo . Llandeilo. In referring to the section, fig. 1, we see, that the alum-schists (2) with bituminous limestone rest upon unfossiliferous and siliceous grau- wacke (1), evidently the equivalents of a part of the Longmynd (Cambrian) of Britam. In No. 2, the lowest zone in which intel- ligible fossils have been detected in Scandinavia, or the “ Regiones A, B,” of Angelin, there are found small Graptolites, Graptopora flabelliformis, several species of Lingula, including one like L. Da- visit, a horny shell nearly allied to Obolus Apollinis, Agnostus pisiformis, Olenus scarabeoides, Boeck, Olenus (Trilobites) latus, Boeck (Eurycare latum, Angelin), (Trilobites alatus, Boeck), Spher- ophthalmus alatus, Angelin, Trilobites pusillus, Sars, Olenus (Dalm.) gibbosus, Wahl., and Asaphus grandis, Sars. This zone (2), being unquestionably the same as the Regiones A, B, of Angelin in Sweden*, is manifestly the northern equivalent of the ‘‘ primordial zone”’ of Barrande in the Silurian Basin of Bohemia, and of the Stiper Stones and Lingula-schists of Britain ; and, though only 150 feet thick, contains Graptoporat flabelliformis (Gorgonia of Eichwald), mixed with Lingula as in our country, and with them the Agnostus pisiformis and the Graptolite Didymograpsus geminus, as well as the Silurian Brachiopod Orthis calligramma, the last three of which occur also in the true Llandeilo zone of the Silurian region of Britain. In other words, we thus see clearly how, in extending our survey, it is impracticable in general classification to separate the Lingula-flags, or ‘‘Zone Primordiale,” from the Lower Silurian rocks. The next mass of schists (3, 4, 5), with an intermediate limestone, bears a close analogy to its congener in Britain, by ushering in with it a profusion of brachiopods, and clearly represents the Llandeilo formation. Thus, amongst its fossils are the Graptolites, Diplograp- sus pristis, D. folium, D. teretiusculus, Graptolithus sagittarius, and the shells, Orthis calligramma, O. elegantula (O. parva, de Vern. ); * See M. Barrande’s lucid memoir, ‘‘ Paralléle entre les Dépots de Bohéme et de Scandinavie,” 1856. _t The generic name proposed by Mr. Salter in 1857 for this curious form, which is evidently one of the Fenestellide, and connects that group with the Graptolites. Report American Assoc. for 1857, Montreal. 40 PROCEEDINGS OF THE GEOLOGICAL society. [May 6. O. flabellulum (?), Bellerophon bilobatus, B. acutus, Orthoceras du- plex, O. annulatum, Lituites cornu-arietis, Phacops conophthalmus (Powis, Sil. Syst.) ; with many Trilobites of species peculiar to Sweden, but, all belonging to the Lower Silurian genera, Asaphus, Ogygia, Trinucleus, Olenus, &c. The group (6,7) consisting of calcareous and argillaceous flags, in- termediate orthoceratite-limestone, and lower encrinal schists, though intimately connected by many forms with the underlying divisions, is yet characterized by many other fossils, which enable us to refer it to the true Caradoc or Bala formation, as now defined, and as will be more completely explained in a new edition of ‘Siluria.? These fossils are, Orthis calligramma, O. testudinaria, O. Pecten, Leptena sericea, Lingula attenuata, Bellerophon bilobatus, B. acutus, Conu- laria quadrisulecata, and probably C. Sowerbyi, with other species. Orthoceras duplex, O. gigas, O. dimidiatum, O. distans, and O. annu- latum ; the last three being Upper Silurian forms in Brita. The other fossils of Lower Silurian age are: Lituites cornu-arietis, Tro- cholites anguiformis, Euomphalus, and Turbo ; several species, in- cluding Luomphalus alatus, Hisinger, with Echinospherites auran- tium, Tentaculites anglicus (annulatus, Sil. Syst.), with the well- known Trilobites dsaphus expansus, Trinucleus concentricus (Carac- taci, Sil. Syst. var.), 7’. seticornis, Ampyx nasutus, Ogygia, Calymene Blumenbachii (var. pulchella), and the Phacops macroura, Sjogren, which closely resembles the P. truncato-caudatus of the British Caradoc formation. The Corals are Stenopora fibrosa and its variety Lycoperdon, with species of Turbinolopsis, &c. The calcareous sandstone (No. 8, sections) would seem, from its organic remains, to constitute the commencement of a transition from the Lower to the Upper Silurian rocks, such as is seen in the Lower Llandovery rocks of South Wales. Thus, with the Orthis testudinaria and O. zonata, Dalm., and Patella antiquissima, His., occurs a characteristic Lower Llandovery species, Rhynchonella angustifrons, M‘Coy, and many large smooth Pentameri of species not yet named. Here are some associated fossils which are also commonly found in the Upper Silurian rocks of Britam, These are: Strophomena depressa, Euomphalus sculptus, Phragmoceras? (Cyrtoceras) ventricosum, En- crinurus punctatus, Actinocrinus moniliformis, Favosites alveolaris, Heliolites megastoma, Halysites catenularius, Cyathophyllum turbt- natum, &e. In speaking of the characters of the fossils of this zone, it is to be observed, that the characteristic Lower Silurian trilobites have already disappeared*. The argillaceous schists with calcareous flags (No. 9a) obviously represent also a part of that intermediate group connecting the Lower and Upper Silurian, to which I have now assigned the name of *« Llandovery rocks.’’ For, in these beds certain species of Pentamert are first met*with, whilst the overlying limestone (94) is, as im * Several of these corals and shells in Britain range from the Llandeilo forma- tion to the base of the Ludlow rocks. 1857.] MURCHISON—SILURIAN ROCKS OF SCANDINAVIA. 4] Britain, charged with the Pentamerus oblongus, and forms in both countries a clear horizon. The fossils are : Fenestella assimilis, Alveolites (Millepora) repens, Ceenites intertextus, Ptilodictya (Eschara) scalpellum, Halysites catenularius, Orthis calligramma, O. elegantula, O. testudinaria, O. Pecten, O. zonata, Dalm., O. lamellosa, Strophomena depressa, Leptena transversalis, Orthis (Spirifer) insularis, O. biforata (Sp. Lynx, Sp. dentatus, Atrypa crassicostis, Dalm., &c.), O. biloba (Sp. sinuatus, V. Buch), Cyrtia trapezoidalis, Trigonotreta compressa, Pen- tamerus ( Atrypa) galeatus, Atrypa prunum, A. tumida, Pentamerus Lens, P. levis, Atrypa reticularis, A. aspera, Dalm., Euomphalus JSunatus, E. sculptus, Acroculia Haliotis, Calymene Blumenbachii, Encrinurus punctatus, Ampyx, Acidaspis, and the Trilobites ellipti- Srons (Proetus’) of Esmark, Tril. elegans, Sars, &e. The band with Pentamerus oblongus is at once followed by another limestone (No. 10) bighly charged with corals and crinoids, and which evidently characterizes the mass of the Wenlock limestone. It is, however, important to remark that, with many corals, the EHuomphalus sculptus, E. carinatus, and even the Orthoceras annu- latum and O. Ibex, Sil. Syst., we again meet with the Pentamerus oblongus and P. levis of the subjacent band, thus linking together, still better than in England, these beds with the inferior strata, and showing a higher vertical range of the above species of Pentameri than is known in England, where they never rise into the Wenlock formation. The list of fossils includes Ptilodictya lanceolata, P. (Es- chara) scalpellum, and the corals, Cyathophyllum turbinatum, Goldf., Ptychophy!lum patellatum, several species of Heliolites, and several forms noticed in the underlying strata, with Sarcinula organum, a species of Lower Silurian age in Brita. The prevailing Encrinite is Actinocrinus moniliformis, Goldf., whilst the Cornulites serpula- rius, Sil. Syst., is accompanied by the following shells, Rhynchonella borealis (Ter. plicatella, Dalm.), Huomphalus carinatus, E. sculptus, and other spiral forms, Orthoceras Ibex, O. annulatum, with the Pentamerus conchidium and the other species above noted. The encrinal schists (11) and Upper Orthoceratite-limestone (12), the Upper Graptolite-marls (13) and the Upper Malmé limestone (14), with the schists and marls of Overland, Opsahl, Noes, Krogsand, &c., represent other members of the Upper Silurian, as far as the lower and middle members of the Ludlow rocks inclusive—the Upper Ludlow rock not being well represented by fossils. Whilst the ordinary Wenlock Corals seem to pervade all the last- named rocks, their lower members or the encrinal schists and Or- thoceras-limestone, characterized by large Orthoceratites with cen- trals iphuncles, may be supposed to represent the Lower Ludlow, the more so, as it contains Gomphoceras pyriforme, Sil. Syst. In the overlying shales Graptolites (Ludensis) priodon abounds ; but it is to be noted that this zoophyte is associated with the Retiolites Geinitzianus, Barr., and Cyathocrinus rugosus, both of Wenlock age an Britain the former even pointing to the very base of the formation. 42: PROCEEDINGS OF THE GEOLOGICAL sociETy. {May 6, Even the upper limestones, schists, and shales, as seen at Malmo and the places above cited, are still charged with some corals and crinoids, known in England only in the Wenlock formation, including among the latter, Hucalyptoerinus decorus and Crotalocrinus (Cya- thocrinus) rugosus. On the other hand, here are also found some of the typical species of the Ludlow rocks, viz. Chonetes (Leptena) lata, Rhynchonella Wilsoni, R. navicula, Turbo corallii, Pterinea retroflexa, Orthoceras Ibex, &c. : In my own rapid survey of the environs of Christiania, as formerly explained to this Society, I could not, any more than M. Kjerulf, detect fossils indicative of the uppermost Ludlow rock, though I first pomted out the conformable passage upwards from the grey Silurian rocks into an overlying red sandstone. In some parts of Sweden, however, and on another occasion, my coadjutor M. de Verneuil and myself detected organic remains in strata which must, we thought, represent the Upper Ludlow, and even a transition into the Devonian. Thus, in Scania we found true Upper Ludlow fossils in red flaggy sandstones which Forchhammer had classed as Old Red Sandstone *. : Again, in proceeding from the northern and central parts of Goth- land, which are occupied by the Wenlock limestone, we at length reached beds of a sandy and marly character, in which some of the species above mentioned, including the Pterinea retrofleca, Chonetes data, and Turbo corallii, were collocated with the Rhynchonella (Terebratula) nucula, Orthonota retusa, Murchisonia articulata, and Beyrichia tuberculata, all fossils of the Upper Ludlow rock. As these forms are, in the ascending order, associated with fossils which occur in the Eifel and other Devonian tracts, including the Calceola sandalina, it was presumed, that the southern pro- montories of Gothland offer a passage from the Silurian into the Devonian rocks. In the meantime we learn by these evidences, how, with the vary- ing conditions of the seas during these epochs, the same species have had a longer existence in one region than in another. M. Kjerulf has verified, 2m sztw, all the organic remains he enume- rates, and has followed each band of rock throughout all its undula- tions or breaks in the Bay of Christiania. From his numerous sec- tions I have extracted three, which are annexed (p. 38). The first of these is the general diagram, fig. 1, the second (fig. 2) repre- sents the ascending order near Beston Kilen, from the lowest fossil- iferous beds, No. 2 (alum-slates, or “‘ primordial zone’), through the lowest graptolite-schists (3), the Orthoceratite-limestone (4), and the Upper Graptolite-schists (5),—the three beds representing the Llan- deilo flags, to the calcareous and argillaceous flags, 6 & 7, containing Caradoc fossils: all these beds and fossils are Lower Silurian, and are seen to be overlaid by the basement-beds of the Upper Silurian, Nos. 8 & J. The third diagram is a section from Orm6, across the whole island of Malmo, and exhibits at the base Nos. 6 & 7 of the Lower Silu- * Quart. Journ. Geol. Soc. vol. iii. p. 34. 1857. | MURCHISON—SILURIAN ROCKS OF RUSSIA. 43 rian, followed by 8 & 9, or the equivalents of the Llandovery rocks, which connect the inferior and superior divisions. These masses are overlaid conformably by, and pass up into the Upper Silurian series, 10 to 14 inclusive, the whole of which are chiefly charac- terized by fossils of Wenlock and Ludlow species. These detailed sections of the strata im the environs of Christiania are most valuable : first, in demonstrating, by comparison, that the Silurian rocks of Norway are, from their base upwards, the true equivalents of those of Britain ; secondly, in pointing out in the very lowest fossiliferous zone the presence of those zoophytes (Grap- tolites) which prevail throughout the series. In the same beds occurs a Lingula, associated with Orthis callactis and other forms which, in Britain, have as yet been found only in the lower part of the Llandeilo formation; and with these is found the Graptopora flabelliformis, a fossil of the Lingula-schists of Wales: thus showing that, like them, the alum-schists form the natural-history base of the Silurian System. The sections also demonstrate that from this base to the uppermost beds, these zones (in all occupying less than 2000 feet in vertical dimensions) represent the whole of the vastly ex- panded British series, and constitute one conformable and natural system, whether viewed physically or zoologically*. In addition to the clear order of superposition of the various Silu- rian rocks and their identification by fossils, M. Kjerulf has further shown, how different members of the series have been here and there metamorphosed into crystallme gneiss. The numerous points at which the sedimentary formations have been pierced by eruptive rocks long ago offered to Professor Forchhammer and myself suf- ficient explanation of such conversions‘. This subject has, indeed, been since worked out in some detail by Mr. David Forbes, whose residence at Christiania has enabled him to contribute satisfactory information, which clearly demonstrates the conversion of sedimentary Silurian strata into crystalline rocks replete with simple mineralst. Results of an examination of the Silurian Rocks of Esthonaa, Northern Livonia, and the Isle of Oesel, made in the years 1853 ¢o 1856. By Professor Fr1rp. Scumipt, of Dorpat. The Silurian rocks of Esthonia, Northern Livonia, and the Isle of Oesel, represented in a map which was transmitted to the Society, consist essentially of a series of strata which follow each other in ascending order at slight angles of inclination, and constitute zones trending generally from east to west. These strata have the follow- ing descending order :-— * Judging from a collection recently transmitted by M. Kjerulf, and which has been examined by Mr. Salter, the specific identification with the British forms may be for the most part depended upon. tT Quart. Journ. Geol. Soc. vol. i. p. 470, &c., and Russia in Europe, vol. i. p. 14, note. $ Quart. Journ. Geol. Soc. vol. xii. p. 166, &c. 44 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6, Grey limestone with shales. Fishes. (No. 5.) Limestone and dolomite. (No. 4.) Pentamerus-limestone. Corals. (No. 3.) Limestone with marly beds. Corals. (No. 2.) Brandschiefer. Calcareous flagstones or “ Pleta.”” (No. 1.) Green sand-beds and chloritic limestone. Argillaceous schist. Ungulite grit. Blue clay and sands. The most ancient beds of the system are seen to subside under No. 1 of Schmidt’s Map (and the above list), or summit of the cliffs of the north of Esthonia on the Gulf of Bothnia, known under the name of ‘‘ Glint ;” and, although occupying no considerable por- tion of the country, those rocks alone have been hitherto chiefly studied. With the exception of the lowest argillaceous and sandy beds, which are well known (as extending from St. Petersburg into the base of these cliffs), the Silurian series of Esthonia is almost entirely composed of calcareous bands more or less pure, which, in the upper strata, often pass into dolomites. The latter varieties, however, occupy no special stratigraphical position, and are not distinguishable through their organic remains from the ordinary limestone with which they are associated. On the contrary, the limestone and the dolomite of the same zone or stage contain precisely the same fossils. Each of the five stages dicated in the map prepared by M. Schmidt possesses a peculiar fauna, which is constant throughout the whole of the horizontal extension of the zone. Very few species traverse two entire stages without undergoing what are termed by that author “‘ modifications.’ Thus, several species belong in common to the two lower bands,—others to the two upper; but, according to him, one species only, the Calymene Blumenbachii, passes through all the stages, from the first to the fifth inclusive, though in the last of these (the equivalent of the Upper Ludlow rocks) it is modified into the C. spectabilis of Angelin. The sharpest separation in the fossiliferous contents of this series occurs between the second and third bands; thus dividing the “‘terrain”’ into Lower and Upper Silurian. These two divisions seem to contain few species common to them, or, to use M. Schmidt’s lan- guage, no form which has not been modified. At the junction of these inferior and superior masses there are, however, transitions, which testify that there has been no violent break in the development of animal life, and induce the author to believe, that in this country the Silurian formation is a whole, whose members constitute a compact series of calcareous strata shading into each other, but not conducting by similar points of approximation to the overlying Devonian rocks of Livonia, which occur, he says, as an entirely separate system. This sharp distinction is indeed explained by the physical relations of the rocks; for, whilst the uppermost Ludlow rocks are clearly represented, they are overlaid transgressively by those Devonian 1857. | MURCHISON—SILURIAN ROCKS OF RUSSIA. 45 masses which, as formerly shown by my colleagues and myself, con- tain the Devonian shells of Devonshire and the Rhine, united in the same beds with the fishes of the Old Red Sandstone of Scotland. However small may be the number of species common to two of the Silurian zones, examples are not wanting to show that, when a change occurs, each typical fossil is replaced in the next succeeding band by an analogous form, which, in its turn, is constant throughout the entire extent of its stratum. Now, as this continuity of forms stops at the uppermost limit of the Silurian rocks, the phenomenon, as M. Schmidt observes, seems to operate as much in favour of the distinction of the various bands or stages, as it clearly does for their union in one system of life. The researches of M. Schmidt have furnished him with nothing new respecting the inferior portion of the Silurian strata, which, pass- ing from the Government of St. Petersburg, underlies the cliffs of Esthonia called Glint. That lower series consists in an ascending order of sands and clay, Ungulite-grit, argillaceous schists, and a chloritic grit and limestone, as described in ‘Russia and the Ural Mountains.’ The summit of the cliffs is composed of grey, flag-like limestone, the “‘ Pleta’’ of the Government of St. Petersburg, and marked No. 1 in M. Schmidt’s map. This limestone ranges a little southwards into the continent, disappearing at a very gentle angle under the superior formations. The blue clay, cropping out to the east of Reval only, sinks on the west beneath the sea-level. The “‘Ungulite-grit ”’ contains its usual fossils, Obolus Apollinis, Orbicula Buchii*, and O. reversa; whilst the schists present us with the Graptopora (Gorgonia) flabelliformis, Kichw. (the Phyllograpsus of Angelin), which, in Sweden, is characteristic of the lowest fossil-beds or alum-slates. | In the green sand‘ or chloritic rock of Esthonia, no one has posi- tively discovered the existence of the microscopic tooth-like bodies that M. Pander has collected from the same bed in the Government of St. Petersburg, and described as fish-teeth. Along with the Odolus, however, M. Schmidt has detected a Lingula and the Orthis calli- gramma. The chloritic limestone is specially developed at the foot of the cliffs of the Isle of Odinsholm. Grains of chlorite are there strikingly disseminated in a greyish-white limestone. This rock constitutes a marked feature, and is equally visible at Baltisch Port and Reval. In point of organic remains, it contains numerous frag- ments of Asaphi, and notably of a species resembling 4. Tyrannus, Murch. (the 4. heros of Dalman). This chloritic limestone passes into the Government of St. Petersburg without containing a peculiar fauna. The calcareous flagstone called Pleta, No. 1, is exhibited in great * The names of all the fossils in this part of the memoir are those given by Prof. Schmidt. The species have not been yet compared, like those of Norway, with their British analogues.—R. I. M. + Prof. Ehrenberg’s researches (Berlin Transact. 1855) tend to prove that a portion at least of the green grains in this sand has been derived from the minute stony casts of the shells of Polythalamia. 46 PROCEEDINGS OF THE GEOLOGICAL SOcIETY. [May 6, constancy of character from the Isle of Odinsholm and the cliffs of Baltisch Port to Narva and the hills south of St. Petersburg, where it is part of the Lower Silurian of M. Kutorga*. The most im- portant fossils of this rock are its Orthoceratites, Orthoceras duplex, O. vaginatum, O. undulatum, Schlotheim and Quenstedt, and the O. acutum, Kichw. These are accompanied by Asaphus expansus, A. raniceps, Illenus crassicauda, Lichas Hubneri, L. verrucosus, Cheirurus exsul, Beyr., Lntuites convolvans, L. faleatus, L. Odini, Eichw., Bellerophon locator, Kichw., B. megalostoma, Kichw., Porambonites equirostris, Rhynchonella nucula, Orthis calligramma, O. infleca, O. extensa, O. obtusa, Orthisina adscendens, Siphono- treta unguiculata, S. verrucosa, Spheronites aurantium, Echino- spherites Balticus, Hemicosmites pyriformis, Receptaculites orbis, Eichw., &c. Towards the upper limit of this stage, and in the eastern part of Esthonia, there is found a bituminous shale, known as “ brand- schiefer’’ or inflammable schist, formerly described by Colonel Hel- mersent. Occurring at Tolks and Pungern, it is very rich in well- preserved fossils, which seem to connect the underlying calcareous stage with the next overlying limestone, many of the species being peculiar to the deposits. ‘Trilobites abound, but have not yet been all identified, though among them are dsaphus acuminatus, Boeck, Cheirurus aculeatus, Kichw., Ampyx, Trinucleus, and Phacops, with Beyrichia and Leperditia, Leptena sericea, L. Humboldti, and other fossils. The second limestone is a fine-grained, yellowish, and bluish rock, occasionally having almost the aspect of lithographic stone, and passing often into marly beds particularly rich in fossils. This stage forms the northern half of the Isle of Dagden, and thence passes eastwards in a broad zone across Hsthonia to the south of Narva and into the Government of St. Petersburg, where it has been called Upper Silurian by M. Kutorga. In reality, however, says M. Schmidt, this limestone is only the superior member of the unquestionable Lower Silurian rocks of Russia. Among its prevailing fossils may be cited Lichas angusta, Beyr., L. Dalecarlica, Ang., Calymene brevicapitata, Portl., Enerinurus multisegmentatus, Portl., Phacops, several species of LIituites antt- guissimus, Kichw., Murchisonia bilineata, Hall, Subulites elongatus, Conr., Strophomena Asmusii, S. rugosa (distinct from S. depressa), Leptena deltoidea, L. sericea (very abundant), Orthis Actonia, O. testudinaria, Orthisina anomala, O. Vernewilii, Streptoplasma corniculum, Heliolites megastoma, H. favosa, Ptilodictya acuta, P. pulchella, Hall, Coccinium proevum, Kichw., Cyclocrinites Spaskit, Eichw., and Calamopora patellaria, Kutorgat. The two preceding stages contain the following fossils in com- * See the Map of the Government of St. Petersburg, by M. Kutorga. + Annuaire du Journal des Mines de Russie, 1838, p. 97. t The so-called Pentamerus ventricosus, Kutorga, of this stage seems to be a Porambonites of Pander. 1857. | MURCHISON—SILURIAN ROCKS OF RUSSIA. 47 mon: Phacops Odini, Kichw., Orthis lynx, Kichw., Leptena unbrex, Lingula quadrata, and Chetetes Petropolitanus. The upper limit of these Lower Silurian strata is characterized by a profusion of Corals, such.as Catenipora, Heliolites, Caninia, Sar- cinula organon, &c. Accompanying these, there are other fossils peculiar to the band, viz. Proetus brevifrons, Ang., Lichas, n. s., Pleurorhynchus, u.s., Strophomena alternata, Atrypa (Spirigerina) marginalis, and Orbicula, n.s. ‘These two latter, however, are asso- ciated with most of the previously mentioned fossils of the second stage; so that the whole form one natural division. This coralline limestone is surmounted by the most ancient stratum of the group classed as the Upper Silurian of Esthonia; being cha- racterized chiefly by the presence of its smooth Pentamert. A marly limestone forms the basement-layer of No. 3, and con- tains Leperditia marginata, Pentamerus linguifer, Strophomena Pecten, Orthis Davidsoni, Rhynchonella aprinis, Vern., and Calamo- pora aspera, D’Orb. This stratum is covered, throughout the whole length of the zone, by the shelly band with Pentamerus borealis, which occupies the highest ground of the mainland of Esthonia, and forms the watershed of all the tract. The bottom beds, with Leper- ditia, observed at a very few spots to the north of the Pentamerus- zone, reappear to the east, west, and south, in a more developed form. In the last-mentioned direction, they serve as the support of a band containing another species of Pentamerus, the P. Esthonus, Eichw., probably identical with the P. oblongus (see Sil. Syst.) ; but, unlike the P. dorealis*, this species does not occupy all the rock. The associated characteristic fossils are, Bronteus signatus, Phill., Orthoceras canaliculatum, Sow., and Catenipora escharoides. Other fossils, the chief habitat of which is in the next overlying stage, now appear, and these are Enerinurus punctatus, Calymene Blumenbachit, and Atrypa (Spirigerina) reticularis. This stage, as already stated, offers points of connexion with the subjacent No. 2, along its line of junction, but the Corals (Catenipora) of the two bands are specifically separable. The stage No. 4, which is developed partly on the continent and partly in the north-eastern portion of the Isle of Oesel, consists of two different rocks, the one a bluish-grey marly limestone, the other a dolomite or magnesian limestone. Its chief fossils are, Proetus concinnus, Lichas Gothlandicus, Ang., L. ornatus, Ang., Bumastus Lindsteineri, Ang., Orthoceras annulatum, Sil. Syst., Rhynchonella Wilsoni (Russian variety: see ‘Russia in Europe,’ vol. ii. p. 88), Athyris tumida, Orthis osiliensis, Schrenck, O. elegantula, Dalm., Leptena transversalis, Streptoplasma calicula, &c. This zone also * In reference to these detailed views, my friend Count Keyserling is of opinion that the band containing the Pentamerus borealis is virtually included in the zone beneath it ; fallacious appearances in this flat and obscure country having led Prof. Schmidt to believe in the superposition of the one to the other. Count Keyserling also thinks that, in consequence of its fossils, more importance should be attached to the brand-schiefer or inflammable schist, which might be considered a distinct - subformation. 48 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. {May 6, contains some remains described as fishes by Eichwald under the name of Sphagodus obliquus. The fifth division forms the summit of the Silurian system of Esthonia, and is composed chiefly of a crystalline limestone, rarely dolomitic, alternating with beds of marl or shale. The remains of fishes now begin to appear frequently, and Pander has recognized in the materials sent to him twenty species, all of which, however, are affirmed by him to be specifically distinct from any Devonian or Old Red forms. The finest of these Upper Silurian species is the Cephalaspis verrucosus, Pand. (Thyestes, Kichw.), and with it is found the Onchus Murchisoni, Ag., of the Ludlow rock; sufficient fragments of the former having been detected to complete the restoration of an almost entire fish. These remains, including numerous scales and also portions of jaws, are now described by M. Pander*. One of the most remarkable fossils of this band is the Hurypterus remipes, Dekay, which is abundant in some of the marly beds, and in so admirable a state of preservation as to permit the delineation of all its minutest parts, which Dr. Schrenck will elucidate. The most important of the other fossils of this, the highest Silurian zone in Russia, are: Beyrichia tuberculata, Klod., B. Wilekensiana, Jones, Leperditia Baltica, His., L. phaseolus, Klod., Orthoceras imbricatum, O. bullatum, Sow., Murechisonia cingulata, Trochus heliettes, Pterinea reticulata, Grammysia cingulata, His., Lucina (Tellina) prisca, Chonetes striatella, Dalm., Spirigerina prunum, Dalm., S. didyma, Rhynchonella Wilsoni, Sow. (Sil. Syst.), Orthis orbicularis, Sow. (Sil. Syst.), Tentaculites annulatus, His. (?), Cya- thocrinus rugosus, Mill., Cyathophyllum articulatum, &c. These grey beds (so manifestly identical through many of the species of their organic remains with those of the Upper Ludlow rocks) present no ascending passage, as in England, into the super- jacent red or Devonian strata. The latter are not seen in the Isle of Oesel, but appear on the continent, where their junction with the Upper Silurian is evidently transgressive. At Tannekill, to the north of Tellin, for example, the Devonian rocks, consisting of a yellowish- grey coarse-grained grit and bluish marls, are seen to overlie at once the formations Nos. 3, 4 of the preceding Silurian succession, with their characteristic Corals. At Dorpat, Randan, Tellin, and Tongal, * The work of my distinguished friend, M. Pander, has been seen for the first time by me as these pages are printing off. Professor Huxley, who has been so obliging as to examine this work, informs me that the Cephalaspis verrucosus (Thyestes, Eichwald) presents a tuberculated ornamentation on the head- and body-scales, which is, as it were, a more regular development of the ornamentation described by Sir P. Egerton as occurring in Cephalaspis ornatus of the uppermost Ludlow rocks (see Quart. Journ. Geol. Soc. vol. xiii. p. 285). These remarkable ichthyolites, of which many genera and species are described, will be alluded to in the new edition of ‘ Siluria,’ when the nature of the singular minute and enigmatical remains, from the Lower Silurian rocks, called ‘‘ Conodonts”’ by M. Pander (op. cit. pls. 1, 2, 3, 4) will be discussed. With the highest respect for the author, and the great ability he displays in his works on ichthyolites, 1 am not yet convinced that these microscopic bodies are portions of the teeth of fishes.—(Oct. 10.—R. I. M.) 1857.| MURCHISON—SILURIAN ROCKS OF SCANDINAVIA. 49 which lie at a considerable distance from the junction with the Silu- rian rocks, the strata are charged with many well-known Devonian fossils. CONCLUSION. In the opening pages of this Memoir a running comparison was instituted between the different subformations which constitute the Silurian basin of Christiania in Norway and their British equivalents ; and, considering the distance of the Norwegian tract from our own country, the coincidence in the succession of fossils is truly re- markable. The point, however, of the labours of M. Kjerulf to which I now particularly recall attention, is that in the very lowest fossiliferous zone (the alum-slates of Norway) the types of Trilobites which were supposed by some authors to be confined to that zone are united with the Orthis calligramma and the Didymograpsus geminus, spe- cies known as occurring in unquestionable Lower Silurian British rocks. Any one of the published sections across the western parts of Shropshire, z.e. from the Longmynd over the Stiper Stones, shows what the parallel order is in Britain*. Having for the last twenty-four years considered and described the Stiper Stones as the true physical base of the Silurian series of strata, it has been satisfactory to me to detect recently, in the black schists associated with the siliceous flagstones of that ridge, additional fossils which so intimately connect them with the Llandeilo formation, that the additional evidence in the new edition of ‘ Siluria’ will, I believe, be conclusive as to the natural base of the British Silurian rocks. For neither in Shropshire nor in Norway can we draw a line of physical or zoological demarcation between these basement- strata, whether termed Lingula Flags, Stiper Stones, or Alum Slates, and those overlying schists into which they graduate, and of which they form an integral part. This union is indeed particularly well marked in Scandinavia, where the alum-slates are simply a mass of black schist, which is no more capable of separation from the overlying beds of similar cha- racters than one bed of the Lower Lias or any other secondary shaly subformation is from another. Seeing the dissimilarity of forms which prevails throughout the Silurian series of Bohemia, as described by M. Barrande, when we look to the distinction between the fossils of each of the subdivi- sions, and especially when we compare such subdivisions with their acknowledged equivalents in the northern Silurian zone now under consideration, it seems to me to be impossible to establish a new classification of the Lower Paleozoic rocks by eliminating the “‘ Zone Primordiale” of that distinguished author from the natural-history system in which he has himself placed it. In Bohemia the “ Zone Primordiale’’ is as integral a part of the Silurian basin so called, as the Stiper Stones were in my original classification. If I am not * See the ‘ Silurian System,’ pl. 32. fig. 1, &c., and ‘ Siluria,’ Fic ta p. 29. VOL. XIV.—PART I. 50 PROCEEDINGS OF THE GEOLOGICAL society. [May 6, justified in referring to my sections aud memoirs of the years 1833, 1834, when I classed the Stiper Stones with the overlying deposits, I am at all events entitled to adhere to that view, now that M. Bar- rande also unites his ‘“‘ Zone Primordiale”’ with the overlying strata ; and since, fully aware of the distinction between its fossils and those which succeeded it in Bohemia, this eminent geologist continues to classify it with the Silurian System. We ail know how in those secondary and tertiary rocks which have been most examined there is often a marked discrepancy in the fossils of each succeeding stratum, so long as we examine a limited area only, and how such sharp separation and isolation of the former inhabitants of the seas vanishes when the same strata are followed over great distances. So is it when, quitting our insular area and extending our researches to Norway, we find strata of black schist, mineralogi- cally resembling the Lingula-flags or the schists of the Stiper Stones, and occupying the same place in the geological series, to be charged with some of the organic remains which in Britain are peculiar to that band, mixed up with species which are known in our own Llandeilo rocks. Again we observe that, as in the Stiper Stones of Shropshire, there is in Norway a vast underlying series of slates and quartzose rocks like those of the Longmynd ; so also are the beds into which the alum-schists pass upwards laden with many species of fossils which are with us in the Lower Silurian rocks of Llan- deilo age. The attempt to separate the alum-schists of Scandinavia from the overlying beds with which they are united in numerous natural escarpments is indeed forbidden on stratigraphical, lithological, and zoological grounds ; and as Linneeus and every subsequent explorer of Scandinavia have connected them, so I confide in the belief that they constitute, by their organic remains, the best base we have been able to trace of that which I call Silurian life. In comparing the Silurian rocks of Scandinavia and Russia with those of Britain, there is no feature by which the whole system is seen to be better.characterized in those countries than by containing in its central part a formation distinguished from the rocks above and below it by certain species of Pentameri, of which the Pentamerus oblongus and the P. lens are the prevailing types. Having satisfied myself, in my own country, that the lower portion of this formation is (as I always maintained) related by its organic remains to the Caradoc formation, and that the upper part of it is charged with a number of shells of the Wenlock age (though still intermixed with the peculiar Pentamert and a few Lower Silurian fossils), I have deemed it right to assign to the deposit a separate and intermediate place in the table of Silurian strata. Ihave named this formation ‘‘ Llandovery rocks,”’ reverting to that tract of South Wales which was originally described in detail, and where both the lower and upper members of the group, and their re- lations to the underlying and superjacent rocks, are clearly exhibited. It is the upper member only of these Pentamerus-rocks which is exhibited at May Hill, on the west flank of the Malverns, and also in 1857.] MURCHISON—SILURIAN ROCKS OF SCANDINAVIA. 51 the typical Silurian tracts of Shropshire, Herefordshire, and Radnor- shire. This upper band only is the May Hill Sandstone*. In parts of South Wales, where both members of the Llandovery rocks exist, there is usually, indeed (but in my opinion not always), a transgression between them, as traced by Professor Ramsay and Mr. Aveline, the lower member constituting over large areas the regular capping of the Caradoc or Bala formation, the upper or May Hill rock appearing to be usually the symmetrical base (as in Siluria proper) of the Upper Silurian group. As, however, the same species of Pentamerus, Atrypa, and Petraia, &c., occur in both these di- visions, 1 am induced by this community of type, and by the opinion of Mr. Salter, to consider the two bands as forming one natural- history province which connects the fauna of the Lower and Upper Silurian groups. Now, if we refer tu certain other regions, the truthfulness of this view is strikingly confirmed; since in them we can detect no such transgression or hiatus as occurs in Wales and the border-counties of England. Even in the neighbourhood of Girvan, in Scotland, fossiliferous Lower Silurian rocks of the Caradoc age seem to graduate upwards conformably into the Pentamerus-zone in question, containing not only the P. oblongus in profusion, but also the Atrypa hemispherica, with the Phacops Stokes of the Wenlock limestone; and thus leaving no doubt that we have there reached, as I formerly showed, the base of the Upper Silurian rocksy. In Norway, however, where the area under consideration is much larger, and where all the Silurian strata are clearly exposed in numerous convolutions in the different islets of the Bay of Christiania, there is, independently of all breaks caused by the intrusion of igneous rocks, a perfectly conformable succession from the Lower to the Upper Siluriant. There, as in Esthonia, the Pentamerus-zone is simply the central link of an unbroken Silurian chain; so local is the phy- sical disturbance in the Welsh region seen to be, when the whole surface of Northern Europe is explored. Whilst the Norwegian and Swedish sections are so valuable in showing the base of the System, the Esthonian order of the fos- siliferous strata is highly instructive in demonstrating the accord- ance of the Upper Silurian rocks with our own. The observations of M. Schmidt are, indeed, most valuable in placing before us, for the first time, a complete exposition of all the natural subdivisions of the Silurian series of so large a part of European Russia. In Esthonia, the approximation to the British succession, from the Llandeilo for- mation to the summit of the Upper Silurian, is very remarkable. Just as in Norway, England, and America, so in Esthonia the * See Proc. Geol. Soc. vol. ii. p. 13; Sil. Syst. p. 442, pl. 36. f. 13; Sedgwick and M‘Coy, Quart. Journ. Geol. Soc. vol. ix. p. 215; and Phil. Mag. 4th Ser. vol. viii. p. 301, &c. + Quart. Journ. Geol. Soe. vol. vii. p. 149. t See the diagram- section across the Territory of Christiania, Quart. Journ. Geol. Soe. vol. viii. p. 182. E 2 52 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6, transition-zone from the Lower to the Upper Silurian is the deposit laden with Pentameri, to which the name of Llandovery Rocks has been assigned, because it was long ago described by me at and around the town of Llandovery in South Wales. Whilst the Wenlock fauna is quite recognizable in Esthonia, as in Norway, the fossils of the highest zone of the former country, including many large Crusta- ceans (Hurypteride), with Lingula cornea and Trochus helicites, are strikingly characteristic of the Ludlow rocks. Such agreement between those remote foreign rocks and our strata of the same age is the more remarkable, when we consider the difference in thickness and the simplicity of lithological characters of the deposits in these northern countries, as compared with the vastly extended British types. The thousands of feet of diver- sified British Silurian rocks, whether slates, schists, shales, conglo- merates, sandstones, quartz-rocks, limestones, mudstones, with vast sheets of interstratified igneous rocks, are represented in the Baltic provinces of Russia by little more than one lithological character only. There, they are all closely united calcareous masses, any one of which has so great a resemblance to another, that, without the aid of Palzeontology, they could never be separated or distin- guished. The united Lower and Upper Silurian constitute, in fact, to use the language of Count Keyserling, “‘but a single volume of limestone of smail capacity and thickness, capable of division into leaves by that person only who is acquainted with their included fossils ;’ the whole series not exceeding 2000 feet, and all the strata graduating into each other by conformity of deposition. The interest, however, which attaches to the full illustration of these Northern European types of the oldest known fossiliferous rocks, does not terminate with the precise comparison between them and the British contemporary formations*. The same species, even, are found to prevail far to the westward in northern latitudes. Small as are the deposits, in vertical dimensions, both of Scandinavia and Russia, the very same succession of life which they offer is found to be persistent from those countries across the British Isles to the heart of North America. The vastly extended Lower Silurian rocks of the United States and Canada, and the enormously spread Upper Silurian of the Arctic Regions, are, like those of our own country, the absolute historical equivalents in time of the thin and simple series described on this occasion, and exhibit a vast number of forms pie nk identical with those I have enumerated. Other species, however, of Silurian typical genera prevail through- out the southern region of Europet. Already we know that the Silurian rocks of France and Spain, as illustrated and compared by * It is true, that in Russia there are fewer British species than in Sweden and Norway, but this is just what we might expect from the relative distances of those lands from our own country. t+ With additional researches, may not this Silurian type of Southern Europe and Siberia be found to have its equivalents in the central and southern parts of America? 1857.] MURCHISON—SILURIAN ROCKS OF SCANDINAVIA. 53 my distinguished associate, De Verneuil, have, however, many specific equivalents in the Lower Silurian rocks of that Bohemian basin which has been rendered classic through the works of M. Barrande. Count Keyserling further recalls my attention to the fact, that the Ural Mountains and Siberia fall ito the same category. This comparison, which was to some extent shadowed forth in the work ‘Russia and the Ural Mountains,’ published in 1845, has been stri- kingly confirmed by the researches of M. Griinewaldt into the cha- racters of the fossils of the eastern flank of the Ural Mountains near Bogoslofsk (lat. 61°). Again, M. Hofmann concludes his Siberian work in terms which show, that the parallel was suggested eleven years ago by Keyserling, as a result of his researches and comparisons ia the Northern Ural. In short, my coadjutor long ago directed notice to the fact, that, both in palzeontological contents and litho- logical characters, the Silurian rocks on the eastern side of the Ural Mountains were dissimilar to those of European Russia and Scandi- navia. Metamorphism alone, he always contended, could not explain this essential difference. The conditions of life, he added, had been one thing in the seas that occupied the Siberian area, and another in the waters which covered the low countries of western and southern Europe during the Silurian epoch. Since that time, this distinction of the varying faunas in contem- poraneously formed basins, separated from each other during the older paleeozoic period, has been abundantly developed by M. Bar- rande, whe has well shown the specific distinctions between the animals which inhabited respectively the regions of Bohemia and Scandinavia during the Silurian era. It is to the similarity, on the contrary, of the organic remains in the northern zone of Silurian rocks, which extends over so vast a space, that attention has been mainly directed on this occasion. Finally, let me state, that another chief object I have had, in bringing together the observations of Count Keyserling, Professor Schmidt, and M. Kjerulf, with comparisons of my own, is to demon- strate that in Scandinavia, as in Russia in Europe, Silurian rocks, both Lower and Upper, and copiously charged with characteristic organic remains, form a united and unbroken whole; and that, whether viewed paleontologically or geologically, they exhibit throughout those northern European regions, and in a very small compass, a natural-history system quite as complete, and more easily understood, than their much more expanded, highly varied, and dislocated equivalents in the British Isles. 54 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20 May 20, 1857. Lieut. H. Thurburn, of the 42nd Regiment M.I., and James Salter, M.B., F.L.S., 6 Montagu Street, were elected Fellows. Dr. H. B. Geinitz, Professor of Geology and Mineralogy in the Univer- sity at Dresden, was elected a Foreign Member. The following communications were read :— 1. Description of a small Loputopont Mammat (Pholophus vul- piceps, Owen), from the Lonpon Cuay, near Harwicu. By Prof. Owen, F.R.S., F.G.S., &e. [Prares Ti, TL PV.) CoNnTENTs. Introduction. Description of the skull. Comparison of the skull with that of other Mammalia. Description of the teeth. Affinities of the P. vulpiceps, as shown by the skull and teeth. Bones of the extremities :—Humerus; Femur; Tibia; Metatarsal bone. Remarks on the limb-bones. Introduction.—The remains of Mammalia from Eocene beds below the Binstead, Gypseous, and Headon or Hordwell series have hitherto been very scanty, and for the most part fragmentary ; whether from the clays of London and Bracklesham, or from the equivalent sands, conglomerates, or ‘‘ calcaires grossiers”’ of the Continent. The best evidence of Pachynolophus—a Lophiodont genus represented by species of small size, characteristic of the conglomerate of Mont Bernon (Pachynolophus Vismei, Pomel) and of the “ calcaire gros- sier’’ of Nanterre, Passy, and Vaugirard (Pach ynolophus Duvalii, Pomel),—consists of portions of upper and lower jaws, with teeth. The Dichobune suillum, Gervais, from the “calcaire grossier”’ of Passy, if it be a true Dichobune, rests upon a fragment of mandible with three teeth, and on a few detached teeth, with an astragalus. The genus Propaleotherium, Gervais (Paleotherium isselanum and Pal. aurelianum, Cuv.), is represented by similar fragmentary evi- dences of jaws and teeth from the lacustrine calcareous deposits at Buchsweiler, on the Lower Rhine, at Issel in the department of Aude, and at Argenton. The fossil eocene Monkey (Macacus | Hopithecus| eocenus) is known only by a small fragment of the under jaw with two teeth, and by a detached mandibular molar from the lower eocene sand of Suffolk. The best and most instructive mammalian fossil hitherto obtained from the London clay has been the portion of cranium with the molar series of teeth on which the genus Hyra- cotherium* was founded. But the subject of the present commu- nication is an entire skull with the complete dentition of both upper and lower jaws (Plates II. and III.) and a portion of the skeleton of * Trans. Geol. Soc. 2nd series, vol. vi. p. 203, pl. 24. 1857. ] OWEN—PLIOLOPHUS VULPICEPS. 53 the same individual, including the right humerus, Pl. IV. figs. 1-4, the right femur, 26. figs. 5 and 6, a great part of the left femur, the left tibia, Pl. IV. figs. 10-13, and three metatarsal bones, 26. fig. 14, apparently of the same hind foot. There have, also, been extracted recognizable portions of the pelvis, and some fragments of ribs; other fragments of ribs, vertebrze, and small bones are left in the matrix. The osseous tissue is silicified and partly impregnated with pyritic matter. This, therefore, is the most complete and instructive mammalian fossil of the age of the London Clay which has hitherto been dis- covered, and its study is replete with peculiar interest. In the course of last winter Mr. Colchester, the able and success- ful explorer and collector of organic remains of the eocene sands at Kyson, Suffolk, brought to the British Museum for my inspection one of the nodules of the Roman-cement bed of the London clay, near Harwich, from which nodule a portion had been chipped off, exposing on the fractured surface the faint outline of a skull, in size and shape like that of a fox. This appearance had arrested the further progress of the breaking- up of the nodule by the workmen, and the specimen came into the possession of the Rev. Richard Bull, M.A., Vicar of Harwich, by whom it was intrusted to Mr. Colchester for my opinion respecting the nature of the fossil, and by whose liberal permission the subse- quent operations were carried out, by which I am enabled to com- municate to the Society the following description of a new genus and species of perissodactyle pachyderm, for which I propose the name of Pholophus vulpiceps*, or Fox-headed Plioloph. The nodule presented the common subspherical form, and was about a foot in diameter. On closely inspecting the fractured sur- face, indications of other bones, besides the skull, were detected, and as the work of exploration proceeded, it plainly appeared that the car- case, or great part of the carcase, of a quadruped, about the size of a fox, had formed the nucleus round which the clay, modified by the chemical constituents of the dissolving and decomposing flesh, had become aggregated and consolidated. I have rarely broken up any septarian nodule of the London clay, which, thus altered, forms the chief material of the ‘ Roman cement,’ without detecting some organic relic which seemed to stand in the relation of a nucleus to such compact spheroid mass. The hardness and compactness of the matrix are extreme ; but, by the aid of the lapidary’s saw and the skilful and careful use of the chisel, Mr. Dew, by whom most of the Sewalik fossils in the British Museum were brought to their present instructive state, succeeded * Accomplished Palzontologists of France having included one of the elements of the term Lophiodon (Aogioy a small crest, ddovs a tooth) in the names of sub- genera of the Lophiodont family, as, e. g., in Pachynolophus, the same principle has guided to the choice of the term Pliolophus for the present accession to the family. By it I simply mean that it is more near to the Lophiodont type than its close ally the Hyracotherium. But the sooner a term becomes -an arbitrary sign the better. 56 PROCEEDINGS OF THE GEOLOGICAL socieTy. [May 20, in extricating entire the skull, and in relieving it from the surround- ing closely adherent matrix, and subsequently in working out the other bones above specified. Description of the Skull: Plate I1.—The skull is moderately long, slender, tapering gradually from the zygomatic region to the muzzle, Pl. II. fig. 2, with an unusually straight upper outline, from the occipital crest to the end of the nasal bones, Pl. II. figs. 3 and 4. The bony rim of the orbit, fig. 3, ov, is incomplete behind for an ex- tent of about one-fifth of its circumference. The occipital region is triangular, bounded by a strong occipital crest, 3, which is continued on each side into the upper border of the zygomatic arch, Pl. II. fig. 3, 27, and, by the middle of its upper part, with a parietal crest, 7. This latter, rismg clearly above the calvarian surface, Pl. IT. fig. 4, to an extent of from one to two lines, advances forward one inch nine lines, and bifurcates, subsiding to the level of the frontal surface, 11, each division diverging and curving outward, with the convexity forward, to the post-frontal process, 12, which projects backward and a little downward, terminating freely about 8 lines above the zygoma, 26, 27. The interorbital part of the frontal region, 70. 11, is nearly flat at its middle, and bends gently down on each side to the superorbital border. The long nasals, 15, form the rest of the upper surface of the skull, which is at first mo- derately convex transversely, and is then grooved along the mid-line to the free ends of the nasals. These bones are 13 lines across their base, and gradually contract to a breadth of 7 lines, which they re- tain for the terminal inch of their extent. The zygomatic arch, springing outward and a little forward from its hinder root or pier, Pl. IT. fig. 3, 27, describes a slight sigmoid flexure, first convex then concave upward, where it forms, 26, the lower border of the orbit; this border extends some 4 or 5 lines further outward than the upper border. There seems not to have been a zygomatic process rising toward the postfrontal, 12, but a mere convexity of the upper border of the zygoma behind the orbit. The extreme vertical diameter of the zygoma is 4 lines. The cerebral part of the cranium forming the inner wall of the temporal fossa shows the greatest expansion of the brain at about the middle of that fossa, behind which, on both sides, the concavity exhibits several irregular indentations and some vascular perforations. There is no superorbital foramen ; a very feeble indent of the base of the post- orbital process is the sole indication of the place of issue of the super- orbital nerve. The anturbital foramen, Pl. IJ. figs. 3 and 4, a, about 14 line in diameter, is situated 9 lines in advance of the orbit, and between 2 and 3 lines above the alveolus of the second premolar. The vertical outer plate of the maxillary, 21, slightly expands where it forms the sockets of the small canine,c. The sides of the bony nostril are almost straight, extending from a distance of 5 lines from the free ends of the nasal, 0, obliquely downward and forward, and being formed by the premaxillary bones, Pl. II. fig. 4, 22: the ver- tical extent of the aperture is about 10 lines. 1857.] OWEN—PLIOLOPHUS VULPICEPS. 57 The mandible, 29, 30, had been dislocated, about 4 lines in advance of its place of articulation, prior to the consolidation of the surrounding matrix, by which it is now fixed with the lower teeth to the same degree in advance of their correspondents above, as in PI. II. fig. 3. This dislocation enables the flattened surface of the major part of the glenoid cavity to be brought into view, at g, fig. 3. In figure 4 the mandible is figured as in its proper position. The ascending ramus of the mandible developes a short recurved coronoid process, Pl. II. fig. 4, 7; below this and the condyle d, it expands, gradually extending backward as it descends from the condyle, describing an irregular convex curve as it passes into the under border, and forming a broad angular plate, 29, for the implant- ation of the pterygoid and masseter muscles. The fossa indicating the insertion of the temporal muscle, fig. 3, ¢, is limited to the upper half of the ascending ramus, where it is bounded by a curved line or bank continued downward and forward from the outer part of the condyle: the anterior border of the depression subsides upon the part of the jaw which extends outward from the alveolus of the last molar. The outer side of the horizontal ramus of the mandible is lightly convex : the lower border, continued from the broad rounded angle, is at first gently concave, then as slightly convex. The ramus very gradually decreases in depth to the first premolar, below which the symphysis begins, Pl. II. fig. 1, s,z. Here the mandible is a little compressed and again expands slightly to form the alveoli of the canines, ¢, and incisors, 2, 1,2,3. The line of the symphysis rises very gradually to the incisive border, s 2, figs. 1 and 2, Pl. II. The following traces of sutures are unmistakeable : the squamous, Pl. II. fig. 3, g, continued forward from the irregular depressions on the side of the cranium, at first straight, then with a downward curve ; the straight part is 9 lines below the sagittal crest, 7: the interfrontal suture, Pl. II. fig. 2, 11, continued into the mternasal one, 26. 15, along the midline of the facial part of the skull: the fronto- nasal suture, 726. f, describes a slight sigmoid curve, as it extends transversely outward and downward to the lacrymal, 7s, fig. 3, Pl. IT. The suture connecting this bone, 73, to the maxillary, 21, and malar, 26, Shows that its facial plate is about 4 lines im vertical, and 3 in fore-and-aft, diameter. "The malar, 26, forms the lower half of the fore part of the orbit ; the anterior end of its almost horizontal suture with the squamosal, 27, begins just below the postorbital process. The naso-maxillary suture, Pl. IT. figs. 3 and 4, m, is nearly straight, 1 inch in length ; its continuation by the naso-premaxillary suture n is about 6 lines in extent ; but this part of the lower border of the nasal, 12, is slightly convex downwards, with a corresponding curve of the suture. The maxillo-premaxillary suture, p, is almost a straight line, parallel with the lateral border of the nasal aperture. The following are admeasurements of the skull of the Pliolophus, _ with some comparative admeasurements of that of the Hyracothe- rium :— 58 PROCEEDINGS OF THE GEOLOGICAL society. [May 20, Pliolophus | Hyracotherium vulpiceps. leporinum. in. lines. in. lines. Diength. of Sg) cs pesne sniescnt ane siecnts sano steerer Extreme breadth of skull, at the zygomata dean ase Extreme breadth of cerebral part of cranium ...... Breadth across postfrontal processes ............+0+08. Breadth of upper jaw opposite first premolars ...... Vertical diameter of skull opposite first true molar Vertical GiameterOf OLDIE cinessesuscaciesrecncesasesee From occipital crest to fore part of orbit ............ From occipital crest to fore part of temporal fossa From the fore part of the orbit to the end of nasals Dene el Mia GiDle, oe saccas sane sesentne cnsanncen ope ens Length of symphysis mandibule ..................... Breadth Of ascending TAaMUS ........-cecssccnesssseoes Height of ascending ramus at the condyle ......... Height of ramus below first true molar ............ Extent of molar series, upper jaw ............sseeeeees Extent of molar series, lower jaw .............seee0re- Extent of three true molars, upper jaw ............ Extent of the four premolars, upper jaw ............ Extent of three true molars, lower jaw ............++. Extent of the four premolars, lower jaw ............ |= —— Se —_ —_ —_ — SOOM KH SCKNTODORWNHWOUR UO OWNS SS SON ORK KKH RNNN OK ORK bd wu bol bol — — Comparison of the Skull.—The extent and well-defined boundary of the temporal fossze by the occipital, parietal, and post-frontal ridges, and their free communication with the orbits, give almost a car- * nivorous character to this part of the cranium of Pliolophus: but, as in the Hog, Hyrax, and Palzeothere, the greatest cerebral expansion is at the middle and toward the fore part of the fosse, with a con- traction toward the occiput ; the brain-case not continuing to enlarge backward to beyond the origin of the zygomata, as in the Fox. The zygomatic arches have a less outward span, especially at their hinder pier, 27, than in the Carnivora. In this part of the cranial structure Pliolophus resembles Paleotherium more than it does any existing mammal ; but the post-frontal processes are longer and more inclined backward. The incompleteness of the orbit occurs in both Anoplothertum and Paleotherium, as in Rhinoceros, Tapirus, and the Hog-tribe; but, in the extent of the deficient rim, Plioluphus is intermediate between Paleotherium and Tapirus. The orbit, Pl. II. fig. 3, ov, is not so low placed as in Paleotherium, Tapirus, and Rhinoceros, nor so high as in Hyraz or Sus. The straight upper contour of the skull is like that im the Horse-tribe and Hyrax, and differs from the convex con- tour of the same part in the Anoplothere and Paleeothere. The size of the antorbital foramen, PI. II. figs. 3 and 4, a, indicates no unusual development of the muzzle or upper lip. In the conformation of the nasal aperture by four bones (two nasals, 15, and two premaxillaries, 22), Pliolophus resembles the Horse, Hyrax, Hog-tribe, and Anoplo- there, and differs from the Rhinoceros, Tapir, and Paleeothere, which have the maxillaries, as well as the nasals and premaxillaries, enter- ing into the formation of the external bony nostril. The ungulate and herbivorous character of Plolophus is most 1857. | OWEN—PLIOLOPHUS VULPICEPS. 59 distinctly marked by the modifications of the lower jaw, especially by the relative dimensions of the parts of the ascending ramus which give the extent of attachment of the biting (temporal, £) and grind- ing (masseteric and pterygoid, 20) muscles respectively. In the shape of the mandible Pliolophus most resembles Tapirus among existing mammals, and the Paleotherium among the extinct ones in which that shape is known. Unfortunately no mandible of a true Lophiodon has yet been found so entire. As far as the portion of the skull of the Hyracotherium leporinum permits the comparison to be made, there is a close general resem- blance between it and Pliolophus ; but the skull of the Hyracothere is broader, at the orbital region, in proportion to the length of the antorbital or facial part*. The orbits are both absolutely and rela- tively larger ; they are also rounder and have a lower position. The straight upper contour of so much of the skull of the Hyracothere as has been preserved, the size and position of the antorbital fora- men, the course of the maxillo-premaxillary suture, and the forma- tion of the bony nostril by the nasals and premaxillaries exclusively, are further indications of the affinity of Hyracotherium to Plio- lophus. This affinity is decisively shown by the more important characters derived from the dentition. Description of the teeth of Pholophus: Plate III.—As in the Hyracotherium, and, indeed, as in almost every species of Eocene qua- druped yet discovered, the Pliolophus presents the type-dentition of the placental Diphyodont series, viz. :— « 33 — 4—4 3—3 ¢ 3-9 Cf 2 ph gaa ga 44. The incisors, Pl. II., 21, 2,3, are preserved in the lower jaw with marks of attrition on their crowns demonstrating corresponding teeth of the same number, 6, and of similar size, in the upper jaw, from which the alveolar part of the premaxillaries had been broken away. The lower incisors, Pl. II. fig. 1, 71, 2, 3, form a semicircle termi- nating the slender slopmg symphysis mandibule, s, and projecting parallel with it, so as to be almost procumbent, Pl. II. figs. 3 and 4, 7. Their crowns present the common wedge-shaped form, with the trenchant border obliquely beveled off, and the more so from the first, 21, to the third, 23: they slightly decrease in size, or at least in length of crown in the same course ; but the outer incisor, 7 3, is not so small relatively as in the Tapir. The degree of attrition to which they have been subject produces a certain breadth of the trenchant border. The canines, 20. ¢, are small in both jaws: only the crown of the right lower one, Pl. II. fig. 3, c, is entire: it is about 4 lines long, in the form of a slender cone, inclined a little forwards, with the - front border convex, the hind one more nearly straight. The lower canine is separated by an interval equal to its own basal breadth, viz. about 2 lines, from the outer incisor, and by an interval of 5 lines * Op. cit. pl. 21: fig; 2. 60 PROCEEDINGS OF THE GEOLOGICAL society. [May 20, from the first premolar. In the upper jaw the canine is separated by a rather wider space than in the lower jaw from the incisors, and by a rather narrower space from the premolars. In thickness of base and, apparently, in length and shape of crown, the upper canines resembled the lower ones. The premolars, p, and molars, m, form a continuous series on each side of both jaws; except that a space of about a line intervenes between the first and second premolars in the lower jaw. The premolars increase in size and complexity to the fourth, which nearly equals that of the true molars. The last of these, m 3, in the lower jaw, presents a third lobe. In PI. II. fig. 3, the premolars of the upper jaw are marked 1, 2, 3,4: the true molars of the lower jaw are marked 1, 2,3: the dislocation of the jaw carries these one tooth in advance. Inthe upper jaw, the first premolar, Pl. II. fig. 3, pi, presents the common subcompressed conical shape, with the base of the crown swelling out below the fangs, and the protuberant part continued along the outside of the middle part to the apex of the cone ; on each side of this promimence the crown presents a de- pression; and the surface, though polished, is broken by a few irre- gular longitudinal indentations, which give the enamel a slightly wrinkled character. : The second premolar, p 2, resembles the first; but is somewhat larger, especially thicker, and with the front and back parts of the base more produced; an outer longitudinal groove near the summit of the cone indents it deeply. The third premolar, p 3, has two cones on the outer side, and an anterior basal talon ; from this a slight ridge is continued upon the outer part of the anterior cone: the whole outer base of the poste- rior cone is girt by a similar low cingulum, continued into a rudi- mental talon behind. The crown expands posteriorly, and its work- ing surface is increased by an internal ridge, and the valley dividing it from the two outer cones. In the fourth premolar, the crown, Pl. III. figs. 1 & 2, p 4, with an increase of thickness, presents greater complexity: the cmgulum is uninterrupted along the outer side from its anterior well-developed talon, c', to the back part where the ridge, ¢, represents the talon. The two outer cones resemble those of the true molars; but there is only one inner cone, and the crown of pa differs accordingly from that of m 1, in being triangular rather than square. A ridge, 7, is continued from the interspace between the anterior talon, c', and the outer anterior lobe obliquely inward and backward to the inner lobe, swelling into a small tubercle at the middle of its course; a lower rising, hardly to be called a tubercle, intervenes between the inner cone and the outer posterior cone. The cingulum forms a well-marked ridge, ¢, along the back part of the crown, and is con- tinued more feebly round the base of the inner lobe, with a brief in- terruption at its most prominent middle parts: beyond this the cingulum is continued into the anterior basal ridge, which expands into the small antero-external basal tubercle, ¢'!. The fourth upper premolar is implanted by two external and one internal roots. 1857. | OWEN—PLIOLOPHUS VULPICEPS. 61 The first molar, Pl. III. fig. 2, m1, shows, as usual, a greater amount of attrition than the preceding premolar : its grinding sur- face presents four low thick cones, two internal as well as two ex- ternal : each external cone is connected with its opposite internal one by a low ridge extending from the fore part of the external to the middle of the internal one, and swelling into a tubercle, r and s, at the middle of its oblique course. The cingulum, ¢ c, seems to be continued uninterruptedly round the crown of this tooth, thickest at the fore and back part, and at the interspace of the inner lobes; and developing the small accessory antero-external tubercle, c!. The outer lobes are connected together by a low plate, internal to the cingulum. The degree of attrition to which this tooth has been subject has exposed the dentine, which is surrounded by a belt of thick enamel upon the summits of the four principal lobes and of the intervening tubercles. This molar is implanted by two external roots and by a broad internal one, longitudinally indented at the middle, and which may divide where it lies deeper in the jaw. The second molar, m 2, is similar to, but rather larger than, the first ; and the tubercle on the oblique ridge connecting the two hinder lobes is less developed. The cingulum, c, is obliterated on the inner side of the posterior lobe. The implantation of the tooth is like that of m1. The last molar is rather narrower behind than m 2; the tubercle, 7, on the anterior of the oblique connecting ridge is smaller: that on the posterior ridge is almost obsolete. The hinder of the two inner cones is relatively less and lower than in m1 and me, and is searcely defined from the oblique ridge s; the cingulum is inter- rupted at its inner base: the talon, ¢, formed by the back part of the cingulum is better marked than in the other molars. In all these teeth the enamel is wrinkled by longitudinal wavy impressions. Of the mandibular teeth, Pl. IV. figs. 4, 5 & 6, only the molar series remain to be described. The first premolar, Pl. II. figs. 3 & 4, p 1, is small, simple, sub- compressed, conical, like the one above ; but it stands apart, an in- terval of about half its breadth dividing it from the second premolar. This tooth, 26. pi, of rather larger size, has a similar form, but with a better-marked hinder talon. In the third premolar, Pl. III. fig. 6, ps, the talon, ec, is developed into a second lobe, which is lower than the first. The first or front cone, a, shows a small anterior or antero-internal talon, and the apex of the cone is cleft ; a ridge from the inner division, 6, being con- tinued obliquely down to the inner angle of the base of the low hinder cone, c. In the fourth premolar, fig. 6, p 4, the division and development of the anterior lobe has proceeded to establish a pair of cones, one external, a, the other internal, 6, connected anteriorly by a basal ridge, in front of which is the fore part of the cingulum. The low posterior lobe, c, shows the rudiment of a second internal cone, d. The cingulum is developed at the fore part, and feebly between the 62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20, two outer cones. The posterior one, c, is connected by a ridge, which advances inward and forward, to the interspace between the anterior pair of cones. The first molar, m1, with an increase of size over the last pre- molar, also shows an equal development of both fore and hind pair of lobes; the summits of the two outer lobes are more abraded than those of the two imner ones, and the dentine is exposed in each. The same oblique ridge is continued from the fore part of the postero- external lobe to the interspace between the anterior pair: the cin- gulum is not developed upon the internal part of the tooth, but it is upon the external part, and especially upon the anterior lobe: pos- teriorly it forms a kind of low talon wedged into the interspace of the hinder pair of lobes. The second molar, m2, shows an increase of size; but its chief and most interesting modification is the development of a tubercle, e, between the two anterior lobes, making three cones on the same transverse line, and thus repeating the character of the molar tooth above. The oblique ridge from the outer and hinder lobe, c, abuts against the intermediate anterior tubercle, e. The inner surface or plane of the inner and hinder cone, d, inclines as it extends forward toward the middle of the crown: the fore parts or prolongations of the himder cones thus converge as they pass forward toward the _ middle of the crown. The cingulum extends from the back part of the crown along the outer side to the fore part. Both this and the preceding molar are implanted by four roots. The third molar, m 3, is distinguished by its greater fore-and-aft extent, due to its additional or third lobe. The ordinary two pairs of cones resemble those of the preceding molar, but the intermediate tubercle between the anterior pair is reduced to a short connecting bar. The hind lobe appears to have been divided mto two small cones, but this part of the tooth was fractured in the attempt to remove the very hard and adherent matrix. I beg to express my obligations to the accomplished artist, Mr. Ford, for the pains which he has bestowed im attainmg the utmost accuracy in the figures above referred to. Affinities of the Pliolophus vulpiceps as shown by the skull and teeth.—Before proceeding with the description of the other parts of the little quadruped which have been extricated from the septarian nodule, it may be convenient to record here the deductions as to the nature and affinity of the Pliolophus vulpiceps which may be drawn from the skull and teeth. The form of the articular surface for the lower jaw, and above all that of the mandible itself, demonstrate the ungulate and more or less herbivorous nature of Pliolophus. Amongst recent non-rumi- nant Ungulates, Tapirus offers the nearest resemblance in the dispo- sition and form of the zygomatic arch, and in the general form of the lower jaw : amongst the extinct Ungulates, Palgotherium most resembles Pliolophus in the same parts of the skull, with a nearer approach than the Tapir makes, im the production of the nasal 1857. ] OWEN-—PLIOLOPHUS VULPICEPS. 63 bones ; but in this character, and in the important one of the more simple formation of the nostril, Anoplotherium offers a closer re- semblance to Pliolophus. In the almost straight upper contour of the skull, the Horse and the Hyraz, amongst existing Ungulates, resemble Pliolophus, and both these Perissodactyles add the corre- sponding character of the juncture of the premaxillaries with the nasals, which Pliolophus presents in common with the Anoplothe- rioids. But the orbit is circumscribed by bone in the above-cited existing Perissodactyles, whilst it opens behind into the temporal fossa in both Anoplotherium and Paleotherium, as in Pliolophus. Microtherium resembles the small Musk-deer in the entire bony frame of the orbit. The form of the skull in Lophiodon proper has not yet been ascer- tained ; but the comparative simplicity of the premolars in Pliolo- phus, and the configuration of the surface of the upper true molars, especially the last, Pl. III. fig. 2, m3, demonstrate that the present small Hocene quadruped has the nearest affinity to the Lophiodont family, amongst the known extinct and recent members of the class. To a Lophiodont mammal, indeed, of the same size from the marls of the ‘ Calcaire grossier’ in the vicinity of Paris (Lophiodon lepto- gnathum, Gervais *, Hyracotherium de Passy, De Blainville +), on which M. Pomel subsequently founded his subgenus Pachynolophus, I felt most inclined, at first, to refer the Plhiolophus; and it was in the prosecution of this comparison that I determined to sacrifice the entireness of one side of the fossil skull, in order to obtain a more complete and satisfactory view of the grinding surface of both upper and lower molars than could otherwise be got. For the comprehension of the followmg comparison, PI. II. figs. 3 & 4, and PI. III. fig. 2, of the present memoir should be examined by the side of the views of the upper molar teeth and of the right mandible and teeth of the Pachynolophus (Lophiodon) Duvalii, Pomel, which M. Gervais has given in his excellent ‘ Zoologie et Paléontologie Francaise,’ 4to, pl. 17. f. 1, la & 2. Unfortunately the grindmg surface of the upper molars only of Pachynolophus has been figured, and with these I proceed to compare the same teeth of Pliolophus vulpiceps. I may premise that the generic or family character of the upper molars in Lophiodon is the development of the outer wall of the true molars and last premolar into two cones, and by the continuation, therefrom, in the true molars, of two oblique ridges which thicken and rise into rather smaller and lower cones on the inner side of the crown. In the last premolar the oblique ridge is continued only from the anterior of the two outer cones, and expands into a single large cone forming the inner half of the crown. In Pachynolophus as in Pliolophus the oblique ridges are lower at their commencement, in comparison with their inner terminal cones, than in Lophiodon, and accordingly a degree of attrition * Comptes Rendus de |’Acad. des Sciences, Paris, vol. xxviii. p. 547. + Ostéographie, Lophiodonts, p. 190. pl. 2. 64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20, which affects the enamelled summit of the whole ridge in Lophi- odon, abrades only the summits of the inner cones in Pachynolo- phus and Pliolophus; moreover the oblique ridges in Pachynolo- phus appear from M. Gervais’s figure to dilate a little in breadth at their beginning, but this swelling is not so marked and circumscribed as in Pliolophus, and consequently an intermediate island of enamel, as at r and s, Pl. III., between an outer and inner cone, is not pre- sented in any of the molars of Pachynolophus, although the first of these, m 1, mm the specimen figured by M. Gervais, has been as much worn down as in the corresponding molar of Pliolophus. In this respect Plolophus presents the next transitional step in the passage from the type-dentition of Lophiodon to that of Hyraco- therium, in regard to the modification of the working surfaces of the molar teeth. The hinder half of the last molar, m 3, presents a minor area, as in Pachynolophus, and a more simple configuration ; the ridge from the postero-internal cone being simple, not expanding into an acces- sory tubercle. M. Gervais calls attention to the seeming quadrilobate character of the outer side of the crown in the true molars of Pachynolophus, produced by the development of the cingulum into a tubercle at the fore and back part of that side of the tooth. Pliolophus resembles Pachynolophus in the tubercle at the fore part of the outer wall, but the cingulum is not so expanded at the back part as to give the appearance of a fourth cone. In this respect Pliolophus resembles Lophiodon proper. In regard to the lower jaw, the lower contour of the symphysis is in the same line with that of the lower border of the ramus in Pa- chynolophus, and the symphysis with the incisor teeth are more pro- cumbent even than in Pliolophus: the diastema between the pre- molars and canine is twice as long, and the consequent modification of the mandible led M. Gervais to propose the specific name Jepto- gnathum for the small Lophiodont of the ‘ Calcaire grossier,’ which M. Pomel had previously dedicated to his friend M. Duval. But a distinction of more decided generic importance between Pachyno- lophus and Pliolophus is presented by the absence of p 1 in the former, which reduction of the number of the molar series* to six, M. Gervais regards as normal, and assigns as the chief generic di- stinction from Lophiodon ; adopting in this respect the conclusions of M. Pomel. The demonstration, which the rare perfection of the skull and teeth of the Pliolophus vulpiceps from the London Clay affords, of the retention of p 1 in the lower jaw, and consequently of the typical dental formula, justifies the same generic distinction of Pliolophus, as of Lophiodon proper, from the small Lophiodont called Pachynolophus by Pomel. ‘The generic distinction of Plho- lophus from all previously known Lophiodonts is more decisively established by the singular modifications of the grinding surface of the lower molar teeth. This surface, in Pachynolophus, seems not to have been figured : M. Gervais describes it, in the penultimate molar (m2), as present- 1857. ] OWEN-—~-PLIOLOPHUS VULPICEPS. 65 ing “two transverse eminences connected by a diagonal crest* ;” and such is described as the type of the lower true molar teeth in Lo- phiotherium + and Tapirulust. This is, in fact, the structure of the lower molar teeth in Lophiodon proper, and that by which it so nearly resembles the existing Tapirs. Pliolophus differs from all previously known Lophiodonts by the division of the part of the tooth answering to the “ colline trans- verse’ into two distinct cones, Pl. III. fig. 6, a, 6 and ¢, d; and the penultimate molar, m2, more especially differs from that tooth in all hitherto known eocene or later forms of hoofed Mammals, in having a third cone, e, interposed between the two anterior cones, and thus exhibiting three cones on the same transverse line, as in the upper molars ;—a structure which we have hitherto seen only in the small mammal of the Lower Oolite described under the name of Stereo- gnathus ooliticus §. I expressed my regret, at that period, when I could only cite the upper molars of Hyracotherium and of a few other eocene Ungulates as manifesting the three transverse cones, that the structure of the lower molars in Hyracotherium was then unknown. As the Pliolophus, though in some respects intermediate between the Lophiodon and Hyracotherium, has a closer affinity to the latter, we may, with some confidence, regard the modifications of its lower molars as significant of those that the same teeth of Hyracotherium will present when found. And the unlooked-for confirmation of my expectation of some further illustration of the affinities of Stereo- gnathus by the lower molars of Hyracotherium, through the now acquired knowledge of the structure of those in the nearly allied Pliolophus, adds, in the same degree, probability to the inference which was founded upon the resemblance between the lower molars of Stereognathus and the upper ones of Hyracotherium. In offer- ing this remark, however, I am quite sensible how uncertain any in- ference from a single lower molar is shown to be by the degree of resemblance in the structure of the lower molar teeth which exists in Tapirus, Macropus, Lophiodon, Dinotheritum, and Manatus, and, again, in those of Hippopotamus and Halitherium. The reference by Cuvier of detached teeth of the Halitherium to the genus Hippo- potamus, and of detached teeth of Dinotherium to the genus Tapirus, just and exact as were these references, viewed as expressions of the correspondence detected by a comparison of the fossil with the recent teeth, ought to warn us against placing too much confidence in den- tal characters, exclusively, as proofs of the closer degrees of deter- mination which Cuvier has shown must depend upon an empirical study of coincidences, rather than on the rational deductions from correlations. The same caution I now feel to be instructively reiterated by my reference of the Hyracotherium, on the ground of similarity of modi- * “ A deux collines transverses reliées par une créte en diagonale.” Paléonto- logie Frangaise, descr. of pl. 17. t Ibid. pl. 11. f. 10-12. t Ibid. pl. 24. § Quart. Journ. Geol. Soc. vol. xiii. Part I. February 1857, pp. 1, &c. pl. 1. VOL. XIV.—PART I. LD, 66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20, fication in the grinding surface of its upper molars, to the same secondary group of Ungulata as includes the Cheropotamus. Most comparative anatomists who have studied the unique evi- dences of that old eocene genus, since my description of them, have arrived at and have recorded the same conclusions*. The only dissentient from them was Mr. H. N. Turner, jun., a most promi- sing and acute naturalist and anatomist, who died too soon for the interests of science. In a very able and characteristic paper “‘ On the Evidences of Affinity afforded by the Skull in the Ungulate Mammalia +,” Mr. Turner points out the basal expansion of the nasal bones, the absence of the superorbital foramen and groove, and the slightly marked depression for the origin of the obliquus inferior oculi, within the orbit, as indications of the perissodactyle affinities of the Hyracotherium: he, also, most acutely discerned in the rudimentary oblique ridges upon which the small intermediate tubercles were developed in the molar teeth rudimenta] homologues “of the bent transverse ridges in the Rhinoceros, Tapirus, Paleo- therium, and other allied genera;” but the degree of resemblance of the molars to those of the Anthracotheria and Cheropotami was such as led Mr. Turner, in regard to the question of the artiodactyle or perissodactyle affinities of the Hyracotherium, to admit, “to whichever group, then, this little animal be referred, the teeth will present marked exceptional characters, and, therefore, it becomes more necessary to seek for further evidence f.”’ This evidence I believe to be now afforded by Pliolophus, on the ground of the following illustrations of its close affinity to Hyraco- therium. Like that genus, its upper true molars exhibit the modification of the Lophiodont type of dentition in the more circumscribed and better-developed enlargement of the middle of the connecting oblique ridges: it also shows the more simple structure of the last premolar by the same non-development of the postero-internal cone. Hyra- cotherium differs from Pliolophus in the more distinct development of the intermediate tubercles, especially of the second or posterior one in pa: the cingulum girts the crown uninterruptedly in the true molars and last two premolars. AHyracotherium differs, also, in the wider interval between the first and second premolar. It may be questioned whether these differences are of generic importance, or whether, with those before pointed out in the con- figuration of the skull, they may not merely indicate another species of this genus which seems to be peculiar to our London Clay. In resolving this question I have been influenced by comparing the * De Blainville, Ostéographie des Anthracotheriums et Chceropotames, fasc. xxi. p. 194. Hyracotherium described and figured “ d’aprés un platre assez bon, envoyé A la collection du Muséum, par M. R. Owen.” Gervais, Summary of Ungulata observed in France :— 11. Caa@roporamina. Entelodon, Cheropotamus, Hyracotherium, Pal. France. descr. of pl. 36. p. 6. + Ann. and Mag. Nat. Hist. Dec. 1850, 2nd ser. vol. vi. p. 397. t Loe. cit. p. 408. 1857. | OWEN—PLIOLOPHUS VULPICEPS. | 67 degree of difference in their dental characters with that which has influenced MM. Pomel and Gervais in subgenerically separating Pachynolophus from Lophiodon ; and by the fact of the mandibular teeth of the Hyracotherium leporinum bemg yet unknown. Lophiodon, Pachynolophus, Pliolophus, and Hyracotherium seem thus to form so many subgeneric modifications of the same natural family of Perissodactyle Ungulates ; and in the modifications of their dentition, especially in the comparative simplicity of their premolars as compared with those of the subsequently introduced Paleotheria, and in the progressive approach to the molar type of the Cheero- potamoids made by Pliolophus and Hyracotherium, they exemplify the tendency toa closer adherence to the general ungulate type. The third trochanter on the femur of the Pliolophus, Pl. IV. fig. 5, ¢, and the association of three metatarsals, in one portion of the matrix, fig. 14, which appear to belong to the same hind-foot, confirm, how- ever, the essentially perissodactyle affinities of that genus, and, there- fore, of its close ally the Hyracotherium. In stating that these modified Lophiodonts are the most artio- dactyloid of the Perissodactyles, no particular hypothesis is advo- cated : there can be but one inference from this and the numerous analogous facts that have already been made known. So, likewise, in regard to the typical character of dentition, as manifested by the number and kind of teeth, we find in this last eocene mammal which has come to light a repetition of that remarkable adherence to a more general mammalian character. The older Oolitic Mammals exemplify a tendency to a type of dentition of a still higher gene- rality than the Mammalian class, as, for example :— Mammalia of which the dentition resembles the general vertebrate type by the back teeth exceeding 7 in number :— Genera. Formations. Thylacotherium .......- Lower Oolite. Spalacotherium ...... Upper Oolite DPFECOMGHOM © ao shsysi's ais 305: Upper Oclite f Purbeck Mammalia resembling the Mammalian diphyodont type in the dental formula of i! 4—4 f= 3—3 =” Z = Se ees es or p — = and m = = 44, Genera. Formations. Paleocyon 22.) 8... Sables de Bracheux (or somewhat older). Coryphodon.......... Plastic clay. Pachynolophus ...... Calcaire grossier moyen. Lophiotherium........ Marnes lacustres d’Alais (Gard). Photons, 3 2c ae London clay. Hyracotherium ...... London clay. Paleotherium........ Paris gyps. Anoplotherium........ Paris gyps. Anchitherium ........ lLignites de la Débruge, prés Apt. ICrOGUNe! bs5 38.2 Pet Binstead. FZ 68 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20, Genera. Formations. Xiphodon............ Lignites de la Débruge. Mi chadon).... ove byl Hordwell. Microtherium ........ Marnes calcaires lacustres, Puy du Dome. Amphitragulus ...... Marnes lacustres en Velay. Amphimeryx Lignites de Débruge. Dopeatherium, nina. Miocéne d’ Eppelsheim. Chalicotherium .... Miocéne d’ Eppelsheim. Aphelotherium........ Marnes calcaires de Barthélemy. Anthracotherium...... Marnes miocénes de Moissac. Hyopotamus Binstead and Hordwell. Anchilophus......... Bothriodon .... Paleocherus .. Cheropotamus...... Cheeromorus.........«- Poébrotherium.......- Calcaire grossier de Batignolles. Miocéne de Moissac. Calcaire lacustre de Cournon. Paris gypsum, and Binstead. Calcaire lacustre, Sansan. Eocene (upper ?), N. America. Hippohyus ....... Miocene, Sewalik Hills. Hippotherium ........ Miocéne d’Eppelsheim. Hipparton oe e25 Marnes fluviatiles de Cucuron. Heterohyus.......... Miocene, Sewalik Hills. PEE LOR OI 3a: auton cpr Lignites de Soissonnais. Ey @UOd ON, je 2i.< Nook oF. Eocéne supérieure du Gard ; Hordwell. PECROION 3 5 ch 20% aeys Lignites de Débruge: ATLOCHOR: O2hiig > oneiasis Eocéne inférieure 4 la Vére. Galethylaw: 6 tidy ssi Paris gyps. VA PhCyOn . . ain.s\9 4 eee Miocene de Sansan. Cherotherium........ Miocéne du Bourbonnais. Rhagatherium........ Eocene of Mauremont, Switzerland. All general rules in organic nature have their exceptions, and differ in that respect from morganic phenomena, in regard to some of the general laws of which no exceptions have been as yet dis- covered. I shall, on a future occasion, discuss the value of the exception to the inference from the body of faets above cited which has been adduced from the Plagiaulax *, and conclude the present paper with some remarks on the bones of the limbs of Pliolophus. Description of some of the Bones of the Extremities." Humerus. Pl. IV. figs. 1 to 4.—The humerus, from the right fore limb, mea- sures 4 inches in length. The convex articular surface of the head of the bone, Pl. IV. fig. 3, is subtriangular in shape, rather flattened above towards the outer side. The great tuberosity is of equal breadth with, but rises above, the articular head. It is slightly grooved obliquely near its outer part, but is not so widely or deeply notched there, as in the Tapir or Hyrax: it terminates by a single convexity. The small tuberosity is not quite so large relatively as in the Tapir and Hyrax, but it is situated, as in them, * Quart. Journ. Geol. Soc. vol. xiii. p. 276. 1857. | OWEN—PLIOLOPHUS VULPICEPS. 69 at the fore and inner part of the articular head, and not so low down as in the humerus from the “terres noires du Laonnais,”’ ascribed to Lophiodon by Cuvier *. The deltoid surface is short : a smooth oblique tract separates it from a second low oblique (pectoral) ridge ; the shaft of the bone rapidly contracts below the head, where it is not so compressed or so broad from before backwards, as in Paleotherium; it is thicker transversely than in Hyracotherium. The supinator ridge begins at about the lower third of the bone, is moderately sharp for about 9 lines, and then subsides into a rather rough flattened surface above the inner condyle; it is very slightly produced. The bone is perforated above the lower articular surface ; this surface has one depression and two prominences, as in the Perissodactyles. The general shape and proportions of the bone are like those of the humerus of the Hyrax. Femur: Pl. IV. figs. 5 to 9.—The femur is rather more than 5 inches in length : its most important character, as indicative of the affinities of the Pliolophus in the ungulate series, is the continuation of the outer ridge of the great trochanter vertically down the outer border of the shaft and its development into a third trochanter, ¢ f, which subsides before it reaches the mid-length of the bone. The great trochanter rises in an obtusely pointed form 5 lines above the articular head; and it developes a tuberosity at the fore part of its base. The neck sinks behind the head before it rises into the tro- chanter. The small trochanter is a longer ridge than in the Hyrax : the shaft below the trochanter becomes less flattened than in the Paleotheres or Lophiodons: the transverse section gives a kind of semi-ellipse with the flatter side slightly convex: it shows a com- pact wall of bone of about a line or a line and a half thick, and a medullary cavity of from 3 lines to 4 lines in diameter. At about 2 inches from the distal end the shaft begins to expand and become three-sided, the hind- and the out-sides being less convex and broader than the inuer side; then an anterior surface is established by the beginning of the rotular groove, about an inch and a half from the lower end: the inner border of the groove is produced and sharp ; the outer border was broken off in the extraction of the bone: the condyles are produced backward, but not so much forward as in Paleotherium: the inner surface of the expanded condyloid end of the bone, Pl. IV. fig. 8, is flat, with a much less prominent part for the internal lateral ligaments than in Tapirus, Hyrawx, or Paleothe- rium. The popliteal depression is very slightly concave transversely : it is divided from the imtercondyloid fossa by a ridge continued in- ward from the back of the outer condyle. Tibia: Pl. IV. figs. 10-13.— The tibia, which was extracted * Ossemens Fossiles, ed. 8vo, tom. iii. p. 411. pl. 79. f. 6 & 7. > “Les pachydermes qui offrent cette particularité sont les rhinoceros, les tapirs, les chevaux et jusqu’a un certain point les damans, c’est-a-dire les genres que j'ai désignés comme formant une petite famille distincte, et 4 systéme de doigts impairs au pied de derriére ; et c’est précisément a cette famille qu’appartiennent les Paleothériums, par tous les autres rapports.””—Cuvier, Ossemens Fossiles, ed. 1835, 8vo, tom. v. p. 287. 70 PROCEEDINGS OF THE GEOLOGICAL society. [May 20, almost entire from the septarian nodule, was of the left leg; its length is 4 inches 9 lines. The proximal articular surface, Pl. IV. fig. 11, is more equally triangular than in Paleotherium. The outer facet is slightly convex ; the inner one slightly concave transversely. The back part of the proximal end of the bone, fig. 10, shows a broad and deep concavity, bordered by sharp margins; the outer part is somewhat less concave; the inner part is slightly convex ; the rotular ridge was not extracted entire, but was evidently well de- veloped, and extended an inch and a half down the bone. The most characteristic feature of the tibia is the articular surface at the distal end, fig. 13, of which sufficient is preserved to show the obliquity of its course across that end, corresponding with the obliquity of the articular trochlea of the astragalus which is common to the odd-toed hoofed quadrupeds. From these the even-toed group are distin- guished by the rectangular disposition of the ankle-joint. Metatarse: Pl. IV. fig. 14.—The portion of matrix containing the part of the calcaneum, c, and three metatarsals, shows the latter dislocated, and with only one articular end entire—the lower one— in one of them. This is, however, as characteristic as any of the distinctive features of the before-described bones, by the unsymme- trical form of the distal trochlea, due to the position of the ridge near one of the borders of the bone. Both this configuration and the position of the metatarsal show it to have been the outermost of the three: the proximal end is broken off: the length of the bone preserved is 1 inch 5 lines. Of the mid-metatarsal only a small part is exposed, from which the articular end is broken away. Of the innermost metatarsal | inch 8 lines is exposed, but both articular ends are wanting. The difference in the diameter of the three meta- tarsals is less than in the Paleotherium, the middle one being only very little thicker than the other two. In the Tapir the middle metatarsal is less expanded than in the Paleotherium. In the Hy- rax the three metatarsals are of equal thickness ; and the Pliolophus, and probably other Lophiodonts, thus resemble the Hyraz and Tapir, more than the Paleotheria did. Remarks on the Bones of the Extremities.—On a retrospect of the characteristics of the limb-bones above described, it will be seen that the humerus testifies to the ungulate character, and the bones of the hind-leg to the perissodactyle modification, of Pliolophus, with a de- monstration that the odd number of hind-toes was “‘ three” instead of ““one-’ or ““ fiye.’’ The great size, position, and altitude of the proximal tuberosities of the humerus, with the shape of the sessile head of the bone, indi- cate the limited extent and direction of motion of the humerus, and that it belonged to a limb not capable of being rotated or bent out- ward, as in the action for seizing, striking, climbing, or burrowing. The comparatively small size of the distal end, and the little-deve- loped supinator ridge equally indicate the want of size in the supinator or pronator muscles in a limb where the rotation of the wrist or the fore-arm is abrogated. The third trochanter on the femur, the oblique fig L. PLIOLOPHU Wi G-H. Ford : Quart. Journ Geol.Soc.Vol XIV Pl Il Fig 4 BOL. PICEPS. Quart Journ Geol Soc Vol XIV Pl II} Rig 3 W West cop Sl ; F s - i 2 “ we, ? d aa i at : : Fa 5 4 7 = i s z ’ ! Fy . 4 whe : ‘ 2 ‘ eee - 7 : « fe y F ; = F 7 a | ° ‘ ke pe ¢ P ; . ° . F oe “ . x 4 aa i oe onl eS * bd - = * i. < ‘ Vi: ») uf i Bete n ‘: * —_ . = ~ Pt ae — : ee, aes F be i i 3 é f . oa ts * y = Le . ee PLIOLOPHU G.HFord. Quart. Journ. Geol. Soc. Vol XIV PI. Big 4 a — eee W West Joy VULPICEPS. GH¥Ford PLIOLOPHUS VULPICEPS Quart Journ Geol Soc. Vol XIV P]. W Weat. Log f ’ . . ‘ oi t . . . ‘ i A ‘ y ¥. - . : - . ® » s fa \ ’ Ms ad 3 _ - é e we 3 * Sx seth , r) ot oa ’ iy a - i aaa | 2 ae , y PLIOLOPH! t Journ,Geol.Soc. Vol. XIV. PI soe Qt 1857.] OWEN—PLIOLOPHUS VULPICEPS. 71 articular fossa for the astragalus on the tibia, and the three metatarsals of the left hind-foot, all concur with the indications afforded by the skull and teeth in the determination of the true position and affini- ties of Phiolophus and, most probably therefore, of Hyracotherium in the ungulate series. DESCRIPTION OF PLATES IL, IIl., & IV., Illustrative of the Pliolophus vulpiceps, Owen. Puate II. Fig. 1. Under view of the lower jaw and incisor teeth. 2. Upper view of the cranium. 3. Right-side view of the cranium and lower jaw, as attached together in the matrix. 4, Left-side view of the cranium, with the lower jaw and teeth brought back to their proper place. Puate III. Fig. 1. Grinding surface of the molars and last premolar, upper jaw. 2. The same, magnified 4 diameters. r 3. The first and second molar, upper jaw of an older individual. From the London clay, Valley of the Thames. 4. Inside view of the molars and last two premolars, lower jaw. 5. Grinding surface of the molars and last two premolars, lower jaw. 6. The same, magnified 4 diameters. Puate IV. . Outer-side view of humerus. . Front view of humerus. . Proximal articular end of humerus. . Inner-side view of proximal end of humerus. . Front view of right femur. Upper articular end of right femur. . Back view of right femur. Inner-side view of lower end of right femur. . Lower articular end of femur. 10. Back view of tibia. 11. Upper articular end of tibia. 12. Outer-side view of upper end of tibia. 13. Part of lower articular surface of tibia. 14. Portion of matrix, with the caleaneum and three metatarsals ef the left hind-foot. [All the figures are of the natural size, except where otherwise expressed: the letters and figures are explained in the text. | ‘ er) oR © Osy og Or Oo dO 72 PROCEEDINGS OF THE GEOLOGICAL sociETy. [May 20, 2. On some Remains of TERRESTRIAL Puants in the Otp Rep SanpsTone of Cartuness. By J. W. Satrer, Esq., F.G.S., of the Geol. Survey of Great Britain, &c. [Puate V.] Numerovs fragments of plants have for several years past been discovered in the Old Red Sandstone of the North of Scotland; but as yet a few only have been figured. The specimens have now been gathered together by the Director of the Geological Survey for the purpose of illustration. As no experienced botanist has yet been willing to take up such obscure relics, I have thought that some general notes on this old flora might be useful, if only to lead the way to a more critical exa- mination of the specimens. Some of them will be figured also in the second edition of “ Siluria.” The best that I have seen are in the collection of Mr. John Miller, of Thurso, who has for some time directed his attention to these Devo- nian plants, and at the request of Sir Roderick Murchison, who long ago observed them, has most kindly entrusted to us the whole of his collection. Mr. R. Dick, of the same place, has also aided largely in these discoveries. Mr. C. W. Peach has more lately found similar © plants at Wick, and Dr. Hamilton in Orkney. I have examined all these collections, and many of the specimens are now placed in the Museum of Practical Geology. The fossils are preserved in hard, grey, sandy flagstones, which are in many cases abundantly marked with impressions of Annelide- burrows in pairs (PI. V. fig. 6); and these probably indicate that there was no great depth of water where these beds were deposited. The late Hugh Miller has even suggested that these strata may have been accumulated on an extremely level muddy shore*. The most striking of the fossils are large stem-like fragments, of every size up to 3 feet in length, either straight and finely fluted, stems (Pl. V. fig. 1) ;. or curved and occasionally branched, roots? (Pl. V. fig. 2). These are all highly bituminized, and divided by oblique lines, which are evidently only due to mineral structure. Indeed the most striking feature about all these specimens is the mode in which they are mineralized. The carbonaceous substance is cleaved throughout in a series of oblique planes, which in the long root-like specimens (fig. 2) are set quite close (2 or 3 in the space of th of an inch), and cleave the substance in lines perfectly parallel, whatever may be the position or curvature of the specimen. In the stems (fig. 1), these cleavage-lines are generally far wider apart, often 1 of an inch; and they form fissures, often filled up by siliceous matter. Owing to the further compression of the wood, the silex stands out in relief, and forms impressed lines upon the matrix, which may readily be mistaken for the marks of structure. Similar diagonal lines have been noticed by Dr. Hooker‘, and attri- * Testimony of the Rocks, p. 437. tT Quart. Journ. Geol. Soc. vol. ix. p. 50. 1857. | SALTER—DEVONIAN PLANT-REMAINS. 73 buted to “ pressure during silicification,”’ in specimens of very similar plants (Calamites, without articulations). The plants he described, from near Lerwick, Shetland, were in the upper division of the Old Red Sandstone, according to Sir Roderick Murchison*. Coniferous Wood. Pl. V. figs.1 & 2. The abvve-noticed stems are 4 inches wide, and the fragments measure more than 3 feet in length, without any tendency to taper away. See fig. 1. The surface is fluted pretty regularly by delicate longitudinal ridges; the intervening hollows being gently concave, not abruptly grooved ; these ridges are tolerably regular and equidistant, without being absolutely continuous; seldom as much as a line apart, but occasionally more. They are not interrupted by any transverse joints as in Calamites; and, from this circumstance, as well as from the more solid texture of the stem, they might have been judged to belong to the Stereocalamee of Unger, some of the genera of which, Calamopitys or Calymma, would, from Unger’s description, present a very similar appearance. With these there are long, curved and flattened linear specimens (fig. 2), sometimes more than 4 feet long, and from an inch to 12 inch broad, very slowly tapering, and forked near the end. Both the straight and the curved stems are even-edged, as if ori- ginally cylindrical; and there are evident traces, in some portions, of a central pith (probably not a woody axis, as the space in the centre is now filled by the matrix), while the enveloping thick sheath is all carbonized. This structure, a thick woody envelope, surround- ing a central pith, may be that of a Conifer allied to the Dadoxylon+ of the Coal-measures; and this is confirmed by the microscopic sections (fig. lc) which have been kindly examined for me by Prof. Quekett, who finds the ordinary coniferous structure—wood- fibres dotted with disks; and these appear to have been in alter- nating double rows, as in the modern Araucarians, and as in the fragments of Coniferous wood, described by Hugh Miller, from beds of Devonian age near Cromarty{. This dotted structure will, of course, effectually distinguish these large stems from the woody struc- tures (Aporoxylon), without disks to the wood-cells, which Prof. Unger has lately § described ; otherwise the external appearance, and even the mode of fossilization, are so similar in both, that I should have provisionally referred our specimens to the same genus, had there been no means of ascertaining the minute structure. Besides these large stems and roots, there are tapering branches, an inch broad and often more than a foot in length, less regularly striated than the stems, but still distinctly fluted all the way up; * Loe. cit. T In Dadoxylon the wood-fibre has more numerous rows ‘of disks than in the Caithness fossils. +t Testimony of the Rocks, p. 435. § Denkschrift. Kais. Akad. Wissensch., Math.-Nat. Classe, vol. xi. 1856: Beitrag zur Palaontologie des Thiiringer Waldes, von R. Richter und F. Unger: p. 181, pl. 13. figs. 3-11. 74 PROCEEDINGS OF THE GEOLOGICAL Society. [May 20, and these bear branchlets at short intervals, in whorls of threes or fours, which diverge at nearly right angles from the branch, some- thing like those of an Araucaria. It is not improbable that these striate branches may belong to the same plants as the stems (and roots?) above mentioned. Rootlets (Pl. V. figs. 3-7).—Other and very numerous specimens, lying flat in the stone, and presenting simply a linear rachis with alternate (fig. 4) or dichotomous (fig. 3) smooth branchlets, appear to me to be far more likely referable to the smaller roots than to anything else. They occur about 6 or 8 inches long, and seldom so much as a quarter of an inch broad; they taper slowly, and are flexuous or zigzag at the origin of the branches, which are them- selves again branched. In a few instances irregular granulations occur on the roots: in others (fig. 7) lateral buds or tubercles take the place of the ter- minal branchlets or rootlets, and become crowded towards the tips. They put one in mind of the tubercular roots of some of the Leguminous plants, or may be still better compared with the tubercles or exostoses found on the roots of many Coniferous plants, 4rau- caria, Thuja, Podocarpus, and others*. These tubercles seem to me to give great colour to the idea that the linear fragments to which they are attached are roots; and, as these are in most respects similar to the other specimens, with dichotomous or alternating branches (figs. 3-6), there is a strong presumption that the latter are roots too. Whether any of them may be referable to the woody plants above described, rather than to the Lycopodiaceous plants next to be noted, it is scarcely possible to decide; but the former is certainly probable. I am more inclined to regard all these as roots, since they bear the greatest resemblance to similar fragments abun- dant in the Upper Devonian beds of the South of Ireland, and which, from their mode of occurrence in a sort of hardened underclay beneath the beds of sandstone, I have always thought to be rootst. Similar fragments are figured in Mr. Hugh Miller’s last work{, and in these the dichotomous character is clearly seen. I do not think their structure or mode of branching at all like that of marine plants. Nor have they any distinct trace of a mid- rib, as if they were cleft or divided leaflets, or of parallel veins, as in the seawrack (Zostera). Nor, indeed, do they show anything but a linear riband (probably once a soft cylindric root) which branched repeatedly. A few more perfect plants deserve to receive specific notice ; and, in naming the remarkable Lycopodiaceous plant (fig. 8), I have had in view both the kindness of Mr. John Miller, of Thurso, and the memory of the lamented author of ‘‘ The Testimony of the Rocks.” * See Dr. Hooker’s paper on these root-tubercles, Proc. Linn. Soc. 1845, No. 58. p. 355*. I have the satisfaction of Dr. Hooker’s concurrence in this view of the nature of the fossils. + Proc. Dublin Geol. Society, vol. vii. p. 63. t Testimony of the Rocks, p. 429. 1857. ] SALTER—DEVONIAN PLANT-REMAINS. 795 A fossil fern found in Orkney and described in Hugh Miller’s work (p. 25) has not occurred among the specimens under our notice. Lycoropites MixLuert, sp. nov. Pl. V. figs. 8a, 86. L. ramis flagelliformibus, 2 pedes et ultra longis; ramulis remotis, foliis secundis 2-3 lineas longis, lanceolatis | obtusis?}. This fine specimen is worthy of a name on account of the rarity of such remains in rocks of this age; but not much can be said as to its structure. The stem (only a fragment 2 feet long is pre- served) is flexuous, about 2ths of an inch thick, and was probably of prostrate growth as indicated by the secund arrangements of the foliage, and the length and slenderness of the stem itself. In this length of 2 feet are only two short branches, about an inch long, and about 7 inches apart, and set on at a very oblique angle, as often seen in recent Club-mosses, The foliage is much larger than in the Lepidodendron next described. The leaves are very indistinct, but are about 1rd of an inch long, lanceolate (obtuse ?), and much curved upwards to one side (the upper side probably). There is some in- dication of their being set on in spiral lines, instead of quincuncially. Locality. Near Thurso. (Mr. John Muiller’s collection.) LEPIDODENDRON NoTHuUM, Unger (?). PI.V. figs. 9a, 96, & 9e. Richter & Unger, Beitrag Palaont. Thuringer Waldes, Vienna Acad. Transact. 1856, pl. 10. fig. 4. Lycopodites, Hugh Miller, Testimony of the Rocks, figs. 12 & 120, pp. 24 & 432 &e. Stems about a foot long, or even longer, and nearly 4 an inch broad, tapering but very little from end to end; the branches short, set on at an acute angle, and blunt at their terminations. Leaves in 7 to 10 rows, very short, not a line long, and scale-like, of an ovate, acuminated form, and rather spreading than closely imbricate. Their acuminate tips are about as long as their broader bases (fig. 9c). Our specimens do not agree exactly with that figured by Unger, having the scales or leaves rather longer. But his figure appears to show only the cicatrices, not the leaves themselves; and the size, diameter of the branches, and close small leaf-scars in both agree, and are different from any species that I have seen figured from the Coal-formation. Loc. From Stromness, Mr. Peach; Thurso, Mr. John Miller. Abundant. The late Mr. Hugh Miller figured* a fine and much-branched specimen of this species. We have others, in which the main stem (a little flexuous) gives off short and narrower branchlets, which are again branched, as in his figure. The tips of the shoots often scarcely show the scales. * Op. cit. p. 432. 76 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20, The above species all occur (with the exception of the Lycopodites Milleri, which is only yet known at Thurso) as well in the Orkneys as at Caithness. Both the Lepidodendron and the linear root-like branches are found in Dale and Viewan quarries at Stromness, Miram Blaw, and near Frith, Orkney. The large stem-like bodies and curved roots are also found with them. These were sent by Dr. Hamilton and Mr. Peach. The best examples, however, were found in the flag-quarries at Thurso, and are in Mr. Miller’s collec- tion, and most of our figures are from his specimens. Mr. C. W. Peach has for some years been diligently searching for these plants, and has sent up some 70 specimens from Kilminster, near Wick, which comprise only the smaller species. We have here therefore the fragments of a flora, which may at least be compared with that discovered in the Thiringer Wald by M. Richter, and which has been so beautifully illustrated by Prof. Unger in the work above quoted. Though not so numerous in species, yet the Scotch collections contain some forms of larger size, indicating a vegetation of considerable importance at an era so far back as that of the Middle Devonian. Prof. Unger’s plants, which he has spoken of as being of a totally new type, and im some respects a prototype of succeeding floras*, are from the Cypridina- schist, or Upper Devonian of Germany, strata which are believed to be of younger age than those described by Mr. Hugh Miller, and plants from which are here figured. The discoveryt by Mr. Strickland and Dr. Hooker of spores of a Lycopodiaceous plant in the passage-beds between the Old Red Sand- stone and Ludlow Rock (to which I lately added, during a visit to Ludlow, branched fragments of the stemsf) is a sufficient indication that we have to make out the characters of a still more antique vege- tation, of which, to judge from the fragmentary evidence yet ob- tained, the characters were not altogether unlike those of later paleeozoic times. The strata from which the fossils above enumerated were obtained have been long ago described, and their relative age determined by the labours of Prof. Sedgwick and Sir R. Murchison||. They are regarded by these authors as part of the Middle Devonian rocks, while in Hugh Miller’s classification they stand as part of his Lower Division. Dipterus and Diplopterus are the prevailing genera of fish that accompany the plants. Note on the PLANT-BEARING DEvontiAN Beps of CaiITHNESs. By Joun Mixer, Esq., of Thurso. Tue fossiliferous beds of the Old Red Sandstone of Caithness form by far the larger part of the area of that county. Along the whole * ¢Siluria,’ lst ed., p. 358. + Quart. Journ. Geol. Soc. vol. ix. p. 10 &c. t It is to be regretted that these small branched specimens, which were 4rd of an inch thick, were lost before they could be fully examined in London. || Geol. Trans. 2nd Ser., vol. iii. p. 125 &c. Quart Journ Geol. Soc Vol XIV Pl. FOSSIL PLANTS FROM CAITHNESS AND ORKNEY. est ith WWest imp. 1857. | SALTER—DEVONIAN PLANT-REMAINS. Me 7) of the boundary-line between Sutherland and Caithness, the gneissose rocks of the Highlands extend into Caithness to the distance of from three to eight miles, and are succeeded by the Old Red Sand- stone, which stretches in one unbroken deposit eastward to the German Ocean and northward to the Northern Ocean. Along the whole of the line of junction of the two deposits, the rocks are so covered with moss and heath that it is extremely difficult to get at the base of the Old Red Sandstone; at the Ord of Caithness, how- ever, in the sea-cliffs immediately under the celebrated mountain- pass of that name, very fine sections may be seen of the great fos- siliferous conglomeratic base of the Devonian or Old Red. From the Ord of Caithness northwards to Duncansbay Head, and from Duncansbay Head westwards to Sandside Head, the seaboard of the county is composed of a range of mural precipices, from 40 to nearly 400 feet in height ; and the whole of the Devonian portion of the county northwards of the Morven and Scarabin Hills is an elevated plateau, rising abruptly out of the sea, but seldom attaining a greater height than 500 feet above the sea-level in any part of the interior. The strata are inclined at low angles, generally dipping towards the north-west, and sometimes almost horizontal; and throughout the greater portion, wherever a quarry has been opened, at the foot of the cliffs, on the sea-shore, or on the tops of the hills, the practised eye can detect fragments of plants mixed with the bones and scales of fish. The most entire and largest specimens, however, of plants have been hitherto found in the neighbourhood of Thurso, in the flagstone-quarries, which are numerous in that locality. DESCRIPTION OF PLATE V., Illustrative of Fossil Plants from Caithness and Orkney. Fig. la. Fragment of a large, straight, compressed, finely fluted, bituminized, stem- like body ; from a quarry three miles west of Thurso. One-fourth of the natural size. (Mr. J. Miller’s collection.) Fig. 16. Portion of the finely fluted surface ; magnified. Fig. le. Traces of woody structure, showing the remains of pitted fibre, with a double row of pits or disks. Highly magnified. Fig. 2. Fragment of a large, curved, compressed, bituminized root-like (?) body; from a quarry four miles east of Thurso. One-fourth natural size. (Mr. J. Miller’s collection.) Fig. 3. Dichotomous rootlet ; from Kilminster, Wick. Natural size. (Geological Survey collection.) Fig. 4. Dichotomous root; from Kilminster, Wick. Natural size. (Geological Survey collection.) The oval mark in the specimen is the outline of an Annelide-burrow. Fig. 5. Branched root, marked with fine tubercles, which have somewhat of a spiral arrangement. Natural size. From Dale Quarry, Stromness. (Geological Survey collection.) Fig. 6. Branched rootlet lying on a flagstone which presents traces of Annelide- burrows (4renicolites), frequently in pairs. Kilminster, Wick. Natural size. (Geological Survey collection.) Fig. 7a. Terminal rootlet with lateral tubercles. Fig. 7b. The terminal tubercles, magnified. 78 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Fig. 8a. Lycopodites Milleri. From a quarry four miles east of Thurso. One- fourth of the natural size. (Mr. J. Miller’s cabinet.) Fig. 84. The same; a small portion, magnified. Fig. 9a. Lepidodendron nothum, (Unger) ?, portion of stem; natural size. From Harland, Wick. (Geological Survey collection.) Fig. 94. Magnified portion of the cast of another specimen, showing the arrange- ment of the bracts. Magnified three times. From Stromness, Orkney. (Geological Survey collection.) Fig. 9c. Portion of fig. 9a, magnified. DONATIONS TO THE LIBRARY OF THE GEOLOGICAL SOCIETY. From July 1st, 1857, to October 31st, 1857. I. TRANSACTIONS AND JOURNALS. Presented by the respective Societies and Editors. AMERICAN Journal of Sciences and Arts. 2nd Series. Vol. xxiv. No. 71. September 1857. From Prof. Silliman, For. Mem. G.S. W. J. Taylor.—Investigations on the Rock-guano from the Islands of the Caribbean Sea, 177. G. P. Scrope.—On the Formation of Craters, and the Nature of the Liquidity of Lavas, 217. H. Haw.—On the occurrence of Natro-boro-calcite with Glauber- salt in the Gypsum of Nova Scotia, 230. E. K. Kane.—Arctic Explorations, 235. P. Casamajor.—A method of measuring the Angles of Crystals by Reflection without the use of a Goniometer, 251. H. St. Claire—Magnesium, Boron, and Aluminium, 261. TiS: eo the probable origin of some Magnesian Rocks, Bo. St. Clair Deville-—Chlorids in Voleanos, 273. C. T. Jackson.—Agalmatolite, 273. A. Gaudin.—Corundum, 273. C. F. Chandler.—Slate-rock of Hungary, 273. A. Seott.—The Bermuda Islands, 274. T. S. Hunt.—The Cherokine of C. U. Shepard, 275. W. J. Taylor.—Occurrence of Aragonite near the Arkansas River, 275. J. Hall, and F. B. Meek.—Fossils from the Cretaceous Forma- tions of Nebraska, 275. J. Hall_—New Fossils from the Carboniferous Limestones of Indiana and Illinois, 276. F. B. Meek.—The Cretaceous Fossils of Vancouver’s Island, Western America, 276, 80 DONATIONS. American Journal of Sciences and Arts. No. 71 (continued). F. V. Hayden.—Notes explanatory of a map and section illustra- ting the Geological Structure of the country bordering on the Missouri River from the mouth of the Platte River to . Fort Benton, 276. =. New Species and Genera of Fossils collected by Dr. F. V. Hayden in Nebraska Territory in 1856, 277. Guyot.—North Carolina Mountains, 277. Waugh.— Himalayas, 278. D. J. Macgowan.—The drying-up of the Yellow River, China, 278. J. W. Dawson.—Devonian Trees, 280. W. J. Taylor.—Examination of a Nickel Meteorite, from Oktib- beha county, Mississippi, 293. E. Pugh.—Meteorie Iron of Mexico, 295. A. Gobel, Wohler, and Duprez.—Meteoric Stones, 295. Eleventh Meeting of the American Association (at Montreal), 301. American Philosophical Society. Vol. vi. pp. 167-202. Du Bois.—Aluminium, 171. A. S. Piggot.—Columbian Guano, 189. Eckfeldt and Dubois.—Apparatus for taking specific gravities, 193, 201. Assurance Magazine and Journal of the Institute of Actuaries. Vol. vii. part 2. No. 28, July 1857. Part 3. No. 29, October 1857. Athenzeum Journal for July to October 1857. From C. W. Dilke, Esq., F.G.S. Notices of Scientific Meetings, &c. British Association Meeting, pp. 1116, 1148, 1181. Coal and Iron in Italy, 1129. Bessemer’s Cast-iron, 1332. Bengal Asiatic Society, Journal. New Series, Vol. xxvi. No. 84. 1657." Ne 1. R. Schlagintweit.—Magnetic Survey of India, 54. : No. 86. 1857. No. 2. A. Schlagintweit.— Magnetic Survey of India, 97. No. 87. 1857. No. 3. H. G. Raverty.—The mountain-district formmg the western boundary of the Lower Derbjat, commonly called Roh, 177. R. Schlagintweit.—Report on the Magnetic Survey of India, 208. Bent’s Monthly Literary Advertiser. Nos. 639, 640, 641. Berlin. Zeitschrift der Deutschen geologischen Gesellschaft. Vol. vii. part 4. 1856. Proceedings of the Society, 498. Proceedings of the Geological Section of the Association of German Naturalists at Vienna, 1856, 510. Letters, 537. EE DONATIONS. 81 Berlin. Zeitschrift der Deutschen geologischen Gesellschaft. Vol. viii. Part 4. 1856 (continued). G. Rose.—Ueber die heteromorphen Zustande der Kohlensaure Kalkerde, 543. E. Beyrich.—Die Conchylien des Norddeutschen Tertiargebirges ; Fiinftes Stiick, 553 (3 plates). F. von Richthofen.—Ueber den Melaphyr, 589. R. Hensel.—Beitrage zur Kenntniss fossiler Saugethiere, 660 (2 plates). —$ —. ———-. Vol. ix. Part 1. 1857. Proceedings and Letters, 1-24. Baeumber.— Ueber das Vorkommen von Nickelerz im Mannsfeld- schen Kupferschiefergebirge, 25 (2 plates). F. Roemer.— Ueber Fisch- und Pflanzen-fiihrende Mergelschiefer des Rothliegenden bei Klem-Neundorf unweit Lowenberg, und im Besonderen iiber Acanthodes gracilis, 51 (plate). C. von Schauroth.—Die Schalthierreste der Lettenkohlenforma- tion des Grossherzogthums Coburg, 85 (3 plates). W. Keterstein.—Ueber eimige deutsche devonische Conchiferen aus der Verwandtschaft der Trigonaceen, 149 (plate). Grewingk.—Der Zechstein in Lithauen und Kurland, 163. Noeggerath.—Das Erdbeben im Siebengebirge am 6 December 1856, 157. Berwickshire Naturalists’ Club, Proceedings. Vol.iv. No. 1. W. Dickson.—Anniversary Address, 3. Breslau. Bericht uber die Thatigkeit der naturwissenschaftlichen Section im Jahre 1856 (Schles. Gesellsch. vaterl. Kultur), abgestattet von den Secretairen der Section H. R. Goppert und F. Cohn. F. Romer.—Ueber neue Fischreste in schwarzen Thonschiefern in dem Dorfe Klein-Neundorf unweit Lowenberg, 8. Ueber weiteres palaontologisches Material, 8. Bach’s Geognostische Uebersichtskarte von Deutsch- land, &c., 9. Fische der Gattung Istiens aus den Kreidebildungen Westphaliens, 10. — Murchison und Nicol’s Geologische Karte Europa’s, 10. Dritte Auflage der Lethea Geognostica (Bronn), 10. Scharenberg.—Clymenia undulata aus den Ebersdorfer Kalk- briichen, 11. = In dem Schnossnitzer Thonlager aufgefundenes ex- emplar eimer Bliithe (Getona membranosa, Goepp.), 11. Zeuschner.— Ueber eine Langs-Morane, 11. Steinbeck.—Ueber die Siegelerde von Striegau, 11. Goppert.—Ueber die Braunkohlen-Formation in Schlesien, 13. Ueber em zur Erlauterung der Steinkohlen-Formation im hiesigen Koniglichen botanischen Garten errichtetes Profil, 14. VOL. XIV.—PART I. G 82 DONATIONS. British Association for the Advancement of Science. Report. of the 26th Meeting, 1856. 1857. C. Daubeny.—Address, xlviii. Report on the Alterations in the Channels of the Mersey within the last fifty years, 1 (map). R. MacAndrew.—Report on the Mollusca of the North-east Atlantic, 101. P. P. Carpenter.—Report on the Mollusca of the West Coast of North America, 159 (4 plates). J. a on Cleavage and Foliation in Rocks. Part I., 369 T. Wright.—Stratigraphical Distribution of the Oolitic Echino- dermata, 396. S. Henslow.—The typical forms of Minerals, Plants, and Animals for Museums, 461. F. C. Calvert.—Incrustations of blast-furnaces, (Sect.) 50. J. H. Gladstone.—The Salts present in the Cheltenham Waters,51. W. H. Baily.—Fossils from the Crimea, 60. J. S. Bowerbank.—Siliceous Deposits in the Chalk-formation, 63. P. B. Brodie.—Corals in the Lias, 64. Pollicipes in the Inferior Oolite near Stroud, 64. J. Buckman.—Basement-beds of the Oolite, 64. R. Harkness.—Old palzeozoic fossils, 65. Joimtings of Rocks, 65. Lignites of Antrim and Mull, 66. Hennessey.—Relative Distribution of Land and Water as affect- ing Climate at different Geological Epochs, 66. K. Hull.—The South-easterly attenuation of the Oolitic, Liassic, | Triassic, and Permian Formations, 67. o J. B. Jukes.—Alteration of Clay-slate and Gritstone into Mica- , | schist and Gneiss by the Granite of Wicklow, 68. | M. Moggridge.—The time required for the formation of Rolled : Stones, 69. | C. Moore.—The skin and food of Ichthyosauri and Teleosauri, 69. si Upper and Middle Lias of the West of England, 70. f R. I. Murchison.—The Bone-beds of the Upper Ludlow Rock, : and base of the Old Red Sandstone, 70. a R. Mushet.—An ancient Miner’s Axe discovered in the Forest of Dean, 71. R. Owen.—Dichodon cuspidatus, Isle of Wight, 72. — Fossil Musk-Ox from the Wiltshire drift, 72. —- Dichobune ovina, Isle of Wight, 72. — Stereognathus ooliticus, Stonesfield, 73. Scelidotherium leptocephalum, La Plata, 73. W. Pengelly.—The Beekites in the Red Conglomerates of Tenby, 74. J. W. Salter.—Pterygotus, 75. —_—— Paleozoic Star-fishes, 76. H. C. Sorby.—Formation of Drift-bedding, 77. —_—— Formation of Magnesian Limestone, 77. -_-— Microscopical Structure of Mica-schist, 78. E. Vivian.—Kent’s Cavern, Torquay, 78, 119. Woodhall.—Lower Lias Rock of the Yorkshire coast, 80. T. Wright.—Upper Lias Ammonites in the so-called Basement- beds of the Inferior Oohite, 80. DONATIONS. 83 British Association for the Advancement of Science. Report of the 26th Meeting, 1856. 1857 (continued). C. C. Babington.—Supposed fossil Fucus from Aust Chiff, 83. L. Jenyns.—Variation of Species, 101. A. G. Findlay.—Volcanic Islets to the South-east of Japan, in- cluding the Bonin Islands, 110. F. D. Hartland.— Vesuvius and its Eruptions, 111. D. Livingstone.—Southern Africa, 113. S. Highley.—Crystallogenesis. H. D. Rogers.—Correlation of the North American and British Paleozoic Strata, 175. Canadian Journal. New Series. No. 10. July 1857. K. J. Chapman.—Cryptoceras in Silurian rocks, 264. Trask.—Earthquake in California, 299. T. S. Hunt.—Metamorphism of rocks, 300. —— Analyses of waters of the St. Lawrence and the Ottawa, 300. Whitney.—Azoic rocks of Canada, 302. Ville and Chapman.—Supposed Emeralds from Algiers, 302. Billings and Chapman.—Cystidea, 302. Wohler and Deville.—Boron, 504. Field.—Silver in Sea-water, 305. Deville and Caron.— Magnesium, 305. Wohler.—Oxide of Silicium, 305. No. 11. September 1857. Gilbert.—The Arizona Copper-mine, 321. S. Hunt.—On the origin and metamorphosis of some Sedi- mentary Rocks, 355. P. Stratford.—Notes on the Natural History of New Zealand, 357. Charleston (South Carolina). Proceedings of the Elliott Society, pp. 49-104. 1856. L. R. Gibbes.—The past and present condition of the Niagara Falls, 91. Frampton.—Argentiferous Galena, 101. Chemical Society, Quarterly Journal. No. 38. Vol. x. Part 2. July 1857. F. A. Abel.—Crystallized binoxide of Tin, 119. oe Manufacture of Iron and Steel, 125. No. 39. Vol.x. Part 3. October 1857 J. ames Napier.—The action of heat on Gold and its alloy with Copper, 229. Civil Engineer and Architect’s Journal. July 1857. No. 280. J. Millar.—Supply of water to Geelong, 216. F, Ransome.—Artificial Stone, 235. 5 T: S. Copenhagen. Queestiones que in anno 1857 proponuntur a Socie- tate Regia Danica Scientiarum cum premii promissu. G2 84 DONATIONS. Copenhagen. Oversigt over det Kongelige danske Videnskabernes Selskab Forhandlinger og dets Medlemmers Arbeider i Aaret 1856. Fr. Wohler.—Kryolith og Aluminium, 247. Critic. Nos. 391-397. Notices of Scientific Meetings, &c. Darmstadt. Notizblatt des Vereins fiir Erdkunde und verwandte Wissenschaften zu Darmstadt. Nos. 41, 42, 43, 44, and 45 (in one), and 46. February to May 1857. R. Ludwig.—-Zur Geologie von Bohmen, 305. Erdwarme, 311. Fossile Affen, 312. Notizblatt des Vereins fur Erdkunde und verwandte Wissenschaften zu Darmstadt, und des Mittelrheinischen geolo- gischen Vereins. No. 1. May 1857. Dijon. Mémoires de I’ Académie Impériale des Sciences, Arts et Belles- lettres &. Deux. Série. Vol. v. Année 1856. 1857. L. Nodot.—Description d’un nouveau genre d’Edente fossile, renfermant plusieurs espéces voisines du Glyptodon, suivie d’une nouvelle méthode de classification applicable a toute Vhistoire naturelle et spécialement 4 ces animaux, (Sect. des Se.) 1 (Atlas of Plates). A. Perrey.—Bibliographie seismique, 183. Dublin Geological Society, Journal. Vol. vii. Part 4. 1857. R. H. Scott.—Carboniferous beds of Killybegs, co. Dublin, 181. J. R. Kinahan.—Annelidoid Tracks in the Rocks of Bray Head, co. Wicklow, 184. W. L. Wilson.—Geology of the neighbourhood of Kenmare, 188. C. P. Molony.—Drift-coal in Sand near Newcastle, 193. S. Haughton.—Pitchstone and Pitchstone-porphyry of Barnes- more and Lough Eske, co. Donegal, 196. Distorted Fossils in Cleaved Rocks, 219 (2 plates). J. Kelly.—Subdivision of the Carboniferous Formation of Ireland, 222. Dublin Royal Society, Journal. No. 6. July 1857. R. Griffith and Adolphe Brongniart.—Fossil plants of the Yellow Sandstone, 313 (plate). Anderson.—Iron and Coal of Connaught, 325 (map). France, Société Géologique de, Bulletin. Deux. Sér. Vol. xin. feuill. 31-36. April 1856. A. Boué.—Paralléle des tremblements de terre, des aurores boré- ales et du magnétisme terrestre, mis en rapport avec le relief et la géologie du globe terrestre, etc. (fin.), 484. J. Barrande.—Note sur quelques nouveaux fossiles découverts aux environs de Rokitzan (Bohéme), 532. Gaillardot.—Découverte d’un gisement de Nummulites prés de Séida (Syrie), 538. Michel.—Note géologique sur la Dobroudcha, entre Rassowa et : Kustendjé, 539. DONATIONS. 85 France, Société Géologique de, Bulletin. Vol. xiii. (continued). A. Damour.—Nouvelles recherches sur les sables diamantiféres, 542. R.-F. de Scyff.— Voyage au Bator, volcan de l’ile de Bali (trad. par A. Perrey), 554. T. Arriens.—Ascension au volean du Kloed en Septembre 1854 (trad. par A. Perrey), 560. J. W. Salter et J. Barrande.—Sur les empreintes de Pas-de-Boeuf des Vaux-d’Aubin, pres d’Argentan (Orne), 568. Hornes.—Liste de 84 espéces marines subfossiles de Kalamaki, sur l’isthme de Corinthe, Dale De Séménoff.—Sur une éruption volcanique 4 Ouyiine-Kholdon- gui (Mandchourie) en 1721, 574. Vol. xiv. feuili. 8-18. Nov.—Dec. 1856. P. de Berville.—Note sur une nouvelle espéce de crustacé fossile trouvée dans le caleaire grossier inférieur (PI. IT.) (fin.), 113. J. Koechlin-Schlumberger.—Etudes géologiques dans le départe- ment du Haut-Rhin.—II. Environs de Belfort, 117. Se. Gras.—Sur la période quaternaire dans la vallée du Rhéne et sa division en cing époques distinctes (Plate III.), 207. A. Viquesnel.—Analyse de la premiére partie de son Voyage dans la Turquie d’ Europe, 249. Albert Gaudry.—Résumé du ler volume de ses Recherches sci- entifiques en Orient, 252. Ch. Sainte-Claire Deville—Mémoire sur les émanations volea- niques, 254. Delesse.—Sur la pierre ollaire, 280. B. Studer.—Observations dans les Alpes centrales de la Suisse, 287. Index for Vol. xii. Franklin Institute of the State of Pennsylvania, Journal. 3rd Series. Vol. xxxiv. July 1857. No. 1. W. M. Roberts.—Improvement of the Ohio River, 23. Dembinski.—Solution of auriferous quartz, 56. August 1857. No. 2. W. M. Roberts.—Improvement of the Ohio River, 73. J. N. von Fuchs.—Soluble glass, its preparation and applications, 121. Gaudin.—Artificial white sapphire, 134. September 1857. No. 3. W. M. Roberts.—On the proposed improvement of the Ohio River, 145. J. N. von Fuchs.—On Soluble Glass, 194. Hamburg. Abhandlungen aus dem Gebiete der Wissenschaften, herausgegeben von dem naturwissenschaftlichen Verein in Hamburg. Vol. i. 1856. Illustrated Inventor. No. 2. November 7, 1857. Isle of Wight Institution. Catalogue of Books, with its Laws and Regulations. 1848. From HE. P. Wilkins, Esq., F.G.S. Se Se 86 DONATIONS. Journal of the Indian Archipelago and Eastern Asia. New Series. Vol. 2. No. 1. 1857. From J. R. Logan, Esq., F.G.S. Literary Gazette for July, August, September, and October, 1857. From L. Reeve, Esq., F.G.S. Notices of Scientific Meetings, &c. C. A. Murray.—Dust-storm at Bighdad, 686. G. Greenwood.—Rain and Rivers, noticed, 704. Geological Society’s Report, 711. W. Symonds’ Stones of the Valley, noticed, 751. Obituary notice of Dean Conybeare, 805. American Association Meeting, 828, 1027. British Association Meeting, 822, 852, 878. London, Edinburgh, and Dublin Philosophical Magazine. 4th Series. Vol. xiii. No.86. July 1857 (Supplement). From R. Taylor, Esq., F.G.S. S. Haughton.—Hypostilbite and Stilbite, 509. W. De la Rue and H. Miller.—Burmese Naphtha, 512. P. P. King.—Specific gravity of Sea-waters, 523. F. Field.—Silver in Sea-water, 524. W. S. Jacob.—The Earth’s mean density, 525. R. I. Murchison.—Silurian rocks and fossils of Norway and the Baltic Provinces, 529. R. Owen.—The Pliolophus vulpiceps from the London Clay, 530. J. W. Salter.—Terrestrial plants m the Old Red Sandstone of Caithness, 533. Heddle.—The sulphato-carbonate of barytes of Thomson, 537. Vol. xiv. No. 90. July 1857. s. Haughton.—The siliceo-felspathic rocks of the South of Ire- land, 47. E. Atkinson.—Chemical Notices, 51. H. Falconer.—The species of Mastodon occurrmg in England, 72. Becquerel.—Slow actions produced under the combined influence of heat and pressure, 76. —_——. ———._ Vol. xiv. No. 91. August 1857. Wohler.—Crystallized Silicon, 103. C. W. Vincent.—Sulphide of Aluminium, 127. | G. P. Scrope.—Craters and Lavas, 128. J. Phillips.—Oolite and Ironstone Series of Yorkshire, 153. J. Buckman.—Oolites of Gloucestershire, 154. T. D. Ansted.—Geology of Andalusia, 155. Rammelsberg.— Beudantite, 159. No. 92. September 1857. F. C. Calvert and R. Johnson.—Chemical changes of pig-iron and wrought-iron, 165. G. P. Scrope.—Craters and Lavas, 188. H. Medlock.—Reciprocal action of Metals and the constituents of Water, 202. C. G. Williams.— Destructive distillation of Boghead Coal, 223. .——_ —__... DONATIONS. 87 London, Edinburgh, and Dublin Philosophical Magazine. Vol. xiv. No. 93. October 1857. From R. Taylor, Esq., F.G.S. T. H. Huxley.—The structure of Glacier-ice, 241. Munich. Gelehrte Anzeigen. Herausgegeben von Mitgliedern der k. bayer. Akad. der Wissensch. Vol. xlii. Januar bis Juni 1856. I. Philosophisch-philologische Classe. II]. Mathematisch-physicalische Classe. C. F. Rammelsberg.—Krystallographische Chemie, 13. G. G. Winkler.—Die Pseudomorphosen des Mineralreiches, 15. G. Landgrebe.—Naturgeschichte der Vulkane, 31. B. Cotta.—Die Gesteinlehre, 71. G. H. O. Volger.—Aragonit und Kalzit, 81. Epidot und Granat, 105. III. Historische Classe. Bulletins der drei Classen. Vogel und Reischauer.—Analyse des sogenannten Magneteisen- stems des Silberberges bei Bodenmais, 57. F. v. Kobell—Stauroskopische Beobachtungen, 78 (2 plates). Vol. xl. Juli bis December 1856. B. Cotta.—Die Lehre von den Flotzformationen, II. 19. Ehrenberg.—Mikrogeologie, Il. 8 Geinitz.—Die Versteinerungen der Stemkohlenformation in Sachsen, II. 22, Girard.—Geologische Wanderungen, II. 2. Hausmann.—Ueber die durch Molekularbewegungen in starren Korpern bewirkten Formveranderungen, II. 1. Leonhard.—Die quarzfuhrenden Porphyre, II. 7. Naumann.—Krystallographie, II. 9. Strecker.—Das Christiania Silurbecken untersucht von Kjerulf, II. 10. V. Kobell.—Stauroskopische Beobachtungen, Bullet. 1 (plate). New York. Annual Report of the Trustees of the New York State Library, 1857. Seventieth Annual Report of the Regents of the Uni- versity of the State of New York. 1857. Catalogue of the New York State Library ; 1855. Vol. i. General Library. Vol. 1. Law Library. 8vo. Albany, 1856. North China Herald. No. 395. June 13, 1857. Hydrography of the Yellow River, p. 183. Photographie Society, Journal. Nos. 56, 57, and 58, and Index for Vol. i. Pick and Gad, a Monthly Record of Mining and its allied Sciences and Arts. Condacted by W. Arundell. No.1. November 1857. Physical and Geological Structure of the Mining Districts of Cornwall and South Devon, part 1, 1 (map). School of Mines, 12. Drainage of Mines, 16. Notices of Books, 22. Miscellaneous, 28. 88 DONATIONS. Quarterly Journalof Microscopical Science, including the Transactions of the Microscopical Society of London. No. 20. July 1857. J. B. P. Dennis.— Microscopical characters of certain so-called Cetacean bones associated with Cetotolites in the Red Crag, ‘191 (plate). No. 21. October 1857. Ray Sheen List of Officers, Local Secretaries, and Subscribers, 1856. —. Monograph of the Freshwater Polyzoa, by Prof. G. J. Allman, 1856. Royal Astronomical Society, Memoirs. Vol. xxv. 1857. Monthly Notices. Vol. xvi. Royal eae ed Society, Proceedings. No.9. April and May 1857 A. S. Waugh, and B. H. Hodgson.—Himalayas, 345. ————.. No. 10. Sir R. I. Murchison.—Anniversary Address, 365. Royal Society. Proceedings. Vol. viii. No. 26. J. Thomson.—Plasticity of Glacier-ice, 455. T. S. Hunt.— Metamorphism of Rocks, 458. No. 27. W. Hopkins.—Conductive powers of various substances, and Terrestrial Temperature, 535. J. P. Joule and W. 'Thomson.—Thermal effects of compression of substances and fluids, 564. St. Pétersbourg, Mémoires de I’ Académie Impériale des Sciences de. Sixiéme Série. Sciences Math. Phys. et Nat. Vol. ix. Seconde partie : Sciences Naturelles, Vol. vu. 1855. —, Bulletin de la Classe Physico-Mathématique de I’ Aca- démie Imp. des Sc. Nat. de. Vol. xii. 1854. Paucker.—Die Gestalt der Erde, 7. —_——_, ———.._ Vol. xiii. 1855. N. v. Kokscharow.—Ueber Klinochor von Achmatowsk am Ural 2. — Ueber den zweiaxigen Glimmer vom Vesuy, 10. J. F. Weisse.—Mikroskopische Analyse eines organischen Polir- schiefers aus dem Gouvernement Simbirsk, 18. Von Baer.—Kaspische Studien, 13, 20. Abich.—Ueber emen in der Nahe von Tula Statt gefundenen Erdfall, 22 (plate). A. v. Volborth,— Ueber die Prioritatsrechte der Trilobiten-Gat- tung Zethus, Pand., gegen die Gattung Cryptonymus, Eichw. H. R. Goeppert. __Ueber die fossile Flora der Permischen Gebilde, 382. _—_. Vol. xiv. 1856. Von Baer.—Kaspische Studien, ] (map). DONATIONS. 89 St. Pétersbourg, Bulletin de la Classe Physico-Mathématique de P Académie Imp. des Sc. Nat. de. Vol. xiv. 1856 (continued). Abich.—Sur les derniers Tremblements de Terre dans la Perse septentrionale et dans le Caucase, ainsi que sur des eaux et des gaz s’y trouvent en rapport avec ces phénoménes, 4. A. Moritz.—Ueber den Salzgehalt des Wassers an der Sudwest- kuste des Kaspischen Meeres, 11. Von Helmersen.— Ueber das langsame Emporsteigen der Ufer des Baltischen Meeres und die Wirkung der Wellen und des Eises auf dieselben, 13 (plate). Von Dittmar.—Zur geognostischen Karte Kamtschatka’s, 16 (map). N. von RoleaclieatsaBeiteane zur Kenntniss einiger Mineralien, 19: H. Abich.—Ueber ein schwefelreiches Tufgestein in der Thal- ebene von Dyadin, 8. Vol. xv. Von Baer. re cle Studien, 3, 6, 12. N. von Kokscharow.— Ueber zwei Topaskrystalle aus Nerts- chinsk, 19. Compte Rendu de Académie Impériale des Sciences de St. Pétersbourg, 1852, 1853. Géologie, 38. eee EM as BBS, 1854. Géologie, 36. ee ee L oo. ———. 1854 et 1855. 1856. Minéralogie, 94. Géologie et Paléontologie, 97. Society of Arts, Journal. Nos. 241, 242-258. (July to October.) Gold in British Guiana, 632. Artesian Wells in the Sahara Desert, 640. -—. Nos. 1-6, 23, 32, 109, 110, 132, 161, 164, 166, 167, 171, and 218. Statistical Society, Journal. Vol. xx. part 3, September 1857. List of Fellows, 1857. ptodbdidtn. Kongl. Vetenskaps-Akademiens Handlingar for Ar 1854. Sednare afdelningen. A. Erdmann.—Uto Jernmalmsfalt i Stockholms Lan, 241 (19 plates). H. v. Post.—Om Sand*sen vid Senne i Westmanland, 345 (2 plates). —-. Konigliga Svenska Vetenskaps-Akademiens Handlingar. Ny Foljd. Forsta Bandet. Forsta Haftet. 1855. 4to. A. Erdmann.—Om de iakttagelser ofver Vattenhojdens och Vin- darnes forandringar, som nyligen blifvit vid atskilliga fyr- baks-stationer Sveriges Kuster tillvagabragta ; jemte Tabel- lariska sammandrag af observationerna for aren 1852-55, 247 (2 plates). ne . —— 90 DONATIONS. Stockholm. Ofversigt af Konigl. Vet.-Akad. Férhandlingar Tret- tonde Argangen 1856. 1857. Erdmann.—Vattenstandet 1 Malaren och Saltsjon 1855, 11. Vattenmarken vid Stockholm, 189. Vikersgards-grufvan, 205. Nilsson.—Saurier och fiskar i Skanes Kritformation, 47. V. Post.—Sandasen vid Képing, 1. Kross-stensbaddar 1 Skedvi Socken, 235. . , Ars-Beriittelse om botaniska Arbeten och Upptackter under Ar 1852. Till Kongl. Vetenskaps-Akademien afgifven J. Em. Wikstrom. 1857. ————. Berattelse om botaniska Arbeten och Upptackter under Aven 1853 och 1854. Till Kongl. Vetenskaps-Akademien afgif- ven af N. J. Anderson. 1856. Berattelse om Framstegen i Insekternas, Myriapodernas och Arachnidernas Naturalhistoria for 1853 och 1854, till K. V.-Ak. afgifven af C. H. Boheman. Stuttgart. Wiirttembergische naturwissenschaftliche Jahreshefte. Achter Jahrgang. Drittes Heft. Zweite Abtheilung. 1857. Plieninger.—Belodon Plieningert, H. von Meyer, 389 (6 plates). Elfter Jahrgang. Drittes Heft. Turin. Mennce della Reale Accademia delle Scienze di Torino. Serie seconda. Tomo xvi. 1857. Cantu’.—Acque minerali di Recoaro, xciv. A. Sismonda.—Studii sulla mineralogia sarda, xevi. De Vecchi.—Osservazioni Geologiche fatti nei dintorni di Bala- klava e di Kamara, xevii. E. Sismonda.—Sur le terrain nummulitique supérieur du Dego, des Carcare, &c. dans !Apennin Ligurien, 443. Tyneside Naturalists’ Field Club, Transactions. Vol. iii. Part 3. J. Hogg.—Anniversary Address, 163. ———— Vienna. Sitzungsberichte der Kaiserlichen Akademie der Wissen- schaften. Math.-nat. Classe. Vol. xx. Parts 2 and 3. April and May, 1856. Lang.—Untersuchung iiber die Structur des Quarzes, 392 (4 plates). Leydolt.—Ueber den Meteorstem von Borkut, 398. Ettingshausen.— Bericht tiber das Werk ‘ Physiotopia plantarum Austriacarum,’ 407 (10 plates). . Register zu den zweiten 10 Banden der Sitzungsberichte (Band 11-20) der math.-nat. Cl. der K. Akad. Wissensch. Vol. xxi. Part 1. June 1856. Pokorny.— Ueber die Darstellung emiger mikroskopischer botan- ischer Objecte durch Naturselbstdruck, 6 (plate). Pebal.—Notiz iiber das kobaltsaure Kali, 169. ol . DONATIONS. 9] Vienna. Sitzungsberichte der K. Akad. Wissensch. Vol. xxi. Part 2. July 1856. Zeuschner.— Ueber eine alte Langenmorane im Thale des Biaty Dunajee bei dem Hochofen von Zakopane in der Tatra, 259. Pokorny.—Darstellung physiotypischer Pflanzenabdriicke, 263 (3 plates). Laurentz.—Fossiles Harz von Brandeis! bei Schlan in Bohmen, 271. Haidinger.—Die hohlen Geschiebe aus dem Leithagebirge, 480 (plate). Bene. sD cbet einige Quellen in Gainfahrn, 533. Oppel und Suess.—Ueber die muthmasslichen Aquivalente der Kossener Schichten in Schwaben, 535 (2 plates). Fillippuzzi.—Indagine chimica sopra I’ aqua della- fonte felsinea in Valdagno, 361. a Tageblatt der 32. Versammlung deutscher Naturfor- scher und Aertze in Wien im Jahre 1856. Nos. 1-8. September 1856. Geology.—v. Haidinger, 30; Heer, v. Russegger, 50; Foetterle, Hornes, 51; v. Hauer, 70; Beyrich, v. Strombeck, Lipold, 71; Schiibler, 71; Hornes, Knopfler, Heis, Porth, 95; Carnall, 96; Ehrlich, 113; Rose, v. Kovats, 114; Karsten, 115; Bornemann, Grailich, Braun, Szab6, 116; Suess, 117; v. Hauer, 138; Cotta, 139; Carnall, v. Hauer, Heer, Cotta, Hornes, Rose, 140; Bornemann, Klipstein, 141. Zoological Society of London, Proceedings. Nos. 314-326**, Title- page for Part 24 (1856), and Nos. 327-333. ————. Transactions. Vol. iv. Part 4. 1857. Il. GEOLOGICAL CONTENTS OF PERIODICALS PURCHASED FOR THE LIBRARY. Annals and Magazine of Natural History. 2nd Series. Vol. xx. No. 115. July 1857. Schmidl.—The Baradla Cavern, near Agtelek, Hungary, 79. No. 116. August 1857. EK. J 6 Ma roe nner of Cryptoceras in Silurian Rocks, G. hes yor ee Sb acae LOD: : : No. 117. September 1857. J. Lycett.—The sands intermediate to the Inferior Oolite and Lias of the Cotteswold Hills, compared with a similar deposit upon the coast of Yorkshire, 170. P. B. Brodie.—The Lias of Barrow, in Leicestershire, compared with the lower part of that formation in Gloucestershire, Worcestershire, and Warwickshire, 190. 92 DONATIONS. Annals and Magazine of Natural History. No. 117 (continued). H. Falconer.—On the species of Mastodon and Elephant occur- ring fossilin England, 231. C. Gould.—Tropifer levis from the Lias Bone-bed, 234. T. H. Huxley.—Pygocephalus Cooperi from the Coal-measures, 235. No. 118. October 1857. Dunker und von Meyer’s Palzeontographica. Vol. v. Part 2, 1857. A. W. Stiehler.—Beitrage zur Kenntniss der vorweltlichen Flora des Kreidegebirges 1m Harze, 47 (3 plates). Vol. vi. Parts 2 and 3. H. von Meyer.—Reptilien aus der Stemkohlen-Formation in Deutschland, 59 (9 plates). Leonhard und Bronn’s Neues Jahrbuch fiir Mineralogie, Geognosie, Geologie und Petrefakten-Kunde. Jahrgang 1857. Drittes Heft. Bunsen.—Ueber die chemische Zusammensetzung des Meteor- Eisens von Atacama, mit emer geschichtlichen Eimleitung, 257 (plate). J. G. Egger.—Die Foraminiferen der Miocan-Schichten bei Or- tenburg in Nieder-Bayern, 266 (11 plates). Letters: Notices of Books, Mineralogy, Geology, and Fossils. 1857. Viertes Heft. Fr. Roemer. Lae we Hollandische Diluvial-Geschiebe, 385. C. Bergemann.—Mineral-Analysen, 393. J. C. Deickie.—Saulenformige Absonderungen in den Gesteinen der Molasse, und polirte Flachen in Nagelflue-gerdllen, 401. R. A. Philippi.—Beitrag zur Kenntniss der Tertiar-Formation in Chile, 404. HG; Brom. .—Ueber die fossilen Emdriicke der Regen-Tropfen, 40 Letters: Notices of Books, Mineralogy, Geology, and Fossils. Edinburgh New Philosophical Journal. New Series. No. 11. Vol. vi. No. 1. July 1857. T. S. Traill.—Occultation of Rivers, 39. C. Richardson.—Chronological remarks on the River Wye, 43. H. How.—Natro-boro-calcite with Glauber’s Salt in the Gypsum of Nova Scotia, 54. W. L. Green.—Cause of the pyramidal form of the outline of the Southern extremities of the great Continents and Peninsulas of the Globe, with considerations on its subsidences and Volcanic lines, 61 (plate). L. Blodget.— Distribution of Rain in the temperate latitudes of North America, 93 (plate). A. A. Hayes.— Phosphate of Lime in Sea-water, 103. D. Forbes.—Chemical composition of some Norwegian Minerals, part 3 (Orthite and Calcite), 112. Duke of Argyll.—Roche moutonnée on a hill between Loch Fyne and Loch Awe, 153. DONATIONS. 93 _ Edinburgh New Philosophical Journal. No. 11 (continued). C. Maxwell.—The Earth’s Motion, 161. A. Taylor.—Carboniferous rocks of Linlithgowshire, 155. J. A. Smith. —Remains of Rein-deer found in Dumbartonshire, 165. A. Murray.—Fossils from Vancouver Island, 168. Fleming.—Chalk-flints of the Forth, 169. J. M‘Bain.—Fossil fish and plants from beneath Arthur’s Seat, 170. G. Lawson.—Dust-showers, 173. Gaudin.—Artificial sapphire, 180. Nickles.—Fluorine in Mineral Waters, 181. C. Maclaren.—Tertiary fossils of Pikermi in Greece, 182. W.S.Symonds.—Paleozoic fossils of Kidderminster and Malvern, 184. Newberry.—Geology of Northern California and Oregon, 184. E. Hitchcock.—A fossil in the Connecticut River Sandstone, 185. ——<—S. ———. ——.. No. 12. Vol. vi. No. 2. October 1857. W. Crowder.—Chemistry of the Iron-manufacture of Cleveland District, 234. W.S. Symonds.—A new species of Eurypterus from the Old Red Sandstone, Herefordshire, 257, 313, James Nasmyth.—Some phenomena in connexion with Molten Materials, 297. Hennessey.—The direction of gravity at the Earth’s surface, 298. Murchison and Salter.—Silurian rocks and fossils of the N.W. Highlands, 311. S. Haughton.—Fossil stems in the Yellow Sandstone of Hook Pomt, 312. R. Harkness.—Records of a Triassic Shore, 313. Dunoyer.—Junction of the Slates and Granite of Killiney Hill, county Dublin, 313. Meneghini.—Geology of Tuscany, 313. R. Griffth.—Suilurian rocks of Ireland, 313. Jukes, Dunoyer, and Salter—Geology of Dingle Promontory, 314. James Yates.—Coniferous fruit from the Greensand, 314. O’Kelly.— Fault at Slevenamuck, 314. G. H. Kinahan.—Igneous rocks of Valentia, 314. W. B. Rogers.—Paradoxides near Boston, 314. R. Mallet.—Fourth Report upon Earthquake-phenomena, 315. H. C. Sorby.—Slaty cleavage, 316. W. King.—Cleavage, 316. R. Harkness.—Jointing and dolomitization of the Lower Carbo- niferous Limestone of the county of Cork, 316. Clarke.—Raised Beach in the county of Waterford, 317. Hennessey.—Changes of the Earth’s structure and changes of the sea-level, 317. R. Godwin-Austen.—Granite-boulderinthe chalk of Croydon,318. H. Schlagintweit.—Erosion and Cleavage, 318. W. Hopkins.—The conductive powers of various rocks, 319. T. Oldham.—Geological Survey of India, 320. 94 DONATIONS. Edinburgh New Philosophical Journal. No. 12 (continued). W. H. Baily.—Fossils of the Carboniferous Limestone of Limerick, 325. — A new fossil Fern from the Coal-measures, near Glin, ‘county Limerick, 326. J. Birmingham. —The Drift of West Galway and of the Eastern parts of Mayo, 326. F. J. Foot.—Geology of part of the county Kerry, 327. R. Harkness.—Geology of part of Cumberland. W.S. Symonds.—Fossils from the Drift of the Severn Valley, 328. E. P. Wright.—The Mitchelstown Cave, Tipperary, 334. Pierce.—Form of the Continents, 348. James Hall.—Source of the materials of the Palzozoic rocks, and origin of the Appalachian Mountains, 348. J. W. Dawson.—Sternbergia, 349. W. E. Logan.—Azoie Rocks of Canada, 349, 350. T. S. Hunt.— Mineral waters and Magnesian rocks, 349. G. H. Cook.—Subsidence of the coast of New Jersey, 349. T. S. Hunt.—Metamorphism of the Sedimentary Rocks, 350. J. D. Dana.—Trilobites in the Potsdam Sandstone, 350. J. W. Dawson.—Newer Phocene fossils of the St. Lawrence Valley, 351. C. Whittesley.— Fluctuations of Level im the American Lakes, 3 A. C. Ramsay.—Breaks in the British Rocks, 353. E. Hitchcock.—Connecticut River Sandstones, 354. Swallow.—Geology of Missouri, 354. J. S. Newberry.—Mode of formation of Cannel Coal, 368. Gold in British Guiana, 376. III. GEOLOGICAL AND MISCELLANEOUS BOOKS. Names of Donors in Italics. Allman, G. J. Monograph of the Freshwater Polyzoa. From the Ray Society. Archiac, Vicomte d’. Notice Biographique sur Mercier de Boissy. 1857. Notice sur la Vie et les Travaux de Jules Haime. 1857. Bache, A. D. On the Tides of the Atlantic and Pacifie Coasts of the United States; the Gulf Stream; and the Earthquake- waves of December 1854. From Sir C. Lyell, F.G.S. Bavaria. Magnetische Ortsbestimmungen an verschiedenen Puncten des Koénigreichs Bayern und an einigen auswartigen Stationen. Von Dr. J. Lamont. Part 2. 1856. Beskow, Bernh. v. Om forflutna tiders svenska Ordsboks-foretag. 1857 DONATIONS. 95 Brodie, P. B. On some species of Corals in the Lias of Gloucester- shire, Worcestershire, Warwickshire, and Scotland. 1857. Carter, H. J. Memoirs extracted from a compilation entitled “‘Geo- logical Papers on Western India.” 1856. Description of some of the larger forms of fossilized Foramini- fera in Seinde, with observations on their internal structure. Memoirs on the Geology of the South-east coast of Arabia. Summary of the Geology of India. Collomb, HE. Mémoire sur les Glaciers actuels. Delesse, 4. Mémoire sur la Minette. Notice sur les Mines de Cuivre du Cap de Bonne- Espérance. 1855. Dennis, J. B. P. On the Microscopical characters of certain so- called Cetacean bones associated with Cetotolites im the Detrital Bed of the Red Crag at Felixstow, Suffolk. Deshayes, G. P. Description des Animaux sans Vertébres décou- verts dans le Bassin de Paris. Livr. 1 et 2. 1857. Deville, Ch. St.-Cl. Etudes de Lithologie. 8vo. Paris, 1850. Observations sur la nature et la distribution des fume- rolles dans léruption du Vésuve du 1* Mai 1855. From Sir C. Lyell, F.G.S. Dewalque, G. Description du Lias de la Province de Luxembourg. Duchessaing. Observations sur les formations modernes de l’ile de la Guadeloupe. From Sir C. Lyell, F.G.S. Dundonald, The Earl of. Brief extracts from memoranda on the Use, Properties, and Products of the Bitumen and Petroleum of Trinidad. 1857. Erdmann, A. Om de iakttagelser ofver vattenhojdens och vindarnes forandringar, som nyligen bliifvit vid atskilliga fyrbaks-stationer kring sveriges kuster tillvagabragta ; jemte tabellariska samman- drag af observationerna for aren 1852-55. Fleming, A. Report on the Salt-range, and on its Coal and other Minerals. From Sir C. Lyell, F.G.S. Fournet, J. Détails au sujet de la formation des Oolites Calcaires. Geinitz, H. B. Die geognostischen Verhiltnisse in den Umgebungen der Stadt Chemnitz. Entwurf zu einem neven Ae 1857. Ueber die geologischen Verhaltnisse des Plauenschen Grundes. 1857. . Ueber die Wiederaufnahme des Silberbergbaues bei Hockendorf im Thale der wilden Weiseritz. — = 96 DONATIONS. Goeppert, H. R. Beispiel einer merkwirdigen Verbanderung. ——. Die Tertiare Flora von Schossnitz in Schlesien. 1855. Die Tertiar-flora auf der Insel Java, nach den Entdeck- ungen des Herrn Fr. Junghuhn. 1854. Ueber ein in hiesigen k6nigl.-botanischen Garten zur Erlauterung der Steinkohlen-Formation errichtetes Profil. ——. Ueber die Braunkohlen-Formation in Schlesien. Ueber die fossile Flora der Quadersandsteins von Schle- sien und der Umgegend von Achen. 1841. Ueber die gegenwartigen Verhaltnisse der Palaontologie in Schlesien, so wie tiber fossile Cycadeen. ————. Ueber pflanzenahnliche Hinschlusse in den Chalcedonen. 1848. Guiet, EH. L. Premictre Lettre Géologique adressée a l Académie des Sciences et aux principales Sociétés Savantes de Paris et des Départements. Gutberlet, H. W. K. J. Ejnschltisse in vulkanoidischen Gesteinen. From Sir C. Lyell, F.G.S. . Ueber das Vorkommen und die Aufbereitung des Edder- Goldes. From Sir C. Lyell, F.G.S. . Ueber die Zeit-Folge der hoheren Oxydation des Mangan- und Eisen-Oxydules und ihre geologische Bedeutung. From Sir C. Lyell, F.G.S. Ueber Schwarzbraunstein im Trachytporphyr der Rhon. From Sir C. Lyell, F.G.S. Hall, James. Descriptions of New Species of Palzeozoic Fossils from the Lower Helderberg, Oriskany Sandstone, Upper Helderberg, Hamilton, and Chemung groups. Haughton, 8S. The Lower Carboniferous Beds of the Peninsula of Hook, County of Wexford. From Sir C. Lyell, F.G.S. Hermann, F. B. W. von. Ueber den Anbau und Ertrag des Bodens im K6nigreiche Bayern. I. Abtheilung. 1857. Jolly. Ueber die Physik der Molecularkrafte. 1857. Madras. Exhibition of Raw Products, Arts, and Manufactures of Southern India, 1855. Reports by the Juries. 1856. From the Commissioners of the Madras Exhibition. Marcou, J. Cours de Géologie paléontologique : Lecon d’ ouverture. 1856. ——_———. Lettres sur les Roches du Jura et leur distribution eéographique dans les deux Hémisphéres. Prem. Livr. 1857. Martius, C. F. Ph. von. Denkrede auf Christian Samuel Weiss. 1857. ee OO DONATIONS. 97 Michelin, H. Description de quelques nouvelles espéces d’ Echino- dermes fossiles. From Sir C. Lyell, F.G.S. . Note sur quelques Echinides fossiles. From Sir C. Lyell, F.G.S. Notice sur un genre nouveau a établir dans la famille des Spatangoides sur le nom de Mera. From Sir C.Lyell, F.G.S. Museum of London Antiquities. 1857. From C. R. Smith, Esq. New York. Documents relating to the Colonial History of the State of New York, procured in England, Holland, and France, by J. R. Brodhead. Edited by E. B. O'Callaghan. From the State of New York. Vol. i. Holland Documents 1603-1656. 1856. Vol. ni. London Documents 1614-1692. 1853. Vol. iv. London Documents 1693-1706. 1854. Vol. v. London Documents 1707-1733. 1855. Vol. vi. London Documents 1734-1755. 1855. Vol. vu. London Documents 1756-1767. 1856. Vol. ix. Paris Documents 1631-1744. 1855. Otto, E. von. Callianassa antiqua, Oito, aus dem untern Quader von Malter in Sachsen. From Dr. Geinitz, For. Memb. G.S. Page, F. J. Report of the Exploration and Survey of the River La Plata and Tributaries. From Sir C. Lyell, F.G.S. Ratti, F. Sul Laghetto di recente formation nella Vicinanze di Leprignano. 1857. Reeve, L. Conchologia Iconica: Avicula, Capsa, Capsella, Psam- mobia, and Sanguinolaria. 1856-57. Rennie, G. On the quantity of heat developed by water when violently agitated ; and experiments to determine the resistance of a screw revolving in water at different depths and velocities. 1857. Roemer, Ferd. Ueber neue Fischreste in schwarzen Thonschiefern in dem Dorfe Klein-Neundorf, unweit Lowenberg. From Prof Goeppert, For. Memb. G.S. Rose, G. Ueber den sogenannten Babylon-Quarz aus England. From Str C. Lyell, F.G.S. Santagata, D. Origine delle orgille scagliose dal calcare compatto dal macigno dall’ arenaria e da un conglomerato ofrolitico. From Sir C. Lyell, F.G.S. Schmidt, C. Ueber die Devonischen und Silurischen Thone Liv- und Ehst-lands. 1856. Schrenk, A. G. Reise nach dem Nordosten des europaischen Russ- lands, durch die Tundren der Samojeden, zum Arktischen Ural- gebirge. Zweiter Theil. Wissenschaftliche Beilagen. 1854. VOL. XIV.—PART I. H 98 DONATIONS. Sismonda, E. Notizia storica dei Lavori falti dalla Classe di Scienze fisiche e matematiche nell’ Anno 1855. Note sur le Terrain Nummulitique Supérieur du Dego, des Carcare, &c. dans l Apennin Ligurien. Spratt, T. A. B. On the Geology of Malta and Gozo. Second Edition. From the Colonial Office. Stein, W. Chemische und chemisch-technische Untersuchung der Steinkohlen Sachsens. (Die Steinkohlen des Konigreichs Sach- sen. Zweite Abtheilung.) 1857. From Prof. Geinitz, For. Memb. G.S. Stur, D. Ueber den Einfluss des Bodens auf die Vertheilung de Pflanzen. From Sir C. Lyell, F.G.S. Toronto. Observations made at the Magnetical and Meteorological Observatory at Toronto in Canada. Vol. ii. for 1846-1848, with Abstracts of Observations to 1855 inclusive. 1857. From the British Government. Trimmer, J. The Keythorpe System of Land-drainage. Victoria. Second Meteorological Report, with diagrams of barometric pressure, &c. By R. B. Smyth. Melbourne, 1857. From R. B. Smyth, Esq., F.G.S. Villa, A. Intorno tre opere di Malacologia del Sig. Drouet di Troyes. 8vo. Milan, 1856. Notizie intorno al genere Melania. Villa, G. B. Ulteriori osservazioni geognostiche sulla Brianza. Vogel, E. Ein neuentdeckter Schmetterling aus Spanien. From Prof. Geinitz, For. Memb. G.S. Witt, H. M. Chemical examination of certain Lakes and Springs on the Turko-Persian frontier near Mount Ararat. From Sir C. Lyeli, F.G.S. Zschau, K. Ueber einen Monazit aus Norwegen. From Dr. Geinitz, For. Memb. G.S. THE © QUARTERLY JOURNAL. OF THE GEOLOGICAL SOCIETY OF LONDON. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. JUNE 3, 1857. William Reed, Esq., M.R.C.S., York, was elected a Fellow. The following communication was read :— On the species of Mastopon and ELEPHANT occurring in the fossil state in ENGLAND.—Part I]. Evernas. By H. Fatconer, M.D., F.BS., F.G.S. [The publication of this paper is unavoidably postponed. | [ Abstract. | In the introductory portion of Part I. of this Memoir*, the author alluded to the ambiguity that has existed relative to the mammalian faunze of the Miocene and Pliocene periods, in consequence of paleeon- tologists confounding several distinct forms of Mastodon, of different geological ages, under one name (M. angustidens) ; and on this occasion Dr. Falconer stated, that, in the application of the name Elephas primigentus (Mammoth) to a multitude of elephantine re- mains from various superficial and deep deposits, over a vast extent of territory, and of different ages, a similar, if not a greater, amount of error and confusion had arisen. In fact, at least half the habitable globe has been assigned to the * Quart. Journ. Geol. Soc. vol. xiii. p. 308. VOL. XIV.— PART I. G 82 PROCEEDINGS OF THE GEOLOGICAL society. [June 3, Mammoth as his pasture-ground, if we were to accept the determi- nations of all those who have written on the remains of Elephas pri- migenius. The duration, too, of this nominal species in time is equally remarkable, so considered ; since, as it has been quoted from the lower and the upper pliocene beds, as well as from the post- pliocene glacial gravels, it ought to have existed before the European area received its present geographical form, and indeed before the Alps, Apennines, and Pyrenees reached their present elevation. After noticing the difficulty met with by the geologist in the classification of the newer Tertiaries, on account of this supposed ubiquitous presence of the Mammoth, the author proceeded to show that several species, belonging to two distinct subgenera, have been generally confounded under the name of Elephas primigenius ; and that each had its limited range in geographical area and geological time. The present condition of the nomenclature of the subject, and the history of the established species of European fossil Elephants *, namely F. (Loxod.) meridionalis, FE. (Loxod.) priscus, EL. (Eueleph.) antiquus, and E. (Eueleph.) primigenius, preceded an explanation of the principles on which the species are determined, and a description of the dental characters by which the Elephants are divisible into sub- genera,—a succinct account of which was given in the former part of the Memoir(vol. xiii. p.462). The “‘intermediate molars” in Elephants have never less than six divisions of the crown, and sometimes as many as eighteen. These molars have not all an equal number of ridges: some Elephants have an augmentation of only one ridge to the crown of the penultimate of these molars; these are ‘“ hypisomerous,”’ namely Stegodon and Loxodon; others, in which the number of the ridges progressively increases, are “anisomerous,”’ and form a third natural group, namely the Luelephas or Elephas proper. The Stego- don has four species, fossil in India; and approaches the Mastodon in the form of the molars. The Zowodon includes the existing African Elephant and three fossil species, and is characterized by its distinct rhomboidal discs of wear on the grinders. Euelephas has thin-plated molars ; but in some species there are intermediate stages, as regards the angular mesial expansion of the plates, between it and Lowxodon. Dr. Falconer next proceeded to review some well-ascertained mam- malian faunze localized in certain parts of Europe, where the con- ditions of deposit are most simple, and to apply the results to the more complex instances, where the remains of more than one distinct fauna are intermingled, or so closely deposited as to be too readily confused by collectors.. With this view, the author instanced the Subapennine or pliocene deposits of the Astesan, and elsewhere in Piedmont and Lombardy, where M. (Trilophodon) Borsoni, M. (Te- tralophodon) arvernensis, E. (Loxodon) meridionalis, E'. (Loxod.) priscus, and FE. (Euelephas) antiquus, with Rhinoceros leptorhinus, Hippopotamus major, &c., are found associated together. In the Subapennine beds of the Val d’ Arno, in Tuscany, M. (Tetralophodon) arvernensis and E. (Loxodon) meridionalis occur with the same Hip- * See the Tabular Synopsis, Quart. Journ. Geol. Soc. vol. xiii. p. 319. 1857. ] FALCONER—MASTODON AND ELEPHANT. 83 popotamus and Rhinoceros. Near Chartres, m France, #. (Lozo- don) meridionalis accompanies H. major and Rhinoceros leptorhinus. The above-mentioned are necessarily the leading mammalian forms of the older Pliocene period. North of the Alps pliocene deposits similar to those of Italy occur in some parts of Switzerland, but they are soon overlaid towards the north by a distinct mass of erratic drift of a different age and with different mammalian remains. In the fluviatile “‘Loess”’ or ‘‘ Lehm”’ of the valley of the Rhine, and in the Glacial Drift of the plains of Northern Germany, these post-plio- cene deposits contain remains of the true Mammoth, with the ticho- rhine Rhinoceros, the Musk-buffalo, &c., which thus constitute the leading types of the post-pliocene mammalian fauna. On the eastern coast of England, the Crag-deposits (the Red . and Norwich Crags) yield the pliocene M. (Tetralophodon) arvernen- sis, E. (Loxodon) meridionalis, and E. (Euelephas) antiquus; and the so-called Elephant-beds at Cromer, Mundesley, and Hasborough fur- _ nish 2. (Low.) meridionalis and E. (Euel.) antiquus, with Rhin. lep- torhinus and Hip. major. These characteristically pliocene fossils, however, are occasionally intermingled with the remains of the post- pliocene H. (Huelephas) primigenius, the latter fossils having been derived from the overlying and later drift-beds, which have thus proved a fertile source of the confusion and ambiguity already referred to. To some extent, similar conditions exist at Bracklesham Bay and Pagham Harbour, where molars of EL. primigenius are found in the upper gravels, whilst remains of LH. antiquus abound in the older mud- deposit, lately described in the Society’s Journal by Mr. Godwin- Austen. Dr. Falconer then considered the fiuviatile deposits of the Valley of the Thames, in relation to their Elephantine remains ; especially at Grays Thurrock and Brentford. At the former place the author recognizes the true pliocene assemblage of EF. (Loxodon) priscus, E. (Euelephas) antiquus, Hippopotamus major, and Rhinoceros leptorhi- nus; but the group of mammals found at Brentford, according to the published determinations, indicate the close proximity of both the pliocene and post-pliocene faunz at different levels of the same section. The Grays Thurrock deposits, and the lower beds at Brent- ford were inferred to be of an earlier age than any part of the Boulder-Clay or Till. The grouping of the LZ. pr imigenius, Rhinoceros tichorhinus, Bu- balus moschatus, &c., in the newer gravels of England and elsewhere was next dwelt upon, as affording an additional clue to the tracing of the several characteristic mammalian faunas over the European area. To the possible objection of there being too many large Probos- cideans grouped in one fauna, the author replied that the bones of Elephantine animals of three distinct species actually occur together in one stratum in Italy, and that six species are found in deposits of one age in the Sivalik hills. Dr. Falconer concludes that the same mammalian fauna existed throughout the period during which both the Crag and the fluviatile beds of the Thames Valley were being deposited; and that a chro- G2 84 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, nological division of the newer Tertiaries into older Pliocene, newer Pliocene or Pleistocene, and Post-pliocene is untenable; too much stress having been laid by authors upon the shell-evidence on this point. At the same time, it is not meant to be implied that all the species of the fauna ranged everywhere throughout the area: some in all probability were peculiar to the south, and others to the north. The presence of Hippopotamus major in the pliocene deposits was pointed out as being of great importance in indicating the character of the pliocene land, which, extending ‘between England and the Continent, must have afforded a great system of rivers and lakes, and probably had a comparatively warm temperature, as late as the deposition of the Grays beds, where also (as is well known) occur some southern freshwater shells, now extinct in England. After some remarks on the negative evidence afforded by this mam- _ malian fauna with regard to the supposed refrigeration of the land during the Pliocene period, Dr. Falconer reviewed the opinions of some English geologists on the physical conditions and faunze of this region during the newer Tertiary epoch, especially the views of Mr. S. Wood, Mr. Prestwich, and Mr. Trimmer; and concluded with a few remarks on the occurrence of EH. antiquus in the Cefn and Kirkdale Caves, and ‘of F. primigenius in Kent’s Hole, and on the non-existence of EL. primigenius south of the Alps, and its restric- tion in the United States of America to the Northern and Central States. In the Southern States and in Mexico a distinct fossil species, EF. (Euelephas) Columbi, hitherto undescribed, occurs along with remains of Mastodon, Mylodon, Megatherium, Horse, &c. JUNE 17,1857. Charles Preston Molony, Esq., Capt. Madras Army, Holles Street, Dublin, and George Robbins, Esq., Grosvenor Place, Bath, were elected Fellows. The following communications were read :— 1. On some ComPaRATIVE Sections in the Ooxitic and IRon- STONE Series of YORKSHIRE. By Joun Puiuuirs, M.A., LL.D., F.R.S., F.G.S., Reader in Geology in the University of Oxford. [Plate VI.] Introduction.— A geologist well versed in the Oolitic groups of the South of England or the North-west of France finds himself per- plexed by the first aspect of the coeval strata in the north of York- shire, which are so rich in bands of ironstone, layers of coal, and hundreds of beds of gritstone and shale, as to resemble a tract of old carboniferous, rather than a terrace of oolitic rocks. Nor are the features and physical geography more similar in the two districts— broad mountainous moor-lands in one, rich corn-laden hills in the other. On further research, the strong contrasts which thus appear between the series of the north and south of England are found to A or Of : | . if K | etal LIAS ar THIRSK. IRONSTONE Chatk. Tim: Clay. Middle Ookite. Lower Oofite. Lias. COMPARATIVE VERTICAL SECTIONS » txeSTR AT A or OOLITE & LIAS. GRISTHORP BOLTBY. LIAS THe COAST. ' LIAS ar THIRSEK. . ' | | | - 4 1 ll ' ; + SECTION ww tre OOLITIC DISTRICT or YORKSHIRE rom N. ro S. (FAULTS OMITTED) cS WN. = i 15) WonDs | . Vale of Picheraug eee Kan, Clay, U) Mudedle Oolete. Lewer Jolite. EEA s EEL lee TA CA A Vvtas. Carboniferous Parmar Toynalds 4 0? ith T Phallips del a zit | ¥ 1857. | PHILLIPS—OOLITE AND LIAS, YORKSHIRE, 85 be most remarkable in the group of the Bath or Lower Oolite, though some peculiarities worthy of notice occur in almost every part of the section between the Chalk and the Triassic formations, and even ex- tend to the Chalk itself. The author proposes, on a future occasion, to present a memoir on the Lower Cretaceous and Upper Oolitic deposits, including the Speeton Clay; but his remarks are now limited upwards by the Coralline Oolite and downwards by the Lias, both included. And they relate to the deposition and succession of strata, with some references to the distribution of organic life. It is now above thirty years since, following the steps of William Smith, I began to draw the parallels of geological time from the south of England into the north-eastern district of Yorkshire. Se- parated as these districts are by the nonconformity under the York- shire Wolds, and still more alienated by modifications affecting more or less all the strata, it was necessary to use great caution in select- ing the principal lines of contemporaneity. Guided by the evidence of organic remains and the succession of strata, we traced in the first place the continuous area of the Lias, and marked the place and value of the Marlstone, which Smith, first of all observers, had cha- racterized near Bath. We then defined the Kimmeridge Clay, Coral- line Oolite, Calcareous Grit, and Oxford Clay, and beheld with sur- prise a rock 60 or even 90 feet thick replacing the weak sands of Christian Malford, and holding in abundance the peculiar fossils of Kelloway Bridge. Even this was not achieved without some diffi- culty ; for the Coralline Oolite of Malton contains several fossils identical with, and others not easily separated from, frequent residents in the Inferior Oolite. Beyond this every fresh step was difficult at that time, and re- quires wary movements at the present moment. In my work on the Yorkshire Coast, published in 1829, the sec- tion of the cliffs was taken as a type, and the results then affirmed, after three complete surveys of the whole coast, have met with gene- ral acceptance. In one important point they have, indeed, been em- ployed by some of my friends with quite as high a trust in their con- tents as I ever felt,—for I have always regarded as a bold decision my reference of the grey limestone series of White Nab to the Forest Marble and Great Oolite of Bath ; and the shelly sandstones of Blue Wick to the Inferior Oolite of Somersetshire (see edition 1, 1829). On another point, the fixing of the Brandsby slate on a parallel above the assumed Great Oolite, though no doubt has been publicly expressed, my friends can hardly have avoided feeling it; for this rock is analogous to the Stonesfield slate, and that lies under the Oolite of Bath. By three separate investigations I have assured myself of the accuracy of my first determination ; and thus, if the place of the Great Oolite be rightly given in the sections of York- shire, the Brandsby stone is an equivalent of Hinton Sandstone or Forest Marble. It is not, therefore, for the purpose of a formal correction, or of an implied amendment of my published sections, that I offer this paper ; but for the purpose of recording variations in the deposits, 86 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, within the limited area chosen, which may throw light on the history of this peculiar type of the Oolites. This history has now acquired other points of interest than those long known to belong to it. The bands of ironstone which were noticed in several parts of my see- tions, and which, gathered in fragments on the beach, yielded a few hundred tons of iron in a year, when transported to Newcastle, are now so much explored in many of the interior hills and vales, as to feed long ranges of blast-furnaces on the Tees, and send half a million of tons of ore in a year to the great iron-works in the west of Dur- ham, by railways which bring back in return 100,000 tons of iron. In a few years this vast ‘yield’? will be doubled or trebled, for the iron-ore is inexhaustible, and what is now worked is much surpassed in richness by some as yet only beginning to be known. It must not be supposed that in every part of the district the Lower Oolites of Yorkshire fit themselves to any one section assumed as a type of their development in the north-east of the county: on the contrary, there occur great variations. Neither can the Bath type of the Oolites be adapted to the Midland districts of England, without some important changes. I propose to show, in the first place, what are the principal differences in Yorkshire, and, by com- paring these with the sections in North Lincolnshire and Oxford- shire, to show how real is the connexion and how great is the varia- tion of the several parts of this large Oolitic field. The Yorkshire coast furnishes one complete section of this series, measurable in every part, which has again and again been measured and remeasured by myself, both before and since the year 1829, the year of the publication of the ‘ Illustrations of the Geology of York- shire.’ I have no material change to make in this section; but in regard of the beds at Gristhorpe, which correspond to the Bath Oolite and the strata between it and Cornbrash, some details will be useful which were not needed in that «ra of geology. Prof. W. C. Williamson * and Prof. J. Morris + have already contributed some observations on this remarkable section, but they do not render it undesirable for me to give measures in detail. Coast Sections near Scarborough.—A vertical section of the beds on the Yorkshire Coast from the base of the Kimmeridge Clay to the top of the Lias, taken by measure from the face of the cliffs, with only the addition of the Upper Calcareous Grit in Silpho Brow, which is near the coast, is about 1120 feet in thickness, of which 420 feet belong to the Middle Oolitic formation in the subjoined proportions :— roo Me feet. . Upper Calcareous Grit (not seen on the coast, but observed = at Silpho, Pickering, Sinnington, &€C.) .......scecesseeeeees 60+ — S 8 | Corallime Oolite...........2.cccceeeessseseseeeerseseeeceeteeeeeceeees 60 on 4. Lower Calcarcous Grit.iicsc.vsetcvatsns sehen en ss.) eveeee nse 80 ef Oxford Clay. ccd odiscivekiiiped, fata ten Seeeden Dems ae 150 a2 4 Kelloway Roel; .,, (ceva. c-caversesesgea st eran ee ee 50 to 70 mo 8 (It is thicker in other places.) * Trans. Geol. Soc. 2 ser. vol. v. p. 223; and vol. vi. p. 143; Proc. vol. 11. Se + Quart. Journ. Geol. Soe. vol. ix. p. 317. 1857. | PHILLIPS—OOLITE AND LIAS, YORKSHIRE. 87 On comparing this with the corresponding section of the south of England, it may be remarked, that only near Weymouth is the Upper Calcareous Grit well exhibited, and that it is there associated © with Kimmeridge clay, and contains, like it, Ostrea deltoidea. Ihave \ seen this once in the Vale of Pickering im Yorkshire. Again we re- ° mark the extraordinary development of Kelloway rock in Yorkshire, to ten times its dimensions in’ Wiltshire ; while, on the other hand, the Oxford clay is reduced to one-fourth of the thickness which it has in the Midland Counties, and is a much more sandy and much less fossiliferous deposit. We now proceed to consider the Lower Oolitic formations. (See Sections 1 and 2, Pl. VI.) Section No. 1 is the well-known general section of the Lower Oolitic series near Bath, as it was understood and named by Smith. Section No. 2 is the corresponding series in Yorkshire. No. 1. No. 2. J. Cornbrash. f. Cornbrash. ; ( 3. Shales, sandstones, ironstones; 3. Hinton Sandstone. [ie ane ca eae ane ene i“ j 2. ee oolitic beds, ironstone; 1. Bradford Clay. * 1. Shales, sandstones, ironstones; | [ plants, coal, freshwater shells. d. Great Oolite. d. Oolite of Gristhorp. Upper Fuller’s-earth clays. Shales, sandstones, ironstones. ec. 4 Fuller’s-earth rock. c. , Beds of coal, plants sometimes Lower Fuller’s-earth clays. erect. 6. Inferior Oolite. 6. Dogger and oolitic ironstone. a. Sands over the Lias. a. Sands of Blue Wick. The two sections being drawn to occupy the same vertical space, the enormous extension of the sandy and the great contraction of the calcareous portions in Yorkshire, corresponding to the more littoral character of that region, is very apparent. There is also very little “clay,” as the term is used in the south of England, in this section in Yorkshire ; it is usually more shaly, often more sandy or even streaked ‘with sandstone laminze, so as to resemble what is called **lin and woon’”’ in Lancashire. The following observations supply a few details regarding the several groups / to a. jf. Cornbrash.—This is often not above 2 feet 6 inches thick, and in this small thickness is a parting. The top is ferruginous, and mostly very shelly; the lower part is shelly, and often contains _ root-like bodies at the bottom. Pale blue clay 4 or 5 feet below. In the strata (e 3) immediately below Cornbrash, clays and shales predominate over sandstones for about 80 or 100 feet ; then we have for the base of this series about 20 or 30 feet of sandstone, resting on pale clays, full of oblique lamination, often containing fragments of wood. The following is a summary of the beds as they appear in Gristhorp Bay,*, south of the island, the thicknesses being some- times measured, sometimes estimated. Total 121 feet 10 inches. * In one of my later examinations of the Gristhorp Section, I received no small help from Mr. Peter Cullen. 88 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, ft. in. JF. Cornbrash above. Pale clay, with some root-like masses resting on dark - Shaly clay’ ists. stip Seaesaneeeeereon te cucarares (cc ereeeeeds 5 0 a Thin skerry sandstone Baca aaseee rites cee desews +s ccasear set 0 4 = Pale Chayas ct daaiei oicivn dildo uotaatae te mere tees te 3ft.to 6 6 —e Skerry sandstone and shale, changing to solid sand- 2 g | BEOMG oases apes oh ons nis eeheUaltes geese ae eee peagr lft.to 6 O a Shale, darkens at the bottom (22. ccncacceceds«suceacararset 14 0 on White sandstone—“ pipy ””—with two thin partings... 5 6 2s Shale, growing dark at the bottom ..............-seeeeeee 6 0 23 23 Pale blue shale and laminated white sandstone (in one ee PIBCEATONSEONE) 5, oi cins'ssen acta cinna-ivmenestekay -ceeeemeene 8 0 ae Alternations of pale bluish and purplish shaly clay ... 9 0 che DhinWandstOUe es .cccicocsassesvaracces aseeeceaeeeeeesecees as Series of pale bluish and purplish shaly clays, with | 29 6 ae) : ; =a bands of nodules Of granular t70N-OFE.....6000..000. = Variable.erits and: SUBLeS .<\siecc«anesscaeacmensaindenaasantane 8 0 zc Variable sandstones, with layers of wood, the top very ES irony ; it is wunconformed on the beds below...12 ft. to 20 0 Pale clays, with a band of jet and some lumps of iron- stone at the bottom ............ we2is ss esnvceuadeaeecmsrmees 4 0 The thicknesses are all variable in a short distance, and the beds of sandstone vary in quality in a few yards. On the north side of the island, the lower part of this series, be- low the granular iron-ore bands, appears as under :— ft. in SAMOSHOME . ve cG ce vane aswirs gt awiovithtas clo SAA Rant emaMtataa sna: seme em emeeer 4 0 ALE: occ vanahat ceva t nde eeeenGns cea salute sickling «tecieueatnaiemn gapae i semeeeae 5 0 Sandstones, with shale partingS .........s.+.sescseeeesseevscevcseoeers 5 0 Sandstones and shales, in wedge-like alternations; the lowest shraleweny Warle™ 22 See hen tes Deca pene ncose ener: 16 ft.to 21 0 Irregular sandstone, with partings of shale and layers of wood, in the state Of jet Or. Oa): 25). ccs ascasserern=as sm eeeneee 1 0 2 J Sandstone, brown, yellow, &C..........0cc..csesssceseveeees 40 0 oe | The lower part sometimes very ferruginous ............ 3 0 Shale ‘andtronstone, balls os sascias sts anensaccens ces ckeesswanenn 3 0 Ferruginous and shelly oolite, resting on upper lias ...... i 2 The total thickness of the Lower Oolitic Series is thus found to be 489 ft. in this combination. If we now compare these sections measured on the actual coast and against the ancient sea-cliffs, we find in regard to the Middle Oolite formation only differences of thickness; the Oxford Clay being remarkably thinner near Thirsk, but the Kelloway rock thicker. But in all the strata below the Cornbrash the differences between the two sections are very great. The Cornbrash, as seen on the Yorkshire coast, is never above 5 feet thick. It contains several distinguishable parts—a thin part at the top rather laminated, and a part at the bottom, argillaceous, or actual clay ; while in the middle is one thick mass, or two beds, of shelly and somewhat ferruginous limestone, hardly oolitic. It contains Nucleolites orbicularis, Myacites securiformis, Ammonites Herveyi, and many other shells, but hardly a trace of Belemnites. Near Thirsk, and for a great breadth of the moorlands eastward of Hambleton, I have not clearly seenit. It is, however, conspicuous in Newton Dale, and thicker than on the coast. The series of sandstones and shales between the Cornbrash or Kelloway rocks and the calcareous beds which first succeed below, yields on the coast two bands of ironstone, and contains Cycadacee ; and one band (rich brown iron-ore) appears near Thirsk. The calcareous shelly beds below, which occur on the coast, and seem to lie in the place of the Forest Marble group of the south of England, appear under Hambleton at the base of the carbonaceous sandstone, and may perhaps be regarded as including the shelly nests in the lower part of the sandstone. A bed of Ostrea Marshit occurs in both situations, near the middle part of the shelly series ; a bed of Ostrea crassa lies towards the lower part at Hambleton ; but Belemnites and Terebratule have not been seen there, as at Gristhorp and Cloughton. Below this point there is great difficulty in tracing lines of con- temporaneity across the district from the coast to the inland cliff. If we suppose, in conformity with many observations, the Gristhorp plant-bearing series to be merely a local deposit, not seen at any i ee ale - 1857. | PHILLIPS—OOLITE AND LIAS, YORKSHIRE. 93 point north of Haiburn Wyke, nor in Staintondale Cliff, the grit, shale, and coal of Hambleton, 164 feet thick, will be below the whole of the Bath Oolite, and correspond to the Haiburn coal series. What in this case is the rough nodular “glance”’ oolite (2 feet) with Avicula, resting onrubbly sandstone, with Nucleolites, 18 feet ? Is it of the date of Stonesfield slate ? The Cricopora-beds of Gristhorp, below the coal series there, lose their distinctness in going northward and westward, so that they become untraceable ; on the other hand, we find the Belem- nitic beds to fail entirely toward the southward and westward. On a line which runs north and south between the coast and the Hambleton Cliff, and which thus partakes of both these negative geographical influences, neither of them is yet certainly known, though we may expect to find the upper set of beds; nor have we on that line any trace of the Gristhorp plants. The rough nodular “lance” bed is recognized, as I think, on the line of the Whitby railway, about 100 feet below the shelly beds of the Bath Oolite. Still less obvious are the lines of contemporaneity lower down in the thick series above the Inferior Oolite, when compared on the two parallels from north to south. On the coast are sandstones and shales, with zones of plants, but no calcareous bands, and no remark- able ironstone; under Hambleton, with a smaller thickness of are- naceous and argillaceous sediments, we have one or even two groups of white cement-nodules (compact argillaceous limestone), one con- taining Glyphie, a group of valuable ironstone-nodules, and even a 3-foot band of ironstone. These deposits are only seen in the western range of the Oolites. | The lowest part of the Bath Oolite formation on the Yorkshire coast consists of the ferruginous ‘“‘dogger,’’ with two bands of shells at the Peak ; under it isa group of grey, micaceous, soft, sandy rocks, apparently the ‘‘Gold Cap Sandstone” of Lyme Regis, ‘Sand of the Inferior Oolite’’ of Bath, and of the Cliff-hill of Lincolnshire. Under Hambleton these are represented by ferruginous oolites, con- taining Ammonites, Hyboclypeus, Trigonia, &c.; but this character of the rock, by which it approximates to the lower part of the sec- tions of Inferior Oolite in Gloucestershire, ceases as we proceed northward, and is modified as we proceed southward. On a line drawn from north to south between the coast and the Hambleton, we find the oolitic band at the top of the Lias very rich in iron. Ina part of Rosedale, especially, it is an oolztic tron- rock, the central part of a great mass on one side of the valley being very attractable by the magnet, and yields, at a maximum, about 50 per cent. of iron. Other Inland Sections.—We may now proceed to trace briefly the variations which take place in proceeding southward from the country of Thirsk toward the Humber and Lincolnshire, where something nearer the normal type of the Bath Oolites is recognized. Kilburn.—In the vicinity of Hood Grange, Hoodhill, and Kilburn, 94 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, the oolitic limestone (d) is frequently quarried; and below it, especially on the southern slope of Rowlston Sear, coal has been obtained within the memory of man only a few feet below the oolite. About Carlton, Coxwold, Newborough Park, and Owlton, the lime- stone is frequently exposed and dug in quarries; and here also coal has been found below it. At Newborough Park it was about 50 feet below the oolite, which is dug and burnt to lime. Brandsby.—Proceeding southward from the country of Thirsk to the parallel of Easingwold, in the Howardian Hills, about Brandsby and Gilling, we find the remains of old coal-works, ranges of limestone, and quarries of roadstone, presenting on the whole the following section :— WANGY SETICS, VEMOWISIT 22.2002 sco sne vied swesnes darddaese tania deeeee -) ft. in. Roadstone, 2 or 3, or 4or 5 feet; laminated sandy glance-lime- | stone, often full of shells, often in broad flat nodules, lying r 50 0 IN NOEb VEHOWION. SATO: 6.0.8 «as snes ack. Ssicty ence hence sodden PRY isaley Clam HElGW oo. cous ot Sanne eis napa -naeselaa- soe eee IAMULY SCRICS cyt ness suelncir tind dine dncaaess secets Se eee Soft shelly sandstone (at Brandsby) ..................eecceeeecees 30 0 Sulidiy Series Soest sete este er dedadeaese et POM eae : Hard laminated sandy glance-limestone ................ccceceuceeeees 4 6 Wale CUA oa 5 ke plein ica isin sles die!s aeaSeySiaie sie lain wim clsictalay ia ae ee I 3 TXONSEOME 4 (c.5< de ancsestanon neteachy + aoasetacd se ae Shale and carbonaceous grits. Signs of COAL ..........ee00. 0.00 50 0 On Gilling Moor a section is reported by Mr. Winch, ‘ Geological Transactions,’ First Series, vol. v. p. 545, &c., to the depth of 179 ft. 6 in., commencing with— aes PAMESTORG? 5.0 a6. cciemericicisnccacew-nee's anon aati 9 0 Grits aud pintes 222. 2°. >. 42-7 eee 27 0 Hard ‘bine *“Calliard’? *\. sc 23sec kek 2/2 Coal (a trace). Plate: aud soft orth 3.0 5:fane-cbeastt deustdes 30 0 Bile HIG GSbQUG s ciesss cies kno Fan eeaew epee 4 0 GGELES HEIGL PLADEN, Cane Ge emint sete ance wnat teas 95° 6 Coaster. nek Aneta 0 6 Shale ssh aided. ated. ded ends doar eee 2 8 At no point further to the south-eastward has the coal-seam been found worthy of opening,—it has indeed scarcely been traced ; but the oolitic limestone, a few yards or fathoms below which it lies, conti- nues distinct, and is quarried almost iu a connected line, by Col- ton, Dawby, and Terrington, to Bulmer and Crambe. The road- stone is found above it distinctly only a short distance, and can scarcely be identified beyond Terrington and Wiganthorpe. At Welburn, Bulmer, and Crambe, white cement-stones occur below the Oolite, as near Thirsk; and below these are oolitic ironstone and ferruginous sands, corresponding to the Dogger-series of Thirsk and the coast; but the strong white gritstones and most of the shales which lie between the Oolite and the Lias about Brandsby, Kilburn, and Boltby are almost absent from the banks of the Derwent. Crossing the Derwent, we trace in like manner the Oolite by 1857. | PHILLIPS—OOLITE AND LIAS, YORKSHIRE. 95 Westow to its disappearance (through unconformity) below the chalk at Kirby-under-dale. The rock emerges again from its eretaceous covering at Sancton, near Market Wrighton, ‘and is traced to Brough- on-Humber, where it is quarried above grey partly micaceous sand and sandstone, and is evidently equivalent to the Oolite of Lincoln- shire, which appears on the opposite shore of the Humber, and rests on sands, grey, red, brown or white, as these do on the Upper Lias. The only example which I propose now to present of the Lincoln- shire sections is that of Harpswell Hill, north of Lincoln, which was traced by myself in 1821, from the actual road-cutting*. The series begins with— White coltiae TMeSKONG: ...(ou sce. ansce- caves akenns 30 feet. eS CU BY ME SAU cn cam. os Sanne cee ukcdnncaeatedans 12 Rare pital eae eee tigas wan venta cade cs scbs vas usbeh eee: 3 ee J Sandy with BEIMI-IAUIS, Kota yn Das easunacncstngccccs scacee 10 aw WA FRIEACEOUS SANG «. ..... 2.000 scn~ess0500 ne eee Se? ge WRSIATENAIEEE oo. Sos aac carom cada ses cone anke os ie Wace 4 PelaWAIBIEIAUIE Goo 65, Ooo A Gie c Ncatatcmoacanpaccmentece. Brown sandstones and shells ............ sssceeseees 40 Blue Lias clays, succeeded by marlstone and Seger: WAR 5 ochemener neil Dens axes do eesee exposed 20 Above the white oolite are clays aa thin stony beds of the Forest Marble series and Cornbrash. These have been fully illustrated in South Lincolnshire by Prof. Morris}, and are found again with similar characters at many localities in Oxfordshire. This white oolite is perhaps generally admitted to be the Great Oolite of Bath,— a point on which I reserve my opinion ; it is certainly represented in Yorkshire by that of Cave, Westow, and Crambe. The Lias Formation.—The Lias varies not so much as the Oolites in a given geographical area, because for the most part its materials were accumulated from long and widely suspended fine argillaceous sediment. The main differences observable in Yorkshire relate to the upper part of this great series, and may be sufficiently illustrated by three actual sections, representing the succession of beds seen in the cliffs about Whitby,—measured in the works at Eston Nab,— and explored in a boring at Feliskirk, near Thirsk. The Lias of the Yorkshire coast is exhibited in a complete and magnificent section through all the upper and middle parts of the lower groups for above 500 feet in thickness ; about 300 feet of beds still lower being imperfectly traced in the interior. In general terms the ae stands thus (see Section No. 4, Pl. VI.) :— ( Alum-shale (80+ feet), including cement-nodules and Upper Lias ironstone-nodules. In the upper parts, gradually Shales diminishing downwards, are Discina reflexa, Nu- 200 fe oe cula ovum, Ammonites bifrons, A. heterophylius, - | and Belemnites tubularis. Abundance of Enalio- saurians. * See Memoirs of W. Smith, p. 97. + Quart. Journ. Geol. Soc. vol. ix. p. 317. + See Illustr. of Geol. of Yorkshire. Also a section of the Upper Lias and Marlstone, communicated to the Geological Society, by Mr. L. Hutton, 25th May, 1836; Geol. Proc vol. ii. p. 41. This is an elaborate series of the Lias in Rockcliff. > 96 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, feet Upper Lias ( Shale with nodules ............cccceseierccsciacceee 60 to 80 Shales, Jet-rock—shale with jet and pyrites ..........sseeeees 20 200 feet. } Hard SRMOY ROBIE is. suene greene eceseane teams? Us onc 20 to 40 Ironstone-band, or ironstone-rock, with irregular Ironstone — partings of shale. (Avicula cygnipes, Pecten equi- and NNEIVER)) "Sos: acinnaciam sxe aurea had eae taas aes 15 to 25 Marlstone < Shales and ironstone-bands.................sseeeee 50 to 76 Series, | Sandstone and shale, with Ophiuride, Cardium trun- ° 150 feet. catum, and many other fossils ..........00....00008 soe 0 \ Sandstone and shale ............ oupiaintaens “aa dekh Wks She 30 Lower Lias Shale below. The details of the great ironstone-bands above the marlstone appear in the following section, measured from the workings at Eston Nab*, and communicated to me by Mr. John Murley, C.E. These beds yield about 50,000 tons to the acre. ft. in. ft. in. - eee Ironstone: top block left as roof ............... 0 il (parting) | Tronstone’s ‘second DIGEK......002 ...-ceccenecece ans 2 3 [ (parting) rl7 0 Ironstone: main DOCK (iiss co2s secs sseanonssenacls 12-9 (parting) | Ironstone: bottom block (variable) ............ 1-10 ¥ 32 6° SHAG savewe semevnaas ewaes seanscsaanneee gers ce Pare ack ant 2.0 Tronstone-band ....0.5...cccenssssciececets BPE ee | es 2) 1b 6 BAG a wrtteatnens coceare a aeawetiestituensnecchenaceat is 6 0 Tronstome-band .. 55.2 sstcsnovaneeat ser csemcea eas oeed 0 10 | At Grosmont, near Whitby, the same series stands in this altered | and divided state, with about 8 feet of ironstone, yielding about — - 20,000 tons to the acre. ft. in. 1 PR ee 5 ta a Pe PS pe heed lor pach Mabe ae a Ironstone, ‘“ Pecten-seam’”’ in two bands, separated by 1 F056 ins. OF Shale: 0134.22 -cdcndceveueesaauceceeee ene 4 0 BIG thoy steno aaa nde anigy uae fade eeuiecanan emus. ta nee ee N 4.8 PRQTSEGNE ¢ SOO, 20s tesins oop yraene ecniasa tenes Reker 1 ee |RSS Ts Sa RE AoE RO aa BS 8 hte, Ni” 7 8 fronstone s eiOd") 6. Jew Cisenwee ech cdobareecets -aenttuat 1 6 PIGS. ia Seiten Wacken. Ole s liven s Rk eee eeerer Se eewee 18 0 Ironstone: “ Avicula-seam”’. joveiscisescucesanundess .chaeees 4 0 38 6 At Feliskirk, in the vicinity of Thirsk, a trial-bore was made, by my advice, through the upper lias, to the ironstone and marlstone, with the following result. The upper bed mentioned is the In- ferior Oolite capping the Lias, as at Thirsk, here very ferruginous (see Section No. 5, Pl. VI.):— | ft. in The oolitic iron-rock of Mount St. John ......... 6te).. 4am Shale, in the upper part cement stones ...............00 116 0 * An analysis of the Cleveland iron-ore from Eston is givenin Mr. Dick’s paper, Quart. Journ. Geol. Soc. vol. xii. p. 357. See also Mr. Crowder’s papers, Edinb. New Phil. Journ. New Ser. vol. iii. p. 286, and vol. iv. p. 49. 1857. ] PHILLIPS—OOLITE AND LIAS, YORKSHIRE. 97 ft. in Upper nodular band of ironstone ............esessseeeees 0. 7 SSR yrce te Ce oe iaielaie sw aie 0 Gee eearers inte Sia OO ee see Oats ede | Lower nodular band of ironstone ....0..........s00ceeeee OG Be ae eae ae ea Scie SBA oetee was ade oheeeewene Mehaee “eG WEARS WOT eo cae a eB nne CREE ARE nacmece DCO o Sch pec acocaeaAacernn ES Say, SALE eee seccsncscn tens cccweheesen sas BRS ose cen 4 20 0 Farther to the south this poor representation of the great Iron- stone and Marlstone series of the Yorkshire coast is traceable; until in Lincolnshire, Rutland, and Northamptonshire it resumes much of its thickness and importance, though not as yet its commercial value. - Conclusion.—On reviewing the facts here selected to illustrate and exemplify the variations of the middle and lower Oolites, and upper and middle portions of the Lias of Yorkshire, we find sufficient grounds to mark out approximately the geographical ranges of some remarkable mineral conditions—and accumulations of organic re- mains,—indicative of peculiarities in the depth and currents of the sea, the direction and proximity of land, and other great charac- teristics of the mesozoic period in this part of the earth’s surface. Reserving for another communication the development of this subject, which cannot be properly examined without additional de- tails, I desire to call attention in the mean time to a few prominent data. (See Section No. 6, Pl. VI.) The whole series of strata from the Cornbrash to the Marlstone, inclusive, grows thinner towards the south, and in a less degree towards the west; so that frem the sea-coast near Whitby to the hills near Thirsk the thickness decreases from 1000 to 590 feet. This appears in each of the main groups. Near Whitby and Guis- borough the marlstone and ironstone occupy 150 feet of the cliffs ; _ but near Thirsk only a few feet. The Upper Lias measures 200 feet near- Whitby, but near Thirsk less than 120 feet; and in this general diminution each part partakes,—though perhaps the upper part, which is the favourite seat of Nucula ovum and Ammonites bifrons, has been most severely truncated. The great series of sandstones, shales, coal-plants, and ironstones, lying above the Lias and below the Oolite of Gristhorp, 500 feet thick in the Peak and the grand range of cliffs at Staintondale, is only 270 feet thick near Thirsk, and is further reduced near Brands- by, until on the banks of the Derwent it is scarcely traceable. The upper carbonaceous series of the ccast is of nearly the same thick- ness at Thirsk, on a line from east to west; but the Oxford Clay diminishes from above 100 to less than 30 feet. Lines may be drawn in directions not deviating much from E.N.E. to W.S.W. which shall coincide with bands of equal deposition, or equal disappearance, of particular mineral sediments, and particular distributions of organic life. For these lines—as defining equality of earthy sediments,—and thus sometimes marking cut similarity of sea-depth and current-action—the author proposes the term “ iso- chthonal,”’ and is of opinion that the tracing of them will hereafter VOL. X1V.—PART I. H 98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, tend much to increase our knowledge of the physical conditions of definite epochs in geology. In the present case the normal to these lines, directed to the N.N.W., appears to the author to indicate the existence of land in that quarter during the whole of the period now under consideration, —land at no great distance, because of the pro- portion of many of the plants,-—the occurrence of Anodon and other inhabitants of fresh or brackish water,—and the occasional vertical position of Hguisetites. These latter facts, indeed, may require the admission of the presence of low marshy land within the area in ques- tion; but the author is more impressed by the probability of high and extensive land, which might yield to rivers, of some magnitude, the enormous mass of quartz-sand and mixed ferruginous sediments which abound between the truly marine limestones and subcalcareous shelly bands. It seems necessary to suppose some old palzeozoic land towards the north, not eminently granitic, but rather of the argillaceous, arenaceous, and quartzose type, with intermixed trap- rocks, such as the Lammermuir Range, which is now so abruptly truncated on its eastern side. If an isochthonal line be drawn from near Thirsk to Robin Hood’s Bay, it will be found that on the north-western side the ironstone band at the base of the Upper Lias is valuable for working—its value growing greater to the north-west. Nearly on this line the Inferior Oolite receives its maximum dose of iron, growing more and more sandy to the north-west, and losing its thickness and character to the south-east. If a line be drawn from near Coxwold to Scarborough, parallel to the preceding, it will nearly coincide with the north-western limit of really oolitic character in the calcareous beds of Westow and Gris- thorp, and with the south-eastern limit of the coal and freshwater deposits of the district. For a limited breadth north-west of this line, Belemnites Aalensis is found in the upper calcareous beds of the Gristhorp series—a position much above what is usual for this shell, —and it is associated at White Nab with Ammonites Blagdeni, equally a species more common in the Inferior Oolite of the South of England. The further development of this subject, the physical condition and depth of the sea-bed, the alternate influence of sea- and fresh- water in the same basin, and the relation of these rocks to those in Lincolnshire and Oxfordshire, must be left for another communi- cation. 2. On the OoxiTtE Rocks of GLOUCESTERSHIRE and NortTH Witts. By James Buckman, F.G.S., F.L.S., F.S.A., Professor of Natural History, Royal Agricultural College, Cirencester. [Plate VII.] Prefatory Remarks. — The object of the present paper is to point out the general geological characteristics of the different mem- bers of the Oolite rocks, as they occur in the Cotteswold Hills, Quart.Journ. Geol. Soc. Vol. XIV. Pl. WL | N.E. GLOUCESTER = a a — — 10 ¥, caer — — — or en el le ti tee olin etn en Sie ae oe a = = S=S5 Sess ae = = SS be soot) See ee ee aes = ———— —= 7 Oo é 6) SS : STRATTON ST. MARGARETS a = = = —— = — ———— 2S SS == es ev WANBOROUGH HILL : J.Buckman Gel. Reynolds & C2 lith. = az 3 cP 7 SECTION rrom BUR DLP to SWINDON, ae ie A trea TL Vor tical Seale 1600 Fest % GLOUCESTER VALLEY EATTON: CRICKLA STRATTON $f MARGARET S © « 2 Bitrcerate 5 a 5 == see Le cal (OY) Bay) Sees PORTLAND. JtMMERIDCE CORAL RAG. OXFORD CLAY. CORNMBRASH. FORASTIAR SDE. Gr VOTE. RETERSEARTH . CLAY. J.Buckman del. Reynolds & C2 With. ner + Aearinoeryen ary © Maw e ag : 5 - zy “tesserae 400% sate = Mt a ne aged. = — te ore 1857. ] BUCKMAN—OOLITES. 99 on as regards the extension of the higher beds into parts of North ilts. This will be done mainly with the assistance of two surveyed sec- tions which were made purposely for this paper ; one extending from the Vale of Gloucester through the bold Cotteswold scarp at Birdlip to the Chalk Hills in Wiltshire, in nearly a straight line from the N.E. to the S.W., to which is added a deviation to Swindon (PI. VII.); the other from Cirencester, over the Oolitic wolds, and on through the Vale of Moreton to Shipton-on-Stour, in a direction nearly north and south. These lines have been taken along the two principal Roman roads which run through Cirencester ; their general straight direction, and the many quarries and openings in and about their fosse, rendering them very suitable for the purpose. It may here not be out of place to state how these sections have been taken, as they are the result of much interesting labour, cheer- fully jomed in by a numerous party. The engineering portion was accomplished by Professor Armstrong, C.E., of the Royal Agricul- tural College, assisted by several of his pupils. By this staff of engineers the levels were surveyed, and wells, ponds,—whether na- tural or artificial,—quarries, and other physical features, were care- fully noted in their progress, so as to assist in the subsequent plotting, and to guide in determining geological lines. The geology of these sections has been laid down in journeys taken along the two lines, in company with a large party of my own class, for whom, and for all engaged, it has formed a labour of love, which has rendered Easter and other holidays periods of recrea- tion, notwithstanding the amount of work therein accomplished. The minor illustrative details I have collected during a period of many years’ residence and constant work among my native hills. For the occasional theoretical deductions I throw myself on the in- dulgent consideration of the Society. Before commencing with the more immediate subject of this paper, it may be proper to say a few words of the many workers in this district, as their names will show the interest which geologists have for a long time taken in that central chain of hills known as the Cotteswolds. To Smith and Lonsdale we are indebted for the first stratigraphi- cal details of the different members of thé Oolites ; and the paper of the latter in the Society’s Transactions * may be considered as a model of industry and accuracy, as the lines therein laid down have been but little interfered with by subsequent explorers. The ‘Geology of Cheltenham,’ by Sir R. Murchison, contri- buted largely to the elucidation of the Liassic and Oolitic rocks of the Cotteswolds ; whilst the publication of Morris and Lycett’s ‘Monograph of the Fossils of the Great Oolite,’ by the Palzeonto- graphical Society, has made us acquainted with a most interesting fauna, which has been largely added to by several members of the * Second Series, vol. iii. p. 341 ; see also Proc. Geol. Soc. vol. i. pp. 98, 111. H 2 100 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, Cotteswold Naturalists’ Club*, foremost amongst which the papers of Strickland, Brodie, and Woodward may be mentioned. Even while the notes for this paper were being collected, Mr. Hull, of the Geological Survey, has read a paper before our Society, has completed the map of a great part of the Cotteswolds, and published a ‘ Memoir of the Geology of the Country around Cheltenham, illus- trating sheet 44 of the Geological Survey’: all these reflect the highest credit on their author. Thus, these rocks especially, up to the Great Oolite inclusive, may be considered as having had no small share of attention bestowed upon them by different observers: not so, however, the beds above the Great Oolite ; as the details of these, in so far as the counties of Gloucester and North Wilts are concerned, have been but very par- tially worked out; and, indeed, the existence of the Oxford Clay in the Cirencester district was a matter not understood until lately. Here, then, it will not be out of place, if these Upper Oolite mem- bers should receive a large share of attention. The Oolitic rocks which we shall have to review may be thus tabulated in descending order :— 13. Portland Oolite . Portlandian . . Pervious to water. 12. Kimmeridge Clay. . S, . . Impervious. 11. Coral Rag . Sane" S . . Pervious. 10. Oxford Clay a . . Impervious. 9. Kelloway Rock ie ° Impervious partially. 8: Cornbrash:. © 3°74) f Pervious. 7. Forest Marble. . . | @ | Impervious. 6. Bradford Clay . | = d Impervious partially. 5. Great Oolite. . . . | joel Pervious. 4. Stonesfield Slate . . St Pervious. 3. Fuller’s Earth . | ; L Impervious. 2. Inferior Oolite 2°" ;.°..° 1" “so eo ee ees, LS PRAHSS \sP ps ce, GOST © lo) ote. 8 hee DEW te) Wor hE These rocks are all conformable, have a general dip from the N.W. to the 8.E., and have a very general evenness of stratification. This, however, is not a little interfered with by a series of downcast faults : these, and the alternations of pervious and impervious strata, have given rise to a very undulating country, the long axes of the valleys being for the most part in the line of dip, whilst a traverse in the line of strike offers a constant succession of hill and vale. At the North Cotteswolds the elevation of the hills is more than 1000 feet ; and here they offer bold scarps, overlooking the Vale of Gloucester ; the scarps, headlands, and gorges in the hill-sides having been formed by the water-action of the old Severn sea. As these facts, however, relate to the physical geology of the district, I pro- pose, in the first place, to give a description of the different deposits of the Oolites, and then, in a future paper, to attempt a description of the subsequent physical changes,—concluding with a detailed and comparative list of the fossil contents of the different strata. * See Proceedings of the Cotteswold Nat. Club, 1848-53. 1857. | BUCKMAN—OOLITES. 101 2. INFERIOR OOLITE. Basement-bed.—The line of separation of the Lias and the Oolites along the whole of the Cotteswolds has always appeared so well marked, both from structure and fossils, that until lately no prac- tical geologist has had the least difficulty in the matter; recently, however, from some papers by Dr. Wright, we notice an attempt to disturb the classification of the Upper Lias and Lower Oolitic beds, respectively, as laid down by previous observers; this writer con- tending that the so-called Oolitic Sands and a few feet of compact stone, very oolitic in structure, should be placed with the Upper Lias. Here, then, at the very outset of a description of the Oolitic rocks I find myself obliged to do battle for an important portion of territory, which is attempted to be added to the Lias upon grounds which, if admitted, I conceive can only end in merging the whole of the Oolites into a Liassic series. Without following Dr. Wright through his elaborate paper *— which I cannot help considering as a clever example of special plead- ing,—I shall endeavour shortly to review the case as it stands. When, in 1834, Sir R. Murchison penned his ‘Outlines of the Geology of the Neighbourhood of Cheltenham,’ he for the first time divided our inferior Oolitic rocks into distinct beds ; and in the second edition of that work, which I had the pleasure of editing, this classification was only altered by way of a still greater division of the beds. It now, however, becomes evident that the descriptions adopted in this work, taken, as they were, from the immediate neighbourhood of Cheltenham, such as Cleeve and Leckhampton Hills, are only locally correct, and more particularly as regards the basement-bed of the Inferior Oolite. In the work mentioned we find the following remarks :—‘‘ The lowest member of the Inferior Oolite has a remarkable mineral aspect ; it is of a rusty brown colour, and is in great part made up of small flat concretions from a quarter to half an inch in diameter. It is called ‘ pea-grit’ by the country people.” And further on :— ‘*Coralline bodies are spread over ‘the iron-shot faces of the beds below Cleeve Clouds.’? Now this description of the basement-bed of the Inferior Oolite defines it with tolerable accuracy for the district referred to, as at Leckhampton the ferruginous more or less pisolitic beds rest immediately on the stiff blue micaceous bands of the Upper Lias. The following is the section :— ie pine 5. Shelly Freestone Sa echo ee \ 10 0 4. True Pisolite...... ag 3. Coarse- -orained Oolite, more or less pisolitic idan vl nO _ 2. Foxy-coloured ferruginous Oolite, seldom pisolitic 20 0 1. Upper Lias shale. The late Hugh Strickland, in the ‘ Geological Journal,’ vol. vi. p- 242, gives a complete section of the Inferior Oolite of Leckhamp- * Quart. Journ. Geol. Soc. vol. xii. p. 292, &c. . 102 PROCEEDINGS OF THE GEOLOGICAL Society. [June 17, ton, which he most carefully measured; and in this he describes Pisolite (Pea-grit) and Ferruginous Oolite (Belemnite-bed) and sand’’ (just including 2, 3, and 4 of the above section) as 42 feet in thickness; and upon this he offers the followimg remarks :—It consists of a ‘ coarse oolite in the upper part, and of the very peculiar large-grained Oolite or Pisolite (Pea-grit) in the lower. A few miles to the south the pisolite disappears, and is replaced near Pains- wick and at Haresfield Hill by strata containing oolitic grains in a brown paste. This is the precise equivalent of the well-known oolite of Dundry, near Bristol, which may be recognized as far off as Bridport, on the Dorset coast. At Leckhampton the pisolite rests on a few feet of ferruginous oolite and sand. The total thick- ness of this portion of the series is 42 feet*.”? These views are also stated in a paper by my friend the Rev. P. B. Brodie, to which, indeed, Mr. Strickland’s section was an appendix. Recently, more extended observations in the South Cotteswolds, as in the Stroud district, have shown that between the tenacious Upper Lias Shales and the beds of true Oolitic structure, we have a variable thickness of from 50 to 70 feet of an incoherent sandy rock, with occasional bands and nodules of a bastard freestone intersecting it; and this bed has by the Government Surveyors been distinctly mapped as “ Oolite Sands.’ Lately, however, Dr. Wright pro- poses to add not only these sand-beds, but a true oolitic, and occa- sionally pisolitic, rock above this, to the Upper Lias ; a view which he attempts to substantiate mainly by appealing to certain species of Cephalopoda occurring in the bed above the sand at Frocester Hill, which, as some of them are undoubtedly Liassic, he would designate _as witnesses of character+, and would tell us that the evidence derivable from the presence of a multitude of Oolitic mollusca with which the Ammonites are mixed—in a rock, too, of oolitic structure —is of no value whatsoever. I here give an analysis of the fossils obtained from Frocester Hill, founded upon a list for which I am indebted to the kindness of my friend Mr. John Lycett ; many of these fossils have also been found by myself and others; and the results are confirmed by my own observation of this newly-named Cephalopoda-bed of the so-called Upper Lias :— Analysis of the fauna from the Basement Oolite of Frocester Hill: Species. Common to the Lias. 1 CAMIMIONII SE: | Se, cece ww LO 5 2. Hielemmgae (Os205 55.» 3 3 3. Gasteromnda, ~ 020%... 1 0 4. Lamellibranchiatat .... 21 0 S. Brackiopoda t 2 icici. «unit 3 3 DOGS cds 43 re 11 * Quart. Journ. Geol. Soc. vol. vi. pp. 250, 251. + 1 would here suggest that the Cephalopoda, being inhabitants of deep seas, and possessed of such wonderful powers of locomotion, are much weaker as wit- nesses than the non-nomadic Lamellibranchiata. , t Many of these extend high up in the Oolites: probably a few go throughout the Oolite-beds. . Be ws 1857. | BUCKMAN—OOLITES. 103 Here, then, we have a total of 43 species, only 11 of which are truly liassic. It should here be remarked that this list does not include the Ammonites bifrons or the A. fimbriatus, upon the former of which Dr. Wright, and, after him, Mr. Hull have laid such stress ; the truth being, that both Dr. Wright’s specimens of these Ammo- nites (for his matrix was traced) and my own were obtained from as much as 20 feet below the oolite-sands, in the true micaceous beds of the Upper Lias Shales, the position of which will be made plain by the accompanying section of beds at Frocester Hill :— : Fig. 1.—Section at Frocester Hill. r > OSX 7 r QNYDWW —— ——— \————_—-——- 2 3 = (4 Ees5ze%2 |Cephalopoda-bed. { Lower Oolite. (or) Liassie according to Dr. Wright. Liassic. a= | ft. in. | ft. in. 1. Oolite -freestone, with two 5a. Position of Inferior Oolite Shells bands of obliquely-laminated at Nailsworth. Beds 2.525 ——. ....——.... 40 0|6. Upper Lias Shales—very mica- 2. A sandy Oolite, with Phola- ceous 20 0 AGIA D - ovaceeh we encase so tede evan 0 6| 7. Band of indurated White Lias, ioe Me PNUANE titan sas can ochcuues onesie 20 0 with Am. bifrons and A. fim- 4. “ Cephalopoda-bed”’............ 4 0 briatus 10 5. Oolite-sands 60 0| 8. Upper Lias Shales, blue. Now, if I am right in my interpretation of this matter, Dr. Wright has gone into the Lias Shales for his proofs that the Cephalopoda- bed, 80 feet. higher, is Lias; nor is it difficult to understand how he may have been led into this error, inasmuch as the upper part of the Lias Shales has become oxidized from atmospheric exposure ; and besides, on this slope the Inferior Oolite Sands have fallen over them, =e » 104 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, so that their true nature is concealed. At the same time, if these Ammonites are thus to be brought as witnesses for the new Liassic theory, what is to prevent the whole of the Upper Lias fossils from being added to the same category ? But whatever tale may be told by the Ammonites, the following shells, taken from Dr. Wright’s own list, are those which I should consider as characteristic of the Oolite; yet many of these are from the bottom of the sands; and, while none of them are Liassic, many of them range through the Great Oolite into the Cornbrash. List of Conchifera: (F) Frocester Hill; (N) Nailsworth *. Lima bellula, Lycett. F., N., also Great Oolite. Pholadomya fidicula, Sow. F., N., Inferior Oolite. Gervillia Hartmanni, Miinst. F., N., Inferior Oolite. Modiola plicata, Sow. F., N., ranges as high as Cornbrash. Trigonia striata, Sow. F., N., Inferior Oolite. Perna rugosa, Gold. N., Inferior Oolite. Hinnites abjectus, Phil. F., N., Great Oolite. Pecten articulatus, Gold. F., Coral Rag. Gresslya adducta, PAil. F., N., : Gresslya conformis, dgass. F., N., both in Cornbrash. Myacites tenuistriatus, 4gass. F., N., Inferior Oolite. Goniomya angulifera, Sow. F., Great Oolite. Astarte excavata, Sow. F., N., Great Oolite. Myoconcha crassa, Sow. N., Great Oolite. Astarte modiolaris, Desh. N., Inferior Oolite. Cypricardia cordiformis, Desh. F., Great Oolite. Cardium Hullu, Wright (C. Buckmani, Lycett). F., N., Great Oolite. Now as regards this list, it is not a little curious that so many of the species should take so wide a range above, but not one below the disputed ground ; and yet it is on this very account that Dr. Wright prefers, in his metaphorical language, to consider them as “‘ witnesses of no character.” At the same time we see how inconvenient it was to have so decidedly a Great Oolite fossil as the Cardium Buck- mani, Lycett, founded on Minchinhampton specimens, in the new Lias list ; and so it is made a new species. Again, on referring to my Cornbrash fossils, I find that out of 71 species, 45 are common to the Inferior Oolite, and amongst them no less than five forms of Ammonites, as follow :— Ammonites Herveyi, Sow........... Fairford and Siddington. a Brochii, Sow........ ... Fairford and Dry Lease. of subradiatus, Sow........ Fairford. * This section of Nailsworth and its fossils were unknown to Dr, Wright when his paper was read before our Society, but they are incorporated in his general list at p. 305, and thus their particular bearing is, as it were, stifled. They were commented upon at the Meeting of the British Association ; after which the list referred to appears to have been altered. t+ In the above list this shell is quoted just as in Dr. Wright’s list Joe. cit. So —-~—S 1857. | BUCKMAN—OOLITES. 105 Ammonites *Humphresianus, Sow. (2). Fairford. " *Jurensis(?) Zieten...... Dry Lease. With even this list of Ammonites before us, we should hesitate in stating that the bed they came from must be Inferior Oolite ; whilst it would be just as unreasonable to demand that the Cornbrash, with its intermediate member the Great Oolite, should henceforth be added to the Inferior Oolite. Again, we must not always conclude a difference of horizon on account merely of a change in species, especially if we reflect how loose is the definition of a species, and how unsettled are opinions concerning their identification; but we must take a more enlarged view of the subject, and not pin our faith too much upon the labels of either Cephalopoda or Brachiopoda, or Mollusca generally : we are bound to take into consideration all the circumstances of lithological structure, stratigraphical position, and every family of included fossils. As the section of Nailsworth has been referred to, it may be well to state that here, at the base of the sands, is a bed of sandy Oolite, which, though small, as is the opening by the road-side, has yet furnished a good list of fossils, which is constantly being added to ; the following, however, will afford an analysis of their groups, as worked out by the assistance of Mr. Lycett during my last visit : — Species. Common to Lias. AMMO MILIO Ee 55 pao aes oe «0 2 0 elemimbidee 2s: 5 cia ac as. | i GastelO POG ils wre Seen eee. 4 0 i MEW TOMS: «0 5.4.+) 1 0 Lamellibranchiata . Re Mik teeiae 5) 3 new eopne 5 0 Brachiopoda RO en ae Pee 2 1 Votal eos. 30 ye 5 Here, then, as we proceed downwards in these sands, the propor- tion of Liassic to Oolitic forms decreases ; but, once pass the sand boundary-line, and all the species are Liassic; and I still contend that Dr. Wright’s most respectable witnesses to his new theory have been taken from the undisputed Lnas. In this state of the evidence, then, I cannot subscribe to the new views ; but, on the contrary, rather incline to the belief that even the sands belong to the true Oolitic horizon. ‘They mark, where they occur, a great change in physical conditions, and, as a consequence, have induced a corresponding impression upon the included fauna, both as regards general appearance and specific details, — two points to be kept distinct, as the same fossil species from different mineral matrices will “have very different aspects; and again, as far as species are concerned, the list from the Cephalopoda-bed has * These two species are stated with some doubt, as the specimens are very imperfect. The list of Ammonites is being added to constantly, and will be found more in detail iu its place in the Cornbrash. 106 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, undergone many modifications since the hassic view has been taken of it. Hence, in the Oolitic sands, and the equivalent beds, we may mark an oscillation, the effect of which was the continuance of several species identical with those in the Lias which the sands immediately superimpose, though the general style of the fossils decidedly points to an Oolitic fauna,—and this the more so, the more the oolitic structure of the rock prevails. - What, then, is here meant by the equivalents of the sand? My present opinion is, that the sands of Frocester are identical in time with the mixed pisolitic beds of the Cheltenham district, and that the iron-shot sands of the Dundry Hill and Somerset sections are also of the same period: the pisolitic conditions prevailed in one part of the Oolite sea, and sandy ones in another; and hence the difference of the fauna. At Haresfield Beacon is found a large Terebratula, at first named T. lata, but now getting the name of a Lias shell, namely, 7. pune- tata, Sow. At Crickley Hill we have a variety of the same shell ; but here the pisclitic stratum, as it occurs at Leckhampton, is some- what changed, since we have as much as 60 feet of a sandy oolite in blocks of hard stone, irregularly interpolated in beds of pisolitic cha- racter. The most truly marked pisolite is near the top of this emi- nently oolitic section, and it is here that the Ter. simplex and Ter. plicata (Buck.) are in such abundance, together with large forms of Ter. perovalis, which, however heterodox the notion may now seem, I feel convinced will be ultimately considered specifically the same as the Haresfield Hull form, and connected by the large specimens theuce obtained.* The following section of Crickley Hill may be compared with that of Leckhampton :— ft. in. 5. Pisolite, with but a small admixture of oolitic as: ragstone ; “. oe ot 4. Freestone, including pisolite is Je 919 3. Hard blocks of oolite, consisting in part ‘of 35 35 0 very indurated pisolite - 2. Sandy oolite, occasionaliy pisolitie .. .- ae ae 1. Lias. Now here the sands are absent, but their thickness is made up by siliceous and indurated oolites; and where the true loose sandy conditions prevailed, the difference is well marked by the fauna; as ever shifting sands and the want of calcareous matters were as inimical to animals in the old as in the modern seas; hence the paucity of fossils in the true sandy deposits: but where muddy con- ditions occasionally intervened for a while—as even in these sands, * This notion is not new, as Bronn (‘ Index Palzontologicus’) considers 7. perovalis asa synonym of 7. /ata, which, again, is the true 7. ovoides (T. lata, Sow.). D’Orbigny considers 7’. simplex to be a synonym of the same (‘Prodrome’). Indeed, these are among several forms of Terebratula from the same horizon, and yet pre- senting as much difference as groups of our modern Mussel-shells. 1857.] BUCKMAN—OOLITES. 107 at their base at Nailsworth* and other places—animal remains are abundant. Hence I am compelled to adopt the following conclusion :— To class the sands with the Oolites; as they evidently mark, to say the least, an oscillation im the previous or true liassie conditions ; and, though a few, and only a few of the Cephalopoda common to the Lias still maintained their ground, yet at the base of the sands we are not without a shelly deposit so thoroughly Oolitic that a glance is sufficient to decide the question. In adopting the line contended for by Dr. Wright, we do so en- tirely upon the evidence of fossils which are yet mostly peculiar to isolated positions ; and, whilst many of them range high in the Oolites, few, if any, are found in the real Lias,—of course, those got from the Lias itself not being properly classed as proofs of the position of the sands, much less of the Cephalopoda-bed. We give up also a well-defined line,—namely, that of a blue mica- ceous clay, overlaid by calcareous sands, the latter being the precur- sors of the more perfect calcareous condition, which, indeed, did sometimes prevail in the same horizon,—only to form a boundary- line between even courses of beds of true colitic structure: this, to my view, appears very unreasonable. Having so far disposed of the question of the basement-bed, it may be well here to give a Table of the different members of the Inferior Oolite rock as they appear in Gloucestershire ; they are as follow, in descending order : Be HE CLYBCUS- DEAS oes. divexescsce oc ccnencecoseus tee Clypeus sinuatus. Sense ee Trigonia costata. Trigonia-grit } 8 : ay we : aD CON SUS mies > we aeloiat Sanaa aks Gryphea Buckmanni. ae \ Ammonites. ete ADGMLC-THATISUONE ‘caccesieveccedsccnececscencecese Terebratula fimbria. Pee RP ESIRE oe ce caias nc cs cede cues sestscdverevdsseues Elizabethe, eee Gryphea dilatata, Phill. teten. Pratt. 1. Ammonites Calloviensis, M. C. Terebratula ornithocephala, M.C. Keenigi, M. C. Trigonia—costated and clavel- — sublevis, M. C. lated forms. — Gowerianus, M. C. The agriculture of the Oxford Clay is very variable; where good farming prevails, and the necessary preliminary expenses incident to draining and otherwise ameliorating the mechanical texture of the subsoil have been entered into, highly rich tracts of land are seen; but where these have been neglected, as in the well-known Forest of Braydon, there will be found some of the stiffest and poorest land in the country: this latter circumstance, coupled with the occur- rence of occasional deposits of lignite in the thick clay-beds, has for centuries led to futile workings for coal, which are not aban- doned even in the present day. A century since, a working of this kind was commenced in the Oxford Clay at Malmesbury, and, after sinking a shaft a little more than 100 yards, the works were abandoned —at the instance, it was said, of proprietors in the Somerset coal-dis- trict, ‘‘ fearing lest the new works would injure them by competition ;”’ and a short time since the recommencement of the works was agitated: but it may be interesting, as marking what a century has done in this direction, to know that, previously to deciding upon so doing, the opinion of a geologist was sought in the matter; and, as I happened to be chosen to make a report upon the subject, it will not be wondered at, that I should recommend the works to be abandoned. However, people still think, from the wild aspect of much of the country occupied by the Oxford Clay—simulating, as it does, the appearance of a district in which mining and manufac- turing has injured vegetation and caused agriculture to be neglected —that the surface indicates mining-ground ; and some of the lignite got out of the clay in the section made for the Great Western Railway is still preserved as good evidence of coal by some, who, occasionally finding similar lignite in the clay in brick-fields and elsewhere, credulously say, ‘‘if coal is so good and so thick near the surface, how much thicker may it not be found at the depth of a mine!”’ 11. Cora Raa. This rock will be seen represented in Section, Pl. VII., at the to of Blunsdon Hill, where it attains the thickness of about 15 feet ; and in the deviation to Swindon small exhibitions of the stratum may * A full list of these, it is hoped, will be given hereafter: there are many new forms. 126 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, be marked: in travelling along the Great Western line of railway, a section may be observed in deep cutting a little to the north of Swindon. Indeed, the Coral-rag may be occasionally observed capping the minor hills in advance of the long chain of the Wilt- shire chalk-range. Occasionally, though our sections and those of Lonsdale and Fitton would make it appear that the Coral-rag is a continuous stratum, having the Oxford Clay below and the Kimmeridge Clay above, it seems in North Wilts to occupy only hummocks, and to be sometimes wanting altogether, when the line of demarcation between the two clays just named is exceedingly difficult to determine. The district now under review, however, is not the best in which to study this bed, as it is here only par- tially developed, and its accompanying drifts of the Calne district are entirely absent: in the words of Lonsdale, ‘‘ The rubbly oolite constitutes the greater part of the Coral-rag of Wiltshire; it is formed of a nodular limestone of an earthy aspect, a brownish, yellowish, or blueish white colour, and abounds with fragments of echini and shells*.’’ This very well describes the rock of my section. Thin as the stratum is in this district, it is very rich in fossils, and amongst others found at Blunsdon are the following ‘ Corals. Thecosmilia annularis Stylina tubulifera -—— Delabechii Thamnastrzea arachnoides Isastreea explanata See Monograph by Edwards and Haime (Palzontographical Society). Echinoderms.+ Cidaris Blumenbachii, Miinster. Diadema subangulare, Goldfuss. Diadema depressum, Agassiz. Nucleolites dimidiatus, PAzll.t Bivalve Shells. Modiola inclusa §, Pecten inzquicostata, Phillips. Crassina ovata, Univalves. Turbo muricatus, Geol. York., pl. iv. f. 14. funiculatus, id. pl. iv. f. 11. Turritella muricata, 7d. pl. iv. f. 8. Ammonites. Ammonites perarmatus||, M7. C. t. 352. Ammonites triplex, M@. C. t. 292. It is worthy of note that the Brachiopoda seem not to be represented in the Coral-rag. * Lonsdale on the Oolite District of Bath, Geological Society Transactions, 2nd ser. vol. iii. p. 241, &c. Read 6th Feb., 1829. + The species are so common as to be found in handfuls; the test, however, is difficult to obtain perfect. "{ Sometimes occurring in masses. § Abundant in galleries in the corals. | This and the following are frequently of great size. 1857.| BUCKMAN—OOLITES,. 127 Now, if we review the disposition of the masses of this rock, and examine its structure, we shall, I think, conclude that it was not deposited continuously on a uniform sea-bottom, but in separated lumps,—by the peculiar method of working of the coral-animal, to whose labours this bed is mainly due, and under circumstances in all probability similar to those of our modern coral-reefs. This, however, would of itself induce in the then existing sea a phy- sical change of condition, which had its influence on the succeed- ing deposit, namely, the Kimmeridge Clay. The latter, though differ- ing slightly from the Oxford Clay with which it is in contact, as on the road from Blunsdon to Swindon, is marked by a good set of fossils: these at times are the only guide, as the colour of both the Oxford and the Kimmeridge Clay is very variable, and besides, through- out their whole extent, both are remarkable for the quantity of fine erystals of selenite diffused through them ; these very large at Ash- ton Keynes, in the lower beds of the Oxford Clay ; and the Kim- meridge Clay at Swindon is full of beautiful crystalline groups of sulphate of lime. 12. KImMERIDGE CLAY. Along the line of section, both im its direction to Swindon and Wanborough, this deposit will be seen to succeed the Oxford Clay, of which, indeed, it may, as far as the district under review is concerned, be considered as the upper beds, having the Coral-rag as an occasionally interpolated and local deposit. The Kimmeridge Clay occupies a wide range of flat country around the hill on which Swindon stands, and here it is a dark, lead-coloured, unctuous clay, of a shaly consistence when first dug; the layers of the clay are parted by white nacreous matter, the only remains of thousands of Ammonites and other shells, which are only locally preserved. Every bed of clay that I have examined about New Swindon, where it is largely worked for brick-making, is full of crystals of selenite, and no less remarkable for the quantity of Trigonellites latus, valves of which, all sizes, are best studied here. The Kimmeridge Clay at this place may be divided into two Stages :— D. The upper one of dark shales, in which Trigonellites latus, Exogyra virgula, and Ammonites prevail. 1. The lower of lead-coloured and blue clays, full of large masses of Ostrea deltoidea and abundant sheaths of Belemnites excentricus, Blainville, often of very large size. The following list of fossils is by no means complete, and is only offered as evidence of the prevailing facies. Reptilia.—A species of Pliosaurus, of immense size ; fine portions of this are in the museum at Cirencester, and in that of the Royal Agricultural College. Belemnites excentricus, Blain. Ammonites serratus, MW. C. Beaumontianus, D’ Ord. Goliathus, Ter. Jurass. Trigonellites latus, Fitton, Mem. t. 23, t. 195. £. : —— Sallierianus, zd. t. 208. Pie 128 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, Rhynchonella inconstans, M. C. Panopza depressa, id. t. 23, f. 9. Ostrza deltoidea, M. C., occurring in Serpula variabilis, Fitton, Mem. t. 23, masses. ye Exogyra virgula, Fitton, Mem. t. 23, — triseriata, id. t. 23, f. 8. f; 10. 13. PorTLAND OoLITE. Swindon Hill, in the line of section, Pl. VII., may be described as an isolated mass of Portland Oolite, capped with the lower beds of the Wealden (Purbeck) series. This Oolite by no means occupies a con- tinuous line along the base of the Wiltshire Hills, as the section through Stratton St. Margaretts shows it to be entirely absent along that line, where the chalk-group rests immediately upon the Kim- meridge Clay. As shown by Dr. Fitton, the Portland Oolite is exceedingly patchy; and the map illustrating his memoir ‘ On the strata below the chalk *’’ well shows the isolated masses of this rock in Wiltshire. ; The Portland rock seems to have been the first upraised land from the oolite-sea, and, as such, formed a theatre for the dwelling of land and fresh-water existences which mark the Wealden deposits : hence, the Wealden would be forming on the isolated peats of Portland at the same time that Greensand and Gault were being deposited in the surrounding seas; thus affording an example in proof that stratigraphical schemes which represent such beds as the Wealden, when on the top of the Portland Oolite, Coral-rag, and Bradford Clay (to confine our remarks to the Oolites), as of different age from the beds surrounding them, is not always correct. This view is founded upon the fact, that Portland Qoolite, with only a capping of Wealden, occurs in North Wilts in occasional knolls or sub-hills ; but, where it is absent, the continuity of the succeeding beds is not at all altered, nor their conformability interfered with. The Portland Oolite has been much denuded since its deposition, and upon its washed surface the dirt-bed, which dips into its hollows and fissures, has left its remains, as seen in the section at Old Swin- don Hill. The following sections will give a tolerably correct notion of the composition of the Portland rock at Swindon, the furthest limit of our observations in this memoir :— A Section of the Upper Beds at the large Stone-quarry. ft. in. ft. in. 6. Clay 8 0 > ees 2. Brownish Marl, mixed 5. White Marl-stone 2 6 8 = with pebbles and gra- 4. Band of Clay 1, f zLe vel, containing vegetable 3. White Marl-stone 3 6 A,” | matter. (=Dirt-bed.) aue 1. Sandy Oolites with thick beds of sand: the sand in oblique _ ft. in. laminz ; to the bottom of the quarry 20 0 The next section illustrates the nature of a sand- and stone-quarry at the base of Swindon old town :— 2. Portland building-stone, about 10 feet. 1. Portland Sands, with thin partings of stone, about 20 45 * Trans. Geol. Soc. 2nd ser. vol. iv. p. 103, &c. 1857. | BUCKMAN—OOLITES. 129 From these data I infer that the Portland Oolite at Swindon is about 40 feet in thickness, and capped by about 18 feet of Wealden beds. It is not my intention to enter into a discussion about the Wealden character of these upper beds* ; I, however, quite agree that they are simply the outliers of a rock which assumes great importance farther south, as in the Vale of Wardour, where they have been so successfully worked and ably described by Dr. Fitton and my friend the Rev. P. B. Brodie. As regards the fossils of the Portland rock, these will be found to be highly typical of an Oolitic deposit ; and, if they be compared with those of the true Chalk, the latter would seem to indicate a sudden and extraordinary change in the fauna; the passage is, how- ever, after all, tolerably gradual from the Oolites to Chalk, through the medium of the Greensand, such fossils as the T'rigonia, Pano- pea, Cardium, Pinna, and Perna being at least important genera common to both Greensand and Portland Oolite. The following list of fossils of the Portland at Swindon, all of which I have obtained from the large quarry, are mostly determined from Dr. Fitton’s list and illustrative engravings; they consist of Ammonites giganteus, W.C. Trigonia gibbosa, Fitton, pl. 22, f. 4. biplex, M. C. species ? Terebra Portlandica, Fitton, Mem. pl. Lucina Portlandica, id. pl. 22, f. 12. 23, f. 6. Cytherea rugosa, Fitton, pl. 22, Natica elegans, éd. pl. 23, f. 3. f. 13: Buccinum naticoides, id. pl. 23, f. 4. Cardium dissimile, M. C. —— angulatum, pl. zd. 23, f. 5. Perna quadrata, M.C. Nerita angulata, id. pl. 23, f. 2. Panopza depressa, M. C.. Trigonia incurva, Benett, Wiltsh. Foss. Pecten lamellosus, 1.C. t. 18, f, 2. Large masses of coniferous wood are often found on the Portland measures ; and occasionally well-preserved trunks of trees are ex- humed at the Swindon quarries. Here, then, I must content myself for the present with having described the more general characteristics of all the members of the Oolitic series of rocks; it will, however, be seen that the discussion of physical changes, such as a description of the many faults by which the country under review is intersected, the facts connected with our numerous valleys both of denudation and depression, the drifts by which the country is overspread, and which are so diverse in character, and other interesting physical phenomena have been, for the most part, unnoticed. This, however, is not from inatten- tion to such important matters, but from want of time to put my notes together ; and so, for such matters, as also for a comprehensive list of fossils of the Oolites, now in course of preparation, I must beg indulgence until the next session of our Society ; indeed, from * Besides Dr. Fitton’s paper above referred to, see Mr. Brodie’s and Mr. Aus- ten’s Notices of these beds, Quart. Journ. Geol. Soc. vol. viii. p. 53, and vol. vi. p- 467. . VOL. XIV.—PART I. K 130 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, » the length of this paper, these subjects may well form a future com- munication. I would now, therefore, conclude with the hope that the present paper may not be without interest, at the same time that I would earnestly beg the kind indulgence of the Geological Society ; since the many calls upon my time have prevented my rendering the sub- ject so complete as I could wish. 3. On the GroLtocy of the SourHERN Part of ANDALUSIA, between GIBRALTAR and ALMERIA. By Professor D.T. ANsTEp, M.A., F.R.S., F.G.S. [The Publication of this paper is unavoidably deferred. | { Abstract. | Tue object of the author in this memoir was to direct attention to several points of interest and importance in the Geology of the south of Spain. These had reference to deposits of various ages, including the metamorphic rocks, both of the Sierra Nevada and the coast. 1. The mica-schists of the Sierra Nevada form a well-marked series, limited in position to the higher elevations. They are garnetiferous, and traversed by veins of serpentine. Bands of quartz alternate with the schists. On the south-west side deposits of highly argentiferous copper-ore have been recently worked, but they appear to be irregu- lar. Specimens of greenstone were discovered by the author on the north side of the Sierra, but not zz situ, and no such rock has been described. On the north side the mica-schist is covered towards the west by limestone, highly crystalline, and recently found to contain deposits of galena. Over these are thick beds of marl and calcareous beds of tertiary date, and irregularly over all is detritus of a com- paratively recent period. On the south side is a deep ravine, thick beds of shale occupying the space between the schists and the lime- stones of the Sierra de Gador, long celebrated for numerous and rich lead-mines. Beyond the limestone to the south are metamorphic schists (not micaceous), and in some places the contact of the lime- stones and these schists is marked by a gradual transition. These schists are continued, with little break, parallel to the coast, and at no great distance from it, for at least a hundred miles; and at intervals they contain deposits of copper-ore not argentiferous. Near Malaga the author has observed a gradual passage from these schists into a conglomerate, and thence into the triassic‘and jurassic deposits subsequently described. The schists are argillaceous and chloritic, and as well as the mica-schists are traversed by serpentine-veins. No organic remains have been discovered in any of the schistose beds. 2. Over the schists on the coast, a little to the east of Malaga, at a point where there is a dislocation, a foetid magnesian limestone is presented to view, and is regarded by the author as Permian. This limestone is black, semi-crystalline, unfossiliferous, entirely distinct from the dolomites of the Sierra de Mijas adjacent, and is immediately overlaid by a group of shales and sandstones, at the top of which is a a ee le Se eee = a 1857. | ANSTED—ANDALUSIA. 13H the calamite-grit next alluded to. It corresponds in position with the conglomerates or passage-beds between the shales and red sand- stones near Malaga. 3. Above the magnesian limestone just deseribed, or immediately over the conglomerates, the author observed a considerable series of whitish marly sandstones, marls, red sandstones, white sandstones with vegetable-markings and occasional lenticular masses of gypsum, extending along the coast from some distance west of Malaga to the eastern side of the Sierra Nevada. Near Malaga, at one spot, cala- mites (Hquisetites) have been obtained from a quarry of white sand- stone used for building-purposes, near the top of the series. Speci- mens of these were exhibited. A band of lignite of no value has been opened in the lower part of the red sandstone series, near the hill of San Telmo. 4. Next in order are the blue and black limestones of the Sierra de Gador, and others of the north side of the Sierra Nevada, both passing into whiter and cream-coloured limestones towards the west, and in the neighbourhood of Gibraltar becoming pale, clear, and semi- crystalline. A few fossils have been found in this limestone at Gib- raltar, some of which were shown. Others have been met with, but very rarely, at intermediate points between Gibraltar and Granada. Although the limestones of the Sierra de Gador and others in that vicinity are highly crystalline and metamorphosed, and are traversed by large veins and fissures containing enormous deposits of galena, the author is satisfied that they are not more ancient than the middle secondary period, and form a continuous series along the whole line of coast. 5. Cretaceous rocks have been described on the summit of San Anton, a few miles from Malaga, and they are believed to range into the interior. The author described the appearance of the red marble of San Anton, containing Belemnites, which are not yet specifically determined. 6. Older tertiaries are known to exist near Malaga. The author described a peculiar calcareous breccia, forming a semi-crystalline bed of limestone, reposing on the cretaceous and jurassic rocks, near Malaga, and covered by a very perfect compact oolitic limestone, capable of taking a high polish, and almost a marble. This bed lies over the limestone-breccia, and beneath or alongside a foraminifera- bearing limestone, composed of Orditoides and Alveolina, and also extremely compact. It belongs to the Nummulitic limestone series. It was traced by the author to some distance. 7. The vicinity of Malaga presents a large space occupied entirely with newer tertiary rocks, and these extend at intervals up the water- courses and river-valleys, and along the coast both east and west. They have been already described to some extent by Col. Silvertop and other geologists, but it is only lately that the author was enabled to discover beds richly fossiliferous, which will enable the Paleeonto- logist to decide absolutely with regard to the relative age of these rocks. The following sequence of the rocks belonging to the newer tertiary and recent periods is suggested by the author as justified by K 2 132 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, the rocks in the south of Spain, and likely to be useful for future reference. Recent ...000009.2. River-detritus. f Angular fragments of slate and other f t) ‘adjacent Tock’\. (sac... Wovesecsesedso-7 etna Coast near Malaga. ‘ Fine white sand and pebbles without | Guadalmedina, Raised beaches. OLSANIC TOMAS » ccsinceve onsoevas'ashas eure t banks of. Marly incrustations with numerous re- : \ [i CONG SNCIUE ” .ccsaasvncdeas coker dpar seers Sta-Cas Coarse gravel with sand and pebbles... | Caletaand Jabonero ROSSIILETOUS {7002's cacaenstuses tosneanaeeer arroyos. Marly sands with land, freshwater, and Upper ‘Tertiary: {\ -wolled: fassils. 2.0.0. 0.5..c,scws0sesdacnaests | Blue clay and marl loaded with forami- > Tejares beds. nifera, univalve and bivalve shells, and | bones of large pachyderms. : Nummulitic limestone. Lower Tertiary. { Oolitic limestone and limestone-breccia. The Tejares (or Brick-pit) beds consist of whitish sandy marls, with land and freshwater fossils overlymg other sandy marls, and blue marly clays loaded with foramiifera, and in many places abounding with fossil shells, both univalves and bivalves, in a perfect state of preservation. Fragments of a jaw and vertebra of Rhino- ceros, believed by Dr. Falconer to be R. megarhynchus, were exhibited at the meeting. The author has since received fragments of a large cetacean, and has been informed that very perfect remains of fishes have been found. The author brought home a large collection of these fossils, for which he was mainly indebted to the active coopera- tion of an English lady, resident in Malaga. He was also assisted by Don Antonio Linera and Don Pablo Prolongo, both of Malaga. The result of the minute examination of these fossils will be communicated later, but they seem to place the deposit amongst those of the Sub- Apennine period, the newest being probably not far distant in time from the newer tertiary deposits of Montpelier and Perenas, recently described by Christol. The beds of this group are laid bare at various places in the Vega or Plain of Malaga, and always present the same character. They have been subjected to elevation and are tilted at a small angle in various places, especially near the hills of triassic and jurassic rock in the interior. The Caleta deposits (so called from the arroyo or river-bed in which they are seen) consist chiefly of sand- and pebble-beds, loaded with fossil shells, chiefly confined to a few species of Pecten and Ostrea, but including other bivalves and some univalves. These de- posits are traceable up the bed of the Caleta for about a mile, and are also seen in the bed of the Jabonero, and in a plain that extends on its left bank. They are far less rich in species than the Tejares, but there are often beds entirely consisting of Pectens or Oysters, mixed only with a little loose sand. The Catalina beds consist of a thin coating of hardish marly lime- stone, containing a few fragments of Pectens and other shells, little if at all different from those living in the adjacent seas, but at 1857.] BAILY—FOSSILS FROM THE CRIMEA. 133 a level of 50 feet or more above that of the Mediterranean. These beds cover immediately the jurassic limestones without the interven- tion of any other tertiaries, and may probably be regarded as raised beaches. The true raised beaches of sand, pebbles, and angular fragments, chiefly of slate-rock, are well exhibited close to Malaga on the east, and at various points between Malaga and Almeria, both on the cliffs where they approach the sea, and up the arroyos or water-courses to the point where these enter the more abrupt and mountainous country behind. Their elevation varies, but often exceeds 60 feet. The nature of these deposits, and the causes to which they are due, are considered by the author to offer matter for careful study im connec- tion with the phenomena of denudation generally in all parts of the world. 8. The author then alluded to the economic geology of the dis- trict under consideration. It contains copper-ores, some of them argentiferous, but generally with too little silver to increase the value of the ore. These occur in bunches, and with few exceptions have not been worked to profit. They are confined to the schists. Lead- ores have been worked for centuries in the Sierra de Gador, and more recently in the adjacent limestone on the north side of the Sierra Nevada. These ores are galena and carbonate of lead, with little or no silver; but galena with antimony-ore occurs near Mar- bella, and lead-ores have been worked in the dolomite of the Sierra di Mijas. Iron-ore in vast abundance, and of admirable quality, is also obtained from behind Marbella. Building-materials of fine qua- lity, both limestones and sandstones, are readily procurable near Malaga, the former from the jurassic, cretaceous, and older tertiary series, the latter from the calamite-grit. Good lime is procurable to any extent, and at moderate price, from the jurassic limestone. Good brick-clay, and fine clays for pottery, from which is manufactured the delicate terra-cotta figures for which Malaga is celebrated, are procured from the newer tertiary beds of the Tejares and others in the plains of the Guadalmedina. White sands for glass-making and other purposes are taken from the triassic beds near the calamite-bed. Gypsum of fair quality is found abundantly in large lenticular masses in the sandstones underlying the jurassic limestones, both near Ma- laga and near the Sierra Nevada. 4. Descriptions of Fosstu INVERTEBRATA from the CRiMEA.* By Wituiam H. Batty, Esq., F.G.S., of the Geological Survey of Great Britain. (Plates VIII., IX., X.] THE specimens described in this communication were principally collected by Capt. C. F. Cockburn, of the Royal Artillery, who has also supplied the Note on the Geology of the Neighbourhood of Sevastopol, which is appended to this paper. * An abstract of this communication was read at the British Association Meet- ing, August 1856. 134 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, JURASSIC. AMORPHOZOA. 1. Scypn1a Cocxsurnt, sp. nov. Pl. VIII. fig. 1, a, 6. A convoluted sponge, having ten or eleven prominent plications or costee, with a central nearly circular canal ths of an inch in diameter. The structure is somewhat obscure, but, where exposed, exhibits an irregular porous texture ; its base appears to have been adherent. Dimensions : length 14 inch, diameter 17 inch. Locality. From red Jurassic limestone near Balaclava. Dedicated to Capt. C. F. Cockburn. ZLOOPHYTA. Order ZOANTHARIA=APOROSA. Fam. FuNGIDz. 2. ComoseEris rrrapians, M.-Edw. & J. Haime, Brit. Foss. Cor. Pal. Soc. p. 101, t. 19. f. 1, a—d. This and the several other fossil corals from the same locality, here- after mentioned, can scarcely be distinguished lithologically or spe- cifically from those obtained from the Coralline Oolite of Steeple Ashton, Wiltshire. Loc. Soudaxioxia. Presented to the Museum of Practical Geo- logy by the Imperial School of Mines at St. Petersburg. Fam. ASTRHIDZ. 2a. THECOSMILIA ANNULARIS?, Flem.sp.; M.-Edw. ibid. p. 84. ti153140 fet. A mass of small Polypidoms, which may be referred to this spe- cles, in compact argillaceous limestone from Simferopol. Presented by the Imperial School of Mines, St. Petersburg. 3. IsastR@#A Greenovueuil, M.-Edw. Pal. Soc. p. 96. t. 17. f. 2. Loc. Soudaxioxia. Presented by the Imperial School of Mines, St. Petersburg. 4. IsastrzA (AstR#A?) PoLYGoNALis, Mich. Fragment of the worn surface of this coral exhibiting a tessellated appearance in red crystalline limestone, from the Bathing-place one mile west of Balaclava. | 5. IsastR&A EXPLANATA?, Goldf. sp. ; M.-Edw. Pal. Soc. p. 94. Regn 28. £21; | 7 A weatherworn mass of what appears to be this species in white crystalline limestone, from between the Monastery of St. George and Balaclava. 6. THAMNASTRZA ARACHNOIDES, Park. sp. ; M.-Edw. Pal. Soc. t. 1Sea. de An adult specimen of a very flat and thin form, having the stars in . Geol. Soc. Vol. XIV. Pl. VIL Quart. Journ Printed. by Hullmandel & Walton. SMES SIC ANYACRE TACHOUS. FOSSILS From pur CRIMEA. del et ith. Werth Baily a - %: * a ‘ @. ° _ ® 3 +3 . 2 is 4 Stet a ae 1857.] ' _BAILY—FOSSILS FROM THE CRIMEA. 135 depressions ; both sides well preserved ; the under side covered with a small species of Serpula. Loc. Soudaxioxia. Presented by the Imperial School of Mines, St. Petersburg. 7. CaLtaMopuyuiia Stoxestt ?, M.-Edw. Pal. Soe. t. 16. f. 1 a-d. Identical with or closely allied to this species. Loe. From between the Monastery and Balaclava. Another specimen, probably identical with this species, but too uperfect for determination, was obtained from the Gorge of Iphi- - genia. | 8. MonrTLIvVALTIA TROCHOIDES, M.-Edw. Pal. Soc. p. 129. t. 26. 12,2 @.. OHO Glee toes bos 2 A very perfect specimen of a single polypidom is contained in the British Museum collection. Presented by Mrs. Cattley. Loc. Tchatyr-dagh or Tent Mountain. ECHINODERMATA. 9. Fragment of a spine of Cidaris? Associated with Terebratula numismalis in Lower Jurassic lime- stone, equivalent to the Lias. Loc. Woronzoff Road. 10. Spine of Cidaris ? In grey limestone from the lowest beds of the Jurassic series. Loc. Gorge of Iphigenia. 11. Spines of Cidaris Blumenbachii. Loe. Soudaxioxia. Presented by the Imperial School of Mines, St. Petersburg. 12. Spines of Cidaris glandifera. Loc. Between the Monastery and Balaclava. 13. Spine of Cidaris? From red clay-veins in Jurassic limestone. Loc. Between the Monastery and Balaclava. 14. Spine of Cidaris? Barrel-shaped. with small central cavity, in red-tinged compact Ju- rassic limestone. Loc. The Bathing-place one mile west of Balaclava. 15. Joints of the stem of Apiocrinites incrassatus, Roemer, Die Verst. Ool. t. 1: f. 12. In red clay from the Jurassic limestone. Loc. Between the Monastery and Balaclava. Larger joints in a similar matrix with corals have been brought from the last-mentioned locality. 16. Portions of the stem of Pentacrinites basaltiformis. Loc. Soudaxioxia. Presented by the Imperial School of Mines, St. Petersburg. 17. Two plates of a Starfish, with punctated surface. 136 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, In grey limestone, with the spine No. 10, from the lowest beds. Loc. Gorge of Iphigenia. Mouuvsca. BRACHIOPODA. 18. TEREBRATULA NUMISMALIS, Lam. This characteristic Lias species was obtained from grey limestone and shale. Loc. Woronzoff Road. Lower Lias. 19. TEREBRATULA ROTUNDATA”, Roemer. Allied to 7. ovoides, Sowerby, in compact pinkish limestone. Loc. Woronzoff Road. 20. TEREBRATULA JAMESII, sp. nov. PI. VIII. fig. 2, a, 6. Shell inequivalved, ovate, longer than wide; rostral valve mode- rately convex, smaller valve somewhat flattened; beak prominent and truncated, with a rather large foramen; lateral margin of valves slightly curved, and a somewhat flattened front; surface smooth, punctated, and marked by concentric lines of growth. Dimensions.—Length 1 inch, breadth ;8>ths of an inch. Loe. From dark-grey Jurassic limestone, Balaclava. Collected by Major Cooke, R.E. Dedicated to Lieut.-Col. James, R.E. ? 21. TEREBRATULA, sp. Probably 7’. subovoides, Miunst. Found with the large barrel-shaped spine, No. 14, in red compact limestone. Bape The Bathing-place one mile west of Balaclava. . TEREBRATULA PEROVALIS ? cr aae the matrix of Ammonites fimbriatus, Middle Lias. Loc. Village of Biasali. Presented by Imperial School of Mines, St. Petersburg. 23. TEREBRATULA. Lower part of a large species, probably Tere- bratula Strogonofii, D’Orb. Geol. of Russia, &c. p.489, in com- pact red limestone. Loc. Gorge of Iphigenia. 24. TEREBRATULINA RADIATA, Sp. nov. Pi. VIII. fig. 3, a-d. Shell inequivalved, nearly hemispherical ; beak produced, slightly recurved, truncated, with a large foramen and triangular deltidium ; surface of valves beautifully punctate, and ornamented with from 20 to 25 longitudinally elevated strie. Dimensions.—Length ;3,ths, breadth ths of an inch. Loc. Balaclava. Six specimens of aa elegant little Brachiopod were detached from the matrix which contained Terebratula Jamesit. 25. RHYNCHONELLA CooxeEl, sp. nov. Pl. VIII. fig. 5, a, 6. Shell considerably wider than long ; ; valves slightly convex ; beak acute; foramen small, surface ornamented by about 30 acute plaits, having a central elevated ao fold composed of 10 plaits. Dimensions.—Height 155 inch, breadth 2} inches. 1857. ] BAILY—FOSSILS FROM THE CRIMEA. 137 Allied to Rhynchonella subtetrahedra, Dav. (Monog. Brit. Ool. Lias, Brach., Pal. Soc. p. 95. pl. 16. f. 9-12), but differs in the greater number of plaits, and in its greater breadth compared with its length. It has a winged appearance, and belongs to the group Alate of Von Buch. The specimens, of which there are two, were collected from the grey limestone of Balaclava by Major Cooke, to whom it is dedi- cated. 26. RHYNCHONELLA PECTINATA, sp.nov. PI. VIII. fig. 4, a, 6. Shell inequivalve, subtrigonal, slightly convex, longer than wide, widest at the front and gradually tapering upwards towards the beak ; beak acute ; foramen large, surrounded by the deltidium, and separated from the umbo ; valves somewhat flattened and fan-shaped, without mesial fold or smus ; surface ornamented by about twelve large plaits or costze. Dimensions.—Height ;5ths, breadth ;6ths of an inch. Allied to R. pectunculoides, Schlot., but differing in its greater length in proportion to its breadth, and in having more costz. Loe. Gorge of Iphigenia, in red crystalline limestone. 27. RHYNCHONELLA SENTICOSA, Von Buch; Davids. Brit. Ool. Lias, Brach., Pal. Soc. p. 73, pl. 15. f. 21. Mr. Davidson describes this species from the lowest beds of the Inferior Oolite. M. D’Orbigny places it in the Oxfordian. Our specimen was collected by Major Cooke from the grey limestone of Balaclava, apparently equivalent to Inferior Oolite. 28. RHYNCHONELLA ACUTA, Sow. From the matrix of Ammonites fimbriatus. Loc. Village of Biasali. Middle Lias or Marl-stone. Presented by the Imperial School of Mines, St. Petersburg. 29. RHYNCHONELLA VARIABILIS “, Schlot. Of this species the back of the rostral valve only is exposed, on a slab of coarse greyish limestone. Loc. From the base of the rocks at the Gorge of Iphigenia. LAMELLIBRANCHIATA. ASIPHONIDA. 30. OstrEA. Small species in a light-brown marl, with but few other traces of fossils. Loc. From Karani. Lias shale? 31. Osrrea, sp. Associated with Cardium equistriatum, No. 35, and Terebratula numismalis, No. 18. Loc. Woronzoff Road leading to Kamara. Lower Lias shale. 32. Ostrea, sp. A coarsely plicated species in the red clay of the Jurassic limestone, associated with Corals, No. 4, spines of Echini, Nos. 13, 14, and Terebratula, No. 21. Loc. Bathing-place one mile west of Balaclava. 33. GRYPHA DILATATA, Sow. 138 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. June 17, Single valves of adult shells, with massive hinge-areas in a similar matrix with the Corals, Nos. 2; 3,, andG, Loc. Soudaxioxia. Presented by the Imper ial School of Mines, St. Petersburg. 34. GrypH#ZA IncuRVA, Sowerby. Associated with Ammonites, Nos. 40, 41, and 42, in reddish marly limestone with ferruginous granules. Loc. Village of Biasali. Middle Lias. Section SIPHONIDA. 35. CARDIUM ZQUISTRIATUM, sp.nov. PI. VIII. fig. 6, a, 6. Shell subtrigonal, convex; umbones prominent and contiguous ; anterior surface ornamented with concentric and very regular smalt ridges, posterior portion with radiating longitudinal lines, widely distant at the margins. It differs from Cardium truncatum of the Lias in being less con- cave, and its radiating posterior lines are more widely distant, and the concentric ridges more defined and regular, the umbones being placed nearest the posterior side. Dimensions.—Height ;3,ths, breadth ;8>ths of an inch. Loc. Woronzoff Road. Lower Lias. . 36. ASTARTE COMPLANATA, Roemer, Verst. pl. 6. f. 28. Associated with the Cardium last described, No. 35; Ostrea, No. 31, and Terebratula numismalis, No. 18. Loc. Woronzoff Road leading to Kamara. In dark-brown shales. Lower Lias. | GASTEROPODA. HoLosToMATA. 37. Narica, sp. an inch, Lee of tube 7 ths of an inch. A second specimen measured but ;6ths of an inch in length, with a diameter of $ an inch. Loc. Monastery of St. George. Dedicated to Col. Portlock, Pres. Geol. Soc. FORAMINIFERA. 77 a. POLYSTOMELLA CRISPA, Linnzeus. Mr. Rupert Jones has detected two specimens of this very minute Nautiloid form (still common in the Atlantic and Mediterranean) on the weathered surface of a limestone, made up of fragments of shells, principally bivalves, and collected by Lieut.-Col. Munro in the neighbourhood of Sebastopol. Mouuvusca. ASIPHONIDA. 78. Myritus apertus, Desh. Mém. Géol. Soc. France, vol. iii. p- 61, pl. 4. f. 6-11. Myoconcha aperta, D’Orb. Loc. Kertch. Iniron-ore. Collected and presented by Dr. M‘Pher- son. 79. DreisseNA (Mytiuus) Rostrirormis, Desh. Mém. Soc. Géol. France, vol. i. p. 61. t. 4. f. 14-16. This and the preceding species were found associated with the numerous and. peculiar forms of Cardium, hereafter mentioned, in the deposits of iron-ore near Kertch. Collected by Dr. M‘Pherson. There is also a specimen in the British Museum. 79 a.. DREISSENA INZQUIVALVIS, Nyst. Mytilus inequivalvis, Desh. loc. cit. pl. 5. f. 1-3. Collected by Dr. M‘Pherson. From iron-ore, Kertch. 144 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, SIPHONIDA. 80. CarpIUM PROTRACTUM, Eich. Voy. Hom. pl. 6. f. 6-8. This small species is common at most of the localities. Loc. Dock-yard, Sevastopol ; Quarantine ; Monastery ; and Gorge of Iphigenia. 81. CARDIUM AMPLUM, sp.nov. PI. IX. fig. 2, a—d. Shell thin, much broader than high, ornamented with about fifteen much elevated radiating ribs, which are strongly imbricated towards the margin, and unequally distant, widely separated and more curved towards the posterior slope of the shell, where the costee become suddenly closer ; umbones subcentral, margins crenulated, hinge-line long and but slightly curved ; right valve with a slightly prominent cardinal and two lateral teeth. Dimensions.—Height ;3,ths, breadth ;5ths of an inch. The only specimen of this small and delicate species is a very per- fect right valve. Loc. Monastery of St. George. 82. Carpium Demiporfl, sp.nov. PI. IX. fig. 3, a, 4, e. Shell elongated, subtrigonal, ornamented with about twelve widely distant and sharp ribs, closely imbricated and less prominent on the posterior slope of each valve ; umbones anterior and approximating, margins crenulated. Dimensions.—Height =5,ths, breadth 5% ths of an inch. Very abundant from the Monastery of St. George (in the bed R of the section) ; mostly casts of the interior. Our figured specimen has a portion of the shell still attached. This species differs from Cardium Fittoni by its greater breadth in proportion to its height, and in having more numerous and less elevated ribs, without the sharp and prominent asperities of that species. P Dedicated to M. Anatole Demidoff, author of the fine work on Southern Russia and the Crimea. 83. Carpium Firront, D’Orb. in Murchison’s Geol. of Russia. Loc. Sevastopol; Monastery. Casts collected by Major Cooke and Capt. Cockburn ; and, with the shell attached, from the Quaran- tine Harbour. 84. CARDIUM CARINATUM, Desh. Mém. Soc. Géol. de France, 1838, p. 54. pl. 2. f. 16-18. Loc. Kertch. Iniron-ore. Collected by Dr. M‘Pherson. 85. CarpIuM squamMuLosuM, Desh. ibid. p. 48. pl. 1. f. 14, 15. Loc. Kertch. Iniron-ore. British Museum Collection. 86. Carpium MAcRopOoN, Desh. ibid. p. 49. pl. 1. f. 3-6. An interesting specimen of this nearly smooth Cardium, in which the shell has been converted into phosphate of iron, the interior con-. taining crystals of carbonate of lime. Loc. Kertch. In iron-ore. Collected by Dr. M‘Pherson. 1857. ] BAILY—FOSSILS FROM THE CRIMEA. | 145 87. CARDIUM CRASSATELLATUM, Desh. ibid. p. 51. pl. 3. f. 7-10. Loc. Kertch. Iniron-ore. British Museum Collection. 88. CarpiumM PAucIcostatuM, Desh. ibid. p. 52. pl. 2. f. 14, 15. Loc. Kertch. In iron-ore. Two specimens collected by Dr. M‘Pherson. 89. CarptuM CoRBULOIDES, Desh. ibid. p. 54. pl. 1. f. 11-13. Loc. Kertch. Iniron-ore. Presented by Captain Cockburn. 90. Carpium VerRNnevi.i, Desh. ibid. p. 55. pl. 2. f. 9, 10. Loc. Kertch. In iron-ore. Presented by Captain Cockburn and Dr. M‘Pherson. 91. Carpium ovatum, Desh. ibid. p. 56. pl. 1. f. 19-21. Loc. Kertch. In iron-ore. Presented by Captain Cockburn and Dr. M‘Pherson. 92. Carpium Epovarp1, D’Orb. C. incertum, Desh. ibid. p. 56. Pee 1113. Loc. Kertch. In iron-ore. Collected by Dr. M‘Pherson. 93. CARDIUM SUBEDENTULUM, D’Orb. C. edentulum, Desh. ibid. p. 51. pl. 3. £. 3-6. Loc. Kertch. In iron-ore. British Museum Collection. 94, CARDIUM PSEUDOCARDIUM ?, Desh. ibid. p. 59. pl. 1.f. 1, 2. Loc. Kertch. In iron-ore. Presented by Captain Cockburn. 95. Cyprina Pauasit, sp.nov. PI. 1X. fig. 4, a, b. Shell large and thick, subtrigonal, broader than high, concen- trically striated, with an oblique angle on the posterior side of each valve ; umbones approximate, oblique and tumid. Cardinal teeth 3, with a posterior lateral tooth. Dimensions.—Height 15%, inch, breadth 2,4, inches. Loc. Monastery of St. George ; the shells being well preserved in crystalline limestone, and casts of the interior (the shell having de- composed) froma more sandy deposit. Fine casts of what appears to be this species were collected by Major Cooke from the left flank of a parapet of the Redan, the stone used in its construction having been procured from a quarry adjacent: the fossils from this deposit are mostly in the state of casts. 96. Cyprina GEorGEI, sp. nov. Pl. IX. fig. 8, a, d. Shell oblong-ovate, concentrically striated, with an oblique angle on the posterior side ; right valve with two narrow cardinal teeth, having a deep pit on one side, and a posterior lateral tooth ; muscular impressions oval, pallial line simple. _ Dimensions.—Height 1, breadth 14 inch. Loc. A single well-preserved specimen of the right valve only was collected from the Monastery of St. George. — VOL. XIV,—PART I, Mae. ciemueee 146 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, 97. CyPRINA NAVICULATA, sp.nov. Pl. IX. fig.-6, a-c. Shell oblong, the anterior extremity rounded, posterior very acute ; cardinal teeth 2, and a penmar lateral tooth. Dimensions. —Height 2 =ths, breadth =3,ths of an inch. Loc. Quarantine Harbour. The foasilé here have their valves. united ; a fortunate fracture in one specimen exposes the hinge. 98. Cyprina? TRIANGULATA, Sp. nov. PI. IX. fig. 9. Shell suborbicular, concentrically striated ; umbones prominent and oblique ; muscular impressions oval, pallial line simple. Dimensions.—Height 1, breadth 1,3; inch. This species is doubtfully referred to the genus Cyprina, none of the specimens showing the hinge, being mostly casts ; but, as it is one of the most numerous of the fossil bivalves from these deposits, it was thought advisable to figure and describe it. Loc. It has been collected from Sevastopol by Major Cooke; from Iphigenia and the Monastery by Captain Cockburn (in hed R). , °99. ASTARTE PULCHELLA, sp.nov. Pl. IX. fig. 10, a—e. Shell small, suborbicular, concentrically striated; two cardinal teeth. Dimensions.—Height ¢th of an inch, breadth the same. Loc. Nine specimens of this beautiful little species were collected, haying both valves united, from the Gorge of Iphigenia (bed J of the section), associated with other small shells. The left valve of a specimen being fortunately removed, the mould and hinge are shown. 100. ASTARTE QUADRATA, sp.nov. PI. IX. fig. 7, a—d. Shell very thick, oblong, depressed, somewhat square, concentric- ally striated ; umbones forming a sharp angle; hinge with two car- dinal teeth, lateral teeth phsestes pallial line deep, simple. Dimensions.—Height {ths of an inch, breadth 1 inch. Loc. Four specimens of this very thick shell were obtained from the Monastery, being fragments of the upper part containing the hinge of both valves well preserved. Several supposed casts of this species (fig. 7, d) were obtained from the same locality. 101. VENUS SEMIPLANA, sp.nov. PI. IX. fig. 5, a, 6. Shell oblong, depressed, concentrically striated, posterior side sub- angular; umbones anterior and acute; hinge of right valve with three cardinal teeth (the central one prominent) and one lateral tooth. Dimensions.—Height ;5,ths, breadth 7jths of an inch. . A single specimen of the right valve only, in good preservation. | Loc. Gorge of Iphigenia. 102. VENUS MINIMA, sp.nov. PI. IX. fig. 12, a—e. Shell elongated oval ; umbones anterior. Dimensions. —Height ;2,ths, breadth *th of an inch. Three specimens of dae very small aaa beautifully preserved shell with both valves united, were collected from the Monastery and Gorge Printed by Hullbmandel & Walton. W.H. Baily del. et lith. TERTIARY FOSSILS rrom tHE CRIMEA. 1857.]— BAILY—FOSSILS FROM THE CRIMEA. . 147 of Iphigenia in bed J of the section, associated with Astarte pul- cheila, &e. 103. Soten?, sp. A single fragment of the posterior extremity of an elongated straight shell apparently belonging to this genus. Loc. Quarantine Harbour. 104. Poramomya IpHIGENTA, sp.nov. Pl. IX. fig. 13, a—d. Shell thick, elongated and compressed ; umbones nearly central ; one cardinal tooth in each valve. Dimensions.—Height 1th, breadth Uths of an inch. Three single valves showing the interiors, Loe. Gorge of Iphigenia. 105. PHotas Hommaret, D’Orb. Voy. Hom. pl. 4. f. 16-15. Loc. Monastery, and Gorge of Iphigenia; from bed P of the section. | GASTEROPODA. OPpISTHOBRANCHIATA. 106. ToRNATELLA MINUTA, sp.nov. PI. X: fig. 7, a, 6. Shell small, cylindrical, smooth ; spire short, acute, with four or | five whirls ; aperture long and narrow, inner lip callous, covering part of the body-whirl. - Dimensions.—Axis ;2,ths, diameter ;4,th of an inch. Loc. Quarantine Harbour. 107. ToRNATELLA INFLEXA, 8p. nov. Pl. X. fig. 8, a, . Shell cylindrical ; spire short, with three or four whirls ; aper- ture long and narrow ; body-whirl inflexed or bent inwards at the middle. Dimensions.—Axis 3, breadth “ths of an inch. | This is a much larger species than the preceding, and differs in | being of less diameter in proportion to its size. Loe. Four specimens, all casts, were collected by Major Cooke, from the Redan. PULMONIFERA. 108. Hexix Dusotst, sp. nov. Pl. X. fig. 1, a, d. Shell subglobose, perforated, and finely striated, having five volu- tions with an elevated conoidal spire ; margin reflected, partly cover- ing the umbilicus. _ Dimensions.—Diameter ;8,ths, elevation ;$ths of an imch. _ This species occurs in considerable numbers, and was obtamed from a marly deposit (bed C of the section), of a bright-red colour, at the Monastery of St. George, and of a yellow tinge from the Gorge of Iphigenia. It was associated with the two next following species. 2 3 It bears a considerable resemblance to the recent H. arbustorum, but is smaller, and the spire not quite so elevated. itt __ Dedicated to M. Du Bois de Montpéreux, to whom we are in- debted for so full a description of the geology of that country, in his great work on the Crimea and the Caucasian Provinces. 4 EZ 148 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, 109. Hexrx Besrii, sp. nov. Pl. X. fig. 2, a-e. Shell small, depressed above, forming an obtuse angle on the body- whirl; under-side tumidly convex; about four whirls; umbilicus moderately sized and deep ; shen nefetted peristome. Dimensions.— Diameter ;3;ths, elevation 52;ths of an inch. This species was found associated with Helix DuBoisii and Bulimus Sharmani, &c., in light-brown marl. Loc. Gorge of Iphigenia. Dedicated to Edward Best, Esq., of the Geological Survey of Great Britain. 110. Butimus SHarMANt, sp. nov. Pl. X. fig. 3, a, d. Shell small, obtusely turreted ; whirls 5 to 7, more or less irre- gular in form and number ; aperture vee Dimensions.— Height ths, breadth ;4)ths of an inch. Loc. Gorge of Iphigenia. Dedicated to George Sharman, met .. of the Geological Survey of Great Britain. 111, PLANORBIS OBESUS, sp. nov. PI. X. fig. 5, a-e. Shell small, orbicular, and very stout, having six whirls, which almost cover each other; aperture compressed and pee Dimensions.—Diameter jth, thickness of outer whirl 5th of an inch. Found associated with the previously described land-shells, Nos. 108, 109, and 110. Loc. Gorge of Iphigenia. 112. PLaNorzBIs CORNUCOPIA, sp. nov. Pl. X. fig. 4, a, b. Shell large, formed of four nearly round volutions separated by a deep suture, the outer volution having two or three transverse con- strictions. Dimensions. —Diameter 1 inch, thickness of outer whirl ,%,ths of an inch. Loc. Of this elegantly formed freshwater shell, the finest spe- cimen is in the Woolwich Royal Artillery Institution, collected from before Sevastopol by Major Anderson, R.A. One other specimen was obtained by Captain Cockburn from the Gorge of Iphigenia (bed P of the section). 113. CycLOSTOMA RETICULATUM, sp.noy. Pl. X. fig. 6, a, 6. Shell turbinated; surface spirally striated and crossed by very fine transverse lines; axis perforated; aperture nearly circular ; whirls 4 or 5. Dimensions of imperfect cast.—Axis ;‘5ths, diam. ;*jths of an inch. This cast retains a-portion of the shell attached, showing distinetly its reticulated sculpture. Loc. Gorge of Iphigenia (bed C of the section). Associated with the land-shells before described. PROSOBRANCHIATA. | | 114, Turso, sp. Casts of a large turbinated shell, which may eS 1857. ] BAILY—FOSSILS FROM THE CRIMEA. 149 be referred to this genus, too imperfect for description, were col- lected by Major Cooke from the Redan. 115. Trocuus CorpErianvus, D’Orb. Voy. Hom. Very abundant at the Quarantine Harbour, sixteen specimens having been obtained from that locality, the deposit in which they were imbedded being a fine-grained compact yellowish marl, particularly rich in specimens of this genus: they are mostly in beautiful preservation, the shells having become crystallized. 116. Trocuus Fenonranvus, D’Orb. Voy. Hom. Loc. Quarantine Harbour. 117. Trocuus Pacreanus, D’Orb. Voy. Hom. Loc. Quarantine Harbour. 118. Trocuus MurcuisonI, sp. nov. Pl. X. fig. 13. Shell obtusely conical, elevated, having five or six volutions ; slightly convex, with about three transverse somewhat granular ridges on each whirl ; base convex, imperforate ; aperture suborbi- cular. 3 Dimensions.—Axis 1,2,ths, diameter ;{>ths of an inch. Loc. Quarantine Harbour. Dedicated to Sir Roderick I. Murchison, Director-General of the Geological Society of Great Britain. 119. TrocHus ANDERSON], sp. nov. Pl. X. fig. 14, a, d. Shell conical, with flat sides and elevated spire; volutions six, ornamented with about five irregular elevated ridges; base nearly flat ; columella suboblique ; aperture trapeziform. Dimensions.—Axis ;4ths, diameter ;°,ths of an inch. Allied to 7. Voronzoffi and T. Pageanus, D’Orb. Voy. Hom., but differs from the latter species by its smaller diameter, and in the ridges not being granulated. Loc. Monastery of St. George. Dedicated to Major Anderson, Royal Artillery. 120. Trocuus Beaumontu, D’Orb. in Voy. Hom. Loc. Monastery of St. George. .21. Trocuus Buarnvitzet, D’Orb. in Voy. Hom. Cast of the interior. Loe. Gorge of Iphigenia. 122. Trocuus Hommaret, D’Orb. in Voy. Hom. Loe. A fine and perfect specimen from the Quarantine Harbour collected by Capt. Cockburn, and a less perfect one from Sevastopol collected by Major Anderson, R.A. 123. TROCHUS PULCHELLUS, sp. nov. PI. X. fig. 15, a, 0, ¢. Shell very small, with an acutely elevated spire ; whirls five, orna- mented with three sharp much-elevated and crenulated transverse ridges; base convex; aperture suborbicular ; umbilicus small. Dimensions.—Axis ;3,ths, diameter ;2,ths of an inch. Loe, Quarantine Harbour. 150 PROCEEDINGS OF THE GEOLOGICAL society. (June 17, 124. Trocuus SUTHERLANDII, sp. nov. Pl. X. fig. 16, a, d. Shell with a short pyramidal spire ; whirls rounded, five in num- ber; base convex, slightly umbilicated ; body-whirl with four or five slight and unequally distant spiral carinations, crossed by numerous faint and regular transverse lines ; aperture nearly circular, Dimensions.—Axis ;5ths, diameter ;3,ths of an inch. Loc. Monastery of St. George. Dedicated to Dr. Sutherland, of the Sanitary Commission, Army 7 of the East. 125. Trocuus LyGont, sp. nov. Pl. X. fig. 17, a, 6. Shell depressedly conical, trochiform,volutions four, convex: suture broad ; aperture subcircular ; umbilicus large and deep. Preece —Axis ths, diameter 18ths of an inch. Loc. Monastery and Gorge of Iphigenia, collected by Capen Cockburn ; also casts of two small specimens from the Redan, col- lected by Major Cooke. Dedicated to Lieut.-Col. Charles Lygon Cocks, of the Grenadier Guards. 126. Lirrorina Monastica, sp. nov. Pl. X. fig. 9, a-e. Shell globular, imperforate ; spire small, obtuse ; volutions three, spirally striated and crossed by faint transverse lines of growth; aperture large, nearly circular ; inner lip callous, covering part of the body-whirl. Dimensions.—Axis ;4,ths, diameter aths of an inch, Loc. Monastery of St. George. 127. PALUDINA ACHATINOIDES, Desh. Mém. Soc. Géol. France, 1838, p. 64. pl. 5. f. 6, 7. Loc. Kertch. Iniron-ore. Collected by Dr. M‘Pherson. 128. CerirHium CaTTLEy4, sp. nov. Pl. X. fig. 12, a, d. Shell turreted ; spire short; whirls five, with about three rows of largely granulated bands; aperture subquadrate ; columella recurved and without a fold. Dimensions.—Axis ;>ths, diameter ;4,ths of an inch. Allied to C: Taittboutti, D’Orb. Voy. Hom.; the tubercles ‘are, however, more distinct and fewer on each whizl.- Loc. Monastery of St. George. There are also two specimens in the British Museum Colleciten, presented by Mrs. Cattley, to whom this species is dedicated.. 129. CeERITHIUM COCHLEARE, sp. nov. PI. X. fig. 10, a-e. Shell elongate, turreted, regularly tapering ; whirls seven in num- ber, with longitudinal sth aperture aes Dimensions.—Axis ; ths, diameter ;%,ths of an inch. Loc. Gorge of Iphigenia (bed J). 130. CERITHIUM TRUNCATUM, sp.nov. PI. x. fig. 11, a, b. Shell small, turreted, obtusely conical ; whirls four ; outline of the 1857. | BAILY—FOSSILS FROM THE CRIMEA. 151 spire slightly swollen towards the middle, top obtuse asif truncated, ornamented with three bands transversely striated and elevated into costz ; aperture subquadrate. Dimensions.—Axis ;4,ths, diameter “th of an inch. Loc. Gorge of Iphigenia. 131. PLEURoTOMA CHERSONESUS, sp. nov. PI. X. fig. 19, a-c. Shell fusiform, turreted, lower whirl with ten longitudinal costz, having two rows of nodules at the upper part of each whirl, trans- versely striated; aperture elongato-ovate, with a short sinus at. its upper part. Dimensions of imperfect specimen.—Axis ;>ths, diameter =4,ths of an inch. Loe. Gorge of as and the Monastery (bed R of the sec- tion). 132.. PLEUROTOMA LAQUEATA, sp. nov. PI. X. fig. 18, a, 6. Shell turriculate and fusiform, volutions elongated and longitudi- nally costated, passing into two rows of obtuse nodules next the suture; aperture elongato-ovate. Dimensions of imperfect specimen with two whirls.—Axis ;5ths, diameter =3;ths of an inch. Loe. Monastery of St. George (bed R of the section). 133. BuccinuM OBESuUM, sp. nov. PI. X. fig. 20, a, 6. Shell ovato-conical; whirls ventricose with distant slightly raised costz ; aperture oval; canal short and reflected. Dimensions of cast.—Axis ;8,ths, diameter ;°;ths of an inch. Loc. Monastery, and the Gorge of Iphigenia (bed R of the see- tion). 134. BuccinuM ANGUSTATUM, sp. nov. PI. X. fig. 21, a, 6. Shell elongated oval, narrow; whirls four or five, with about ten slightly raised and distant costze ; aperture oval; canal short. Dimensions.—Axis ;5,ths, diameter ;4,ths of an inch. Loc. Monastery of St. George. 135. BuccINUM MONILIFORME, sp. nov. PI. X. fig. 22, a, 0. Shell ovato-conical ; whirls five, angular; spire elevated, with slightly raised costee ; the upper part of the whirl bears an angular band of elongated obtuse nodules, and a row of bead-like obtuse no- dules next the suture of each whirl; aperture oval; canal short and reflected. Dimensions.—Axis ;8,ths, diameter ;3,ths of an inch. Loc. Gorge of Iphigenia. 136. Bucctnum Dovutcuin#, D’Orb. Voy. Hom. pl. 3. f. 20-22, Loc. Monastery of St. George. 137. Buccinum Dave.vuinum, D’Orb. Voy. Hom. pl. 3. f. 23, Loe. almaale of St. George. 152 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, 138. Buccinum corsianuM, D’Orb. Voy. Hom. pl. 3. f. 24, 25. Loc. The Quarantine, Monastery, and the Gorge of Iphigenia. 139. Buccrnum pissituM, Eichw. Murch. Russia, pl. 43. f. 35, 36. Loc. The Monastery, and the Gorge of Iphigenia. A few remarks naturally arise from an examination of the species. Commencing with the oldest or Jurassic, these bear the greatest re- semblance in specific identity to those of our own country; the characteristic examples of Terebratula numismalis from the lowest fossiliferous beds serving to point out the shales of the Woronzoff road to be equivalent with those of our Lower Lias, as the presence of Rhynchonella acuta, Gryphea incurva, Ammonites Jurensis, and A. fimbriatus from the village of Biasali, indicates the Marlstone or Middle division of the Lias. The fossils received from Balaclava (principally Brachiopoda) appear to be related to forms from the Lower or Inferior Oolite, — although for the most part specifically distinct from any met with. in England ; Rhynchonella senticosa, an Inferior Oolite species, bemg the only one I have been enabled to identify from that locality. Fossils from the intermediate formations of the Secondary age are absent in this collection, although several species, principally Cepha- lopoda, are catalogued as belonging to the Oxfordian division from Baktchserai by M. Du Bois de Montpéreux, and from Kobsel on the south coast of the Crimea by M. D’Orbigny. In this collection are contained several species, principally Zoo- phyta, from Soudaxioxia, forming part of a series formerly presented to the Museum of Practical Geology by the Imperial School of Mines at St. Petersburg. These fossil corals are perfectly undistinguish- able from similar species met with in the Coral Rag of Steeple Ashton. The Neocomian or Lower Greensand group, as well as the upper division of the Cretaceous series, has some few fossils identical with British species. The principal part of the fossils from this forma-~ tion are from Baktchserai, and are catalogued by M. Du Bois in his ‘ Tableau de Fossiles de la Craie en Crimée.’ An interesting form of spiral bivalve belonging to the Chamide, allied to our Requienia (Diceras) Lonsdalii, but more nearly to Requienia Ammonia, Matheron, occurred in great abundance, ac- companied by a large Nerina allied to N. gigantea. Many frag- ments of these species were collected by Major Hudson, 39th Regi- ment, from a very coarse crystalline limestone used in the construc- tion of roads between Balaclava and the Plateau. The Upper Chalk of Inkerman has supplied several species (prin- cipally Ostrea) common to our own country; the most important and beautiful fossil, as well as the most abundant, from this locality is the Crania spinulosa, Nilsson, before alluded to. The Nummulitic or Older Tertiary fossils are also principally ca- talogued by M. Du Bois in his ‘ Tableau,’ as occurring at Baktch- serai. This collection contains some large and characteristic species Number of specimens ee) » ey oe) 1857.] BAILY—FOSSILS FROM THE CRIMEA. 153 from Simferopol, amongst which are the large Echinoderm called Conoclypus conoideus, Ostrea gigantea, and Cerithium giganteum. Of the Foraminifera the principal species are Nummulites distans, Deshayes, and Nummulites Raymondi, D’Archiac (N. rotularius, Desh.). Several species of Mollusca included in M. Du Bois’ list, such as Cardium porulosum, Cerithium giganteum, Fusus turgidus, Voluta muricina, and V. luctatriz, with Turritella imbricataria, are common in the Barton and Bracklesham beds of this country. The Middle, or Newer Tertiary formation, which, under the name of Steppe Limestone, covers the largest extent of country in the Crimea, is abundant in fossils having peculiar characters different from those of any deposit in England, being closely analogous to forms at present existing in the great inland salt seas of the Aral and Caspian. The peculiar forms of Cardium and Dreissena found in the deposits of iron-ore near Kertch and in other parts of the Crimea, of brackish-water origin, are believed to indicate the former existence of a great inland sea, of which the Aral and Caspian are remnants, but which was larger than the present Mediterranean; a belief of which the illustrious Pallas was the first propounder. The Mollusca from other Newer Tertiary deposits near Sevas- topol are more marine in their character, the Bivalves belonging principally to the genus Cyprina, the Univalves to peculiar. forms of Buccinum and Trochus: of the latter, 11 species were collected, 6 being identical with forms figured in the ‘ Voyage of M. Hom- maire,’ and described by M. D’Orbigny, from Kichimev in Bessarabia : they also occur in the Tertiary deposits of Podolia and Volhynia, indicating a probable contemporaneity of all these geological forma- tions. Table of Jurassic Fossils found in the Crimea. Name. | Locality. Lias. Bees One Amorphozoa. 1 |Scyphia Cockburnii, Baily. Pl. VIII.|Near the Monastery of| ...0.0. * fig. la, d. | St. George. Zoophyta. Comoseris irradians, Edw. seseenceeces| SOUGAXIONIA. ..cesesecsvees eeanes * Thecosmilia annularis, Flem., sp.... Simferopol ...........0.06] seeeee ee * Isastrea Greenoughii, Edw. ........- NOUGANIONIAsS.os.se8ss0ss: Leseve ere * ? Astrea polygonalis, Mich. | explanata?, Goldfisss.seccsoceres Between Monastery and| ...... | * Balaclava. Thamnastrea arachnoides, Park.,sp.|\Soudaxioxia....ss..sseeee.| cveees oes % Calamophyllia Stokesii, Hdw. ...... Between Monastery and| ..... : * Balaclava. Montlivaltia trochoides, Edw. ...... Tchatyr Dagh ..... eeaees Beatles * - Echinodermata. Cidaris ? (Spe) ......ccecccvecscncoesse| WOLONZOL Road ....000es % Seaplane saeaceond ke tipertee ison res Gorge of Iphigenia wee] eesese * — Blumenbachii (spines), Goldf..| SOUAXIOXIA, cerssersngees! caves sea * 154 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, aa E Z Name. Locality. Lias. £°S Ze 1 |Cidaris glandifera, Goldf.-. svsasiseees Between Monastery and| ...... ; Balaclava. QZ jamie Pi hasdessahentcmeeertebenveuseness GOs “avisc.cceeereed ete! SAL 2 | eeee Tl icaccteseedetus de teuten eds. May 1 mile W. of Balaclava.| ...... 2 |Apiocrinites incrassatus, Ramer |Between Monastery and| ...... (joints). Balaclava. 8 |Pentacrinites basaltiformis, Mill. ...|Soudaxioxia........scsesse| ceeses 2 (StHrtists (WIAGES) see cceverssaeste testes ce Gorge of Iphigenia......} ...... Mollusca. 4 |Terebratula numismalis, Zam. ......|Woronzoff Road ......... * 1 |—— rotundata?, Roemer .........06. Woronzoff Road ......... + 1 |—— Jamesii, Baily. Pl. VIII. fig. 2. |Balaclava..........ceceeces| cece 1 |—— subovoides ?, Minst........+.... Between Monastery and ...... Balaclava. 1 perovalis ?, Sow.......... Patosvess Biasal . 0 sii.0s Jit cai Marlstone. 1 Strogonofii ?, D’Orb..........+0 Eplsigeniagyiasi< peau slseapientiae 6 |Terebratulina radiata, Baily. Pl. VIII.|Balaclava.........16. esses| ceesee _ fig. 3 a-d. 2 |RhynchonellaCookei, Baily. P1.VITI.|Balaclava......sssccecsesss| seesee fig. 5 a, d. 1 |—— pectinata, Baily. Pl. VIII.|[phigenia....... spares ny eee _ fig. 4a, b. 1 |—— senticosa, Von Buch .....ccc000- Balaclava.o:ssnestscehees wal fiat 1 |—— acuta, S0w.....,.cerrecseecccsoeses Biasali j..007.+5 ao esmaiemians Marlstone. 1 |—— variabilis ?, Schloth. ............ Tpligenia.:t.ss.c, 2556 Apts beeen Avicula decussata, Rens. (ie BGs) 2 ERE RAR * S (OWE, Spi: Ty seatsags tees ibe sac paedeeg Karand iy :scsacdaastecsieh ee *? ok fe naa bee edie eon beltesinetians Seinntes Woronzoff Road ......... Eb, | Ssccansiacsavonsa st aeeeweseaenedganie 1 mile W. of Balaclava.| ...... 2 Gryphiea dilatata, SOWs 2. die .oceosenc NOUGARIONIA.s.c,cescosaess seeeee 1 INCUTVA, (BOM s ion 5stxhse bebe 34 heer Biasali Village............ Marlstone? 6 |Cardium equistriatum, Baily. Pl.|Woronzoff Road ......... * . Vill, te, 6 a, 6. 4 |Astarte complanata, Remer ......... Woronzoff Road ......... * Pholadomya conformis, D’Oré....... Se Coast. /Grimien, cscs ed) cecaee DUN GRIERs SIi 1; sams'sees sats spew seme alesis Between Monastery and) ...... Balaclava. 1 |Neripeea grandis, D’ Orb. <.......0-.. Vil. Djanatai ........+ a eer Chemnitzia Heddingtonensis, Sow.. Belemnites latisulcatus, Voltz. ...... MGDBEL) 25 ws cesar. senereees |e eee — hastatus, Blainv. ............06- EODSE! 50d. cocsdnesecesesten|) eee 1 |Ammonites Uralensis ?, D’Ord....... 1 mile W. of Balaclava.) ..| 1 |—— Raquinianus ?, ? D’ ORGS eo ea Vail \Biasali .s.esccecsnee ++] Marlstone, 1 Jurensis, Zieten paseenesia es csemay Ady canenceanautens Mailstone. 1 |—— fimbriatus, Sow...........ceeevee ODi5. ces saaesqpagaes Marlstone; —— Brongniartii?, Sow. (Du Bois) |Baktchserai.......++...+++ saan: —— giganteus, Sow. (Du Bois)...... Batis) ss casae shiewet Sabi. cekn —— perarmatus, Sow. (Du ane ABs s Vercdesccdessserl ie cece -lunula, Zieten (D’Orb.) . ..|Kobsel, S. Coast, Crimea} ,.... : —— viator, D’ Orb. wsccccsecsereeenes do. dQ, spae= selon eesbhe —— Tatricus, Pusch,...cec.scceseee sent (Be GOs) esos saan — Hommarei, D’Orb. ...000..0005 do. ihe pe eee ——4 Adele, TOPE: ones teeeteceentes do. G05. ain ee 3 —— tortisulcatus, D’ Orb..........06. Kobsel ait Soudagh oo} sso. 1 ‘lPrigpnellites, ‘Spii?.) deen cadensee ccs --|Woronzoff Road ......... * —— Theodosia, Desh. ...cccrssecceee > eked i: Rhynchoteuthis antiquatus, D’ Ord. ? Tit i ee ee Infer. |(Oxfordian) Ovlite.| Coral Rag. %* *& X %* OE Hae we #? * Callovian. Low. Oxf, Portland? * * Low. Oxf. * Low. Oxf, Oxford. * 1857.) | + SBAILY—FOSSILS FROM THE CRIMEA. 155 Table of Cretaceous Fossils found in the Crimea. (Lower Cretaceous or Neocomian.) is Z Name. Authority. Locality. | ag 2 a3 zo ~ pener morphozoa. ‘|Scyphia Oeynhausii, Goldf. ...;Du Bois de Montpéreux, Tableau de|Baktchserai. Fossiles de la Craie en Crimée —— furcata, Goldf. ......0.00.. do. do. waiiee do. Manon capitatum, Goldf. ..,... do. Gee a nctane do. Zoophyta. Astrea tubulosa, Goldf., & var. do. do. shades do. _|—— caryophylloides, Goldf.... do. do. dspess do. — continua, Goldf......... ake do. do. gees do. —— cristata, Goldf. .....s00... do. dow... «\a2ang do. Meeandrina ........ Peer er errr en do HO: aieiks do. PMMA GA vciiuaienesrdssededenes +s do aris. eb gBee do EAtH@UENGTOU (cas conisasessace ses do il ae ee do Pavonia (?Fungia discoidea, Gas). sites Sibiasees es do dai’. sedate do. Echinodermata. : Discoidea macropyga, Desm.... do ae i scceee do. Cidaris clunifera, 4gas. .... do or seers do. —— vesiculosa, Goldf. ......... do ot MSF do. SE eMIGING. wus de cance egos seeeesae do. Ct a mes do. Dysaster cordatus, Baier ...... Du Bois, Voy. au Cauc. pl. 1. f. 2-4. |Crimea. Bryozoa. Ceriopora dichotoma, Goldf. ...|\Du Bois, Tableau de foss. de la Craie.| Baktchserai. —— striata, Goldf.....ccseecceeee Co) CER ae eee ) ——— MICTOPOTA .2....ceessecccees do dg.) sbsiss do Mollusca. Terebratulina striata, Wahl. ... do. dos Eres do. Terebratula biplicata, Sow....... do. do. ponies do. flabellata, Goldf. ......... do foe tesnene do —— diphya, Von Buch ...,..... do do. ts do —— decipiens, Du Bois....... “ do do. esndee do —— vicinalis, Schiot............. do Ce do Rhynchonella alata, Goldf. do Cire > ceeees do AIS Delcehasia ASReSececeaeeeenees do GO: ..< ¥usdae do. Ostrea caleheied., PES ees do do. ats ee do —— nodosa, Miinst. ..........0. do doe eee do frons ?, Park. (gregaria, do i. dail tea do Du Bois). -exopyra, Mich. ...0.....05. do Hos "ieee nee do Pépten, Spt ..<.vowrteaseees-..c5 tt do He.) Cipiocs do . |Lima ovalis, Desh. ......0... weaes do Gar?) ete do elongata, Miinst. ......00. do do. cae do Spondylus. ....,100..c.sescaressene do CS ahaa ss do Exogyra Couloni, Defr.......... do. GQ. asae- do. o— lateralis, 0 basi do, do. deaes do. _ minima, Du Bois ...... 8 do do. eee do. ~ _ |Gervillia solenoides, Defr....+. do. Ds: |: whteat do. 156 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, Table of Cretaceous Fossils (continued). H g Name. Authority. Locality. 268 Es ge , Arca globosa, Du Bois ..,......|Du Bois, Tableau de foss. de la Craie.| Baktchserai. ——, SP. NOV. .sceeesseretesseenes 20 |Requienia, sp. NOV.......sesccceee Baily... sesscascedsnakevaecaenteee reese ..(Near Balaclava. ? Prionia globosa, 4@.........0.4. Du Bois, Caucas...... anaes Hapteneas Baktchserai. Corimya taurica, 4g. ............ i A Mi mes Se Es 8 do. WritOn, Sloe hecsdecaenesenenacenesce Du Bois, Tableau, rd a ee do. 1 |Natica prelonga, Desh. ........- Baily; D’Orb. Ter. Crét. pl. Vie sh, Near Balaclava. 12 |Nerinea gigantea?, D’H.-Firm.|Baily ; D’Orb. Ter. Crét. ii. pl. 158.. do. 1 J SP. MOV. ...csessececscscceces Baily eeiisceermtecedcercs Keone l/r Geis: Wer pie Saeed iiveweciecescaceccsoss QO hecevars ches it CaaS eee RR Inkerman.. so (U, Che 2 |Turritella, sp. ....... Sunwacwetsiass GO. sacrscccoracces seseceees seers] do. U. Ch. Belemnitella mucronata, ‘Schiot.|Du Bois, Tableau, &c. ......++. Baktchserai|U. Ch. Wy rtiGaNaIS is eS is Sct penanc ons do. do. sesesssese| GO. ...(Ch. M. Ammonites asper, Von “Buch. ’ (—— constrictus, Du Bois) f ia Se mae do. _ ...|Gault? Scaphites constrictus, Sow. ae a Sai nt oe Vertebrata. Pisces. : 1 Lamna ? PTUTTTITT TTT Baily TYTAXETT TL hy Inkerman... U. Ch. 158 PROCEEDINGS OF THE GEOLOGICAL Society. [June 17, Table of Older Tertiary Fossils found in the Crimea. (Nummulitie =Suessonian, D’ Orbigny.) 4 : ‘Name. Authority. , Locality. #3 3 oO Zz ‘be ged Foraminifera. x |Nummulites distans, Desh. .».....|Deshayes; Baily....,s++++..++é+06 | |Near Simferopol e Raymondi, Desh. .......cseeeseeese do. Ge sess aeusbceinbcoes and Inkerman. Echinodermata. Conoclypus conoideus (Clypeaster|Cat. p. 109 ; Echin. Oe i. p. 64.|Near Simferopol, DuBoisii), 4g. pl. 10. f, 16; 67. oh 10.| River Salghir. f..- 11-134 Du Bat, Voy. au ‘ Caucase. Spatangus depressus, Du Bois ...|Voy. au Caucase, pl. 1. f. 16. Amblypygus latus, 4g. .......+0++|/Du Bois, Caucase. ......se0eeese0s..(Salghir: Mollusca. Terebratula vitrea?, Zamk. ......|Du Bois, Tableau, &¢. .........0 Baktchserai. Ostrea gigantea, Brander Selnewics Deshayes; Baily.......... ey .-|Near Simferopol. POUT, SP. ccsscedenthactsse. iisenns Du Bois, Tableau, &c. .........0.- Baktchserai, Spondylus asperulus, Mins?....... do. GO. sangre vaxensben do Cardium porulosum, Brander ... do dO. sygsingtess meee do Crassatella tumida, Lamf.......... do i eee tele sAtsnanel do. Tsocardia, Sp. ...cccssesee RetcweMicacn do MO. asin soneoones do TrigOnia, Spy. s0edncstscdsseee cance do. do. neap gait do MUSE; SPF jis eveddssonhisiernces cers do Os") \ cwunsee wenden do Fusus Ficulneus, Lamarck . dL gauksne do 0S cases REE do. GVa +s igcteehescudbaunteesiarsee assess do Na «tehicoh aba kane do. Voluta muricina, ‘Lamk bine oweuaee ers do GO; . -clecusharndenee do luctatrix, Seven setcvessecden: do do. oe do Mitra terebellum, Zamk. ......... do. do. ~ asthccndkakal do Ovula tuberculosa, Duclos .......+. do HO. |” sue sseeenseee do Cerithium giganteum, Lamkh....... do HMOs Vi spect ceaieaees do. Turritella imbricataria, Zamk. ... do 2 Lo ama NS do - |Trochus giganteus, Du Bois ...... do 0s. ees sxesasen do. Table of Middle or Newer Tertiary Fossils found in the Crimea. (Falunian, D’ Orbigny.) ‘ 3 Name. Reference. . Locality. 24 | r au racir aac tases a 7, Amorphozoa. 2 |Scyphia Portlocki, Baily ......|Pl. IX. £1, b, see.scseoeeeeee...| Monastery of St. George. . Foraminifera. Polystomella crispa, Linneus...|Syst. Nat. 3370 ......+0+e00+00.+-| Near Sevastopol. Mollusca. ‘L {Mytilus apertus, Desh. ....++...|Mém. Géol. Soc. Fr. 1838, t. 3. Kertch, in hued p. 61. pl. 4. f. 6-11. posits. 1857.] BAILY—FOSSILS FROM THE CRIMEA. 159 Table of Middle or Newer Tertiary Fossils found in the Crimea (continued), Sa x 8 Name. Reference. Locality. 2E g°5 Ze Mollusca. Mytilus Calypso, D’ Ord. Mém Géol. Soc. Fr. 1838, t. 3.|Kertch, in iron-de- subcarinatus, Desh. ... p. 62. pl. 4. f. 12, 13. posits 1 |Dreissena rostriformis, Desh....\ibid. p. 61. pl. 4. f. 14-16 water do. do. 1 inzequivalvis, Desh........++ ibid. BUSES 53 ea, ctv do. do. 3 |Cardium carinatum, Desh....... ibid. p. 54. pl. 2. f. 16-18 ...... do. do. —— planum, Desh. ......000.. ibid. p. 46. pl. 2. f. 24-30 ...... do. do. — depressum, Desh. ......... ibid. p. 47. pl. 2. f. 19-23 ...... do. do. —— subemarginatum, D’Or. | |.,. crt aah Desh.) | (bid: p. 48. pl 1. f 7-10 ...., do. do 2 |—— squamulosum, Desh. ......\ibid. p. 48. pl. 1. f. 14, 15...... do. do. ~ |—— sub carinatum, Desh. ...... ibid. p. 49. pl. 3. f. 1, 2,6 ...... do. do. 1 |—— macrodon, Desh. ......... ibide. p: 49. 7pl. IS & 3-6 «2.0.0... do. do. 1 |— erassatellatum, Desh....... ibid. p. 51. pl. 3. f. 7-10 ...... do. do. Gouriefli, Desh. ........00- ihid. p,. 52. pl..3.£. 1.2 esyuvtes do. do. 3 paucicostatum, Desh. ibid; p. 52. pl. 2. £14; 45a ice. do. do.. — sulcatinum, Desh, ......... ibid. p. 53. pl. 2. f. 3-5 ......... do. do. —— subplanicostatum, D’O. | |... | a aaa a \ ibid. p. 53. pl. 2. £. 7) 8 .ece.-.| do. do. 1 corbuloides, Desh. .......+. ibid. p. 54, pl. 1. f. 11-13 ...... do. do. 4 |—— Verneuilii, Desh. ...s00... ibid. p. 55. pl. 2.7.9, 10 ...... do. do. 4 |—— ovatum, Desh. ........... ibid. p. 56. pl. 1. f. 19-21 ...... do. do. 1 |— Edouardi, D’Orb. ..... | |-1- ie ae aa oh ila \ ibid. p. 56. pl. 2. f. 11-13... do. do subdentatum, Desh. ...... ibid. p. 57. pl. 1. f. 16-18 ...... do do. 1 |——subedentulum, D’Ord. ) |.,. et tae | ibid. p. 51. pl. 3. £ 3-6 s.ccee0ee do do. —— acardo, Desh. .oc......sesee ibid. p. 58. pl. 4. f. 1-5 ......... do. do. 1 |— pseudocardium, Desh. ...\ibid. p. 59. pl. 1. f. 1, 2.......4. do. do. 18 |—— protractum, Hichw. ...... Voy. Hom. pl. 6. f. 6-8 ......... Quarantine Harb. 2, Monastery 8, and Gorge of Iphi- genia 8. 1 |—amplum, Baily ....cccccees Pl. IX. f. 2 a-d. ......ss0000.0....|Monastery. 20 |—— Demidoffi, Baily .,....... PL IX. £3 a=c .....iasu ieee do. i 4 |—— Fittoni, D’Ord. .......000- Mureli,. Biieiniks..cvessmuecivisi. Sevastopol 2, Qua- —— (six other species of Car- rantine 1, Mona- dium undeterminable, from stery 1. Quarantine, Monastery, Iphi- genia, and Sapoune Height). 8 (|Cyprina Pallasii, Baily ......... PU ER Bas Bsn siasevetscicetis Monastery 1 |—— Georgei, Baily ......000... PILTM £8 a,b ..cagivsdsscwiscakd Monastery 3 |—— naviculata, Baily ......... PI. IXs £ G aac. . wesivssarecrtive Quarantine Harb 15 |—— ? triangulata, Baily ...... Oe ee oe ae es ive ssa ..+.. Sevastopol 2, Mo- nastery 11, Iphi- genia 2. 9 |Astarte pulchella, Baily......... PG £10 G6 «ise wecsccdevsent Iphigenia ; bed J. 8 quadrata, Baily .........04 ie US Boho, Soc ssccnepeeweene Monastery. 1 |Venus semiplana, Baily ......... a. ES GB. pasnacstean phaxaes Gorge of Iphigenia. 4 |—— minima, Baily ..... seareet(Ele Le U2 a=6 oeons possnewet »-..(Monastery 1, Iphi- : genia 3; bed J.. DESO, SP .5 LOU sas. stvenseennceas|nuss ine ssadebveties sucess peicsccnccens Quarantine Harb. - $8 |Potamomya Iphigenia, Baily...\Pl. IX. f. 13 ad be onaam seems ...»e. Gorge of Iphigenia. 10 |Pholas Hommarei, D’Or%....... Voy. Hom. pl. 4. f. 16-18 ...... Iphigenia 3, and Monastery 7. Number of &/specimens. is] to m bo <—— KH HPOKMDEK HHH One We Oo nds Co 16 — me °) 160 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, Table of Middle or Newer Tertiary Fossils found in the Crimea (continued). Name. Reference. Locality. Tornatella niunuta, Batliy- s...2<\Pl. Xf. 7G) Ge oeeteaetsec se eene -.(Quarantine Harb. —— inflexa, Baily ......c0esceee PLR. PAB, Vases cctee eb denaaeeene Redan, near Seva- stopol. Helix DuBoisii, Baily............ PIAS: £4, BA vost. atiiecaeeniee Monastery 10. Iphigenia 12. —— Bestii, Baily ....cccccsceees Pl. Xi. £2 A-€ .occscseescsecessoone{l PRIGCIIEs Bulimus Sharmani, Baily ...... Pl) My DG, D inciccinnncen dete ..... (Iphigenia. Limnza peregrina, Desh. ......|Mém. Soc. Géol. Fr. t. iii. p. 63/Kertch. —— obtusissima, Desh.......... Ibid:f. "Vc. sete eee eae Kertch. —- velutina, Desh. .........060¢ ibid. £; T2-14 Ge wonseeee eas Kertch. Planorbis obesus, Baily ......... Pik, fiance evant anes Iphigenia. —— cornucopia, Baily .........|Pl. X. f. 4 a, x wis - = - ‘— a a a = ' ‘ " a oes Sars ‘ . = . oe , A ‘ a ae , : or ie Pot = te ; : ; a 4 - ‘ @ ben 7 a 7 . ite ot . : - : ie 7 . 3 . oi iret aa ems ie 5 a ra A td oA’ > f . . y ; : . nn iy 4 ; ae. eae ( | res “ed < : sae a eM > : oe ‘ : * ‘ - = ‘ » - : F ° } = » ‘ ; . 7 ‘ ; * i as 7 - THE QUARTERLY JOURNAL OF THE GEOLOGICAL SOCIETY OF LONDON. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. JUNE 17, 1857. [ Proceedings continued from page 176. ] 11. On the Grouoey of the NorTH-EAST PART of the DoBRUTCHA. By T. Spratt, Captain R.N., F.R.S., F.G.S. Havine had an opportunity, during the latter part of last year, of extending my geological inquiries in the eastern part of the Dobrutcha, and of obtaining a better idea of some parts of its character, I am induced to offer a few remarks as a continuation of my former paper on this locality*. It is known that the northern extremity of the Dobrutcha is ter- minated by a chain of mountains that obtain an elevation of between 1000 and 2000 feet. They consist of highly-inclined limestones, shales, and schistose rocks. But the bold features usually assumed by the description and elevation of rocks of this nature are generally subdued here by their flanks and shoulders being covered by a considerable deposit of arenaceous marls, of reddish, grey, and brown colours. The marls are undoubtedly of alate date; but their origin I am not able to determine, from the total absence of fossils wherever examined by me. | In this remark I allude especially to the group of superficial, earthy or arenaceous, red and brownish marls of the Steppe, separable from the known freshwater marls; for I have recently * See Quart. Journ. Geol. Soc. vol. xiii. p. 77. VOL. XIV.—PART I. P 204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, ascertained that the former are not a continuation of the lower fresh- water deposits which I have already noticed at Kustenjeh, and as I once supposed. I shall commence my remarks at the north end of the Dobrutcha by simply referring to the existence of these older rocks at Isatchka, Tultcha, and Besh Tepeh on the Danube; and, although some ap- pear to be metamorphic from volcanic agency, they are no doubt of an early age; perhaps either Devonian or Carboniferous. The only place where rocks of a similar age appear on the shores of the Black Sea, in the Dobrutcha, is at Kara Irman, near Cape Media. At this spot, which is near the south-west corner of the Raselm Lagoon, and where the delta of the Danube commences, there are dark shales of considerable thickness, and much resembling the shales and schistose strata occurring on the flanks and base of the Balkan, near Cape Emeneh. The section (fig. 1, p. 206) of the coast-cliff, from Kara Irman towards Cape Media, is of much interest, from the contact of a lime- stone of Secondary age with these older shales ; both being overlaid by the superficial, reddish-brown, earthy marls of the Steppe, without any intermediate group. The dark shales and schists, a, of fully 500 or 600 feet in thick- ness, form a portion of the rocky shore at Kara Irman, at the angle of the coast, where a ridge of the Steppe projects into the Black Sea as a small promontory, and acts as a natural groyne to hold in check the alluvial deposits of the Danube. At this point there was formerly a scala, or landing-place, for communication with the vil- lages of the neighbourhood, and the ancient town of Istia seems also to have been near here. These dark shales dip to the northward, at an angle of 40°, the strike being 8S. 83° W.; and, although appearing along the coast for about a quarter of a mile, they are nowhere more than 3 or 4 feet above the sea, and are immediately overlaid by about 40 feet of the soft, reddish-brown, earthy marls of the superficial series of de- posits, e. I had no opportunity of examining them minutely in search of fossils. 10) The cliffs of white compact limestone, 6,, contain corals and marine shells ; they are only from 16 to 20 feet high. The beds lie nearly horizontally, and seem to have been originally deposited against the older shales; but they may have been thus brought in contact by a fault. | These limestones are shattered, and filled with small cavities, especially where the fossils are most abundant. A Rhynchonella seems to be the characteristic fossil. | The second mass of limestone, 6,, is a coast-cliff about one mile nearer Cape Media *; and the compact white limestone of which it is * The specimens from Cape Media, forwarded to the Society by the author, consist of yellowish, cream-coloured, and grey limestones (hard and crystalline) with Pectines, Terebratule, Rhynchonelle, a univalve, and Corals. Some hard, yellowish, and grey limestones, sent by Capt. Spratt from Lake Raselm, much resemble those of Cape Media, and contain remains of Ammonites 1857. | SPRATT—DOBRUTCHA. 205 composed, although identical in mineral character with the first mass, in contact with the shales, is less fossiliferous and more distinctly stratified. Both these masses are overlaid by about 2 feet of rubbly white marl (omitted in the Section), succeeded by the reddish-brown marls e,e, which are not more than 20 feet thick over the lime- stones ; but are fully 40 and 50 feet thick in the intermediate spaces. As none of the identified freshwater marls cap these limestones, but only such as are of a doubtful age and origin, possibly connected with a disturbed or changing condition in the later period of the freshwater series, these limestones must have stood as ridges, rocks, or islets, when the freshwater lake, which I believe once covered the area of the Black Sea and Archipelago together, existed, and of which the lower deposits south of Kustenjeh, and the upper at Baljik, 400 feet above it, give some positive indications, as also, I think, the freshwater limestones or marls of Odessa and Kertch. Between Cape Media and Kustenjeb is a freshwater lake, about 4 miles long and 2 broad. It is separated from the sea by a strip of sandhills, which extend between the extremities of two ridges of the Steppe, and terminate in a cliff at the south, towards Kustenjeh. The inner shores of the lake are for the most part chalky cliffs, or marly banks, that were, without doubt, the sea-margin at some early period; so that this freshwater lake has been formed out of a small arm of the sea, by means of the alluvial sand having been moved along the coast from the Danube (by the prevailing winds and cur- rents), and thus accumulated in nearly a direct line across the mouth of the bay. From the existing copious springs of fresh water on the shore of the bay, the enclosed arm of the sea, or salt lagoon, has become a freshwater lake. The bay was also originally a deep- water inlet of the Black Sea, since it has now a depth of 18 or 20 feet nearly all over the lake. The north-west shore of the lake is chiefly low banks of brown marl, belonging to the superficial series. But the south-west shore presents geological features of considerable interest, more particularly between the villages of Kanara and Pallas *. At about half a mile from the former village is a small islet covered by a grove of trees; but the islet is not more than 4 or 5 feet above the sea. Of this islet 2 or 3 feet is a rich soil, and the base a mass of inclined strata of compact cream-coloured limestone, much re- sembling that which I have noticed at Cape Media. (Ceratites >), Pectines, Terebratule, Rhynchonelle, Modiola, a small Echinoderm, fragments of Crinoidal stems, and Corals. A somewhat similar cream-coloured compact limestone, sent by Capt. Spratt from Cape Karabournou, Roumelia, con- tains fragments of Ostrea, Lima, Terebratula, Corals, a fragment of a Crustacean, and casts of univalves and bivalves. A softish buff-coloured laminated limestone from Cape Dolashma, Lake Raselm, cortains numerous small Jnocerami in layers, and branching fucoidal bodies.—Epir. * These localities are shown on the map illustrating Capt. Spratt’s ‘‘ Route between Kustenjé and the Danube,” published in the ‘ Journal of the Royal Geo- graphical Society,’ vol. xxvi.—Ebpir. P2 Fig. 1.—Section of the Eastern Coast of Cape Media. PROCEEDINGS OF THE GEOLOGICAL Society. [June 17, 7 REE SSS Kustenjeh. ——-- ———— ——————— ——— Fig. 3.—Section at Kustenjeh. (The rubbly and chalky marl, overlying J, 4, is omitted.) e, e. Reddish marls of the “‘ superficial series.”’ ———— —— = —— —— d c. Older Tertiary shelly limestone. d. Freshwater deposits (50 feet). e. Reddish marls of the Steppe (100 feet). Fig. 2.—Section of the South-west Coast of Kanara Lake, near Kustenjeh. e, e. Brownish marls of the “ superficial series.” 4), dj. Fossiliferous limestone of Secondary age. a. Old schists. _ ,. Limestone and shale of Secondary age. 05, 63, 64. Chalk and chalk-marl. c,c. Sandstone of Tertiary age. —— ——— Mi | i ‘it bi | | { | i WE PRED Vu _— te e d = 1857. | SPRATT— DOBRUTCHA. 207 A rocky point, which juts into the lake to the east of Kanara, seems also to be a part of the same limestone. The opposite section, fig. 2, will explain the disposition of the - formations :— A cream-coloured compact limestone, 6,, interstratified with light-grey shales, in layers from | to 3 feet thick, together attaining a thickness of 500 or 600 feet, occupies the point ; and at the ex- tremity the strata dip to the S.W. by S., or S.W., at an angle of 35°. Here they are more cry stalliné than at 200 or 300 yards within the point ; this indicates, perhaps, a proximate igneous rock not visible. The dip of the strata diminishes as they recede from the point towards the village of Kanara, where they seem to be in contact with, and overlaid by, white chalky marl, 6,; but whether passing into and conformable with it, I could not ascertain, on account of the superficial marls of the Steppe, e, covering the whole. Although I procured no fossils from the limestones, 6,, at Kanara Point or at the island, the beds seemed to be identical in mineralogical character with those at Cape Media, fig. 1 ; more par- ticularly as the chalk-marls overlie them in apparent continuity of succession. The chalk-marls* appear, by the fossils that I procured from them, to be either of the Cretaceous or Upper Jurassic age. About half a mile to the south-east of the village of Kanara rises a semicircular cliff of the chalk-marl, nearly 80 feet high (6,, in the section, fig. 2). The chalk-marl dips to the south-east or south- ward, at from 5° to 8°, and is capped by about 15 feet of yellowish- brown sandstone, c, with oolitic rock. This appears to be an early tertiary deposit, and corresponds with some oolitic strata that occur at the base of Kustenjeh Point (see ¢, fig. 3), as also with the oolitic strata of the Malakoff ridge at Sevastopol. . The deposit, c, capping the chalk, is unconformable, and is evi- dently of an early Tertiary age ft. This chalk-cliff must have been an elevated point in the fresh- water lake of the Tertiary period, since it is covered and flanked only by the superficial marls of the Steppe series (e in both the sec- tions). These also fill the valleys on either side-of the ridge. At about half a mile more to the south-east is another chalk-cliff, 6,, which extends along the coast for more than a mile, and beyond the village of Pallas. This cliff seems to be composed of an upper series of the Chalk, since the strata have the same dip as in the former section, and contain a large quantity of siliceous bands and nodules, though very few fossils. I could procure only a few frag- ments, as the whole series of strata composing this cliff are more indurated than in the chalk at Kanara. * Portions of a Ventriculite, together with ferruginous ramose concretions and pyritous balls, are in the specimens of this soft white calcareous rock, sent by the author. It contains also cretaceous Foraminifera.—Ep1r. Tt Specimens sent to the Society are—a hard oolitic white limestone with bivalves (Lucina ?) ; a cream-coloured compact crystalline limestone; and a hard yellowish limestone, full of casts of univalves and bivalves, chiefly two forms of fluted Cardium or Adacna.—EpIT. 208 PROCEEDINGS OF THE GEOLOGICAL Society. [June 17, This cliff is also capped by about 10 feet of rubbly oolitic sand- stone, ¢, like that at the cliff near Kanara, and containing similar fossils. If this, as I conjecture, be an Kocene bed, it is here a mere remnant of that group. The chalk-cliffs gradually decrease in elevation from the village of Kanara, and altogether disappear a little beyond Pallas, where the superficial red marls replace them, and form the sea-cliffs to Kus- tenjeh. This group of maris, of the superficial series, are well developed in the cliffs both to the north and south of Kustenjeh. To the north of it, the cliffs are more than 100 feet high, and entirely composed of these marls. Some of the strata are dark umber-brown, and contain nodules of soft chalk, also bands and crystals of gypsum ; but there are no gravels—no indication here of their having been deposited in waters under any violent movement. ‘To this the soft chalk-nodules are the only exception, showing probably an agitation or current, and appear to have been derived from the proximate chalk-deposits, before described. But I saw no heavy nodules of indurated chalk, or of chalk-flmt, such as would indicate any violent aqueous movement. These deposits, fillmg up the denuded hol- lows and valleys which existed on the surface of the Cretaceous and early Tertiary ridges, are destitute of fossils, and seem to be due to a rapid deposition from highly-charged waters. And this also seems to be indicated by the absence of such a uniform and constant series of strata as may be expected to occur in slowly-formed deposits. When I partially described the Kustenjeh marls*, I was not able to separate them into two distinct groups. But further researches more to the south have enabled me to discover that the probably freshwater deposits of the lower series, in which I procured a frag- ment of an Elephant’s tusk, and some casts of a Cyclas-like bivalve, do not pass into the overlying series of reddish-brown mars. My conjecture of the freshwater origin of the lower portion of the deposits to the south of Kustenjeh is confirmed by my discovering more terrestrial and probably freshwater-shells in them; and thus they are identified with the upper series of freshwater deposits, which I have noticed as covering a fragment of the early Tertiary at Baljik+, where they are more than 100 feet in thickness, and 500 feet above the sea. But at Kustenjeh they are only observed at the sea-level, and from 30 to 40 feet above it. I therefore take this opportunity of correcting my former section of the Kustenjeh deposits by the one given at p. 209, with fuller details. The lowest bed is about 5 feet of yellowish-white oolitic limestone, c, fig. 4, with marine fossils. This is apparently of the Eocene age, and much resembles the oolitic rocks near Varna{ and Sevastopol. The * Quart. Journ. Geol. Soc. vol. xiii. p. 78. + Loe. cit. p. 77. ~ In the opinion of M. Abich, For. Mem. G. 8., who has carefully examined the fossils from the neighbourhood of Varna, these deposits are of Miocene age.— Ep. Q. J. G.S. . 1857. | SPRATT—DOBRUTCHA. 209 pe the strata is apparently to the N.E., at an angle of 8° or 10°. In examining minutely the deposits forming the Point of Kus- tenjeh, I found that this rock terminates abruptly on the north and south sides of the promontory, as if by a fault ; and it is overlaid by deposits that seem to belong only to the red marls or superficial series, e, although the lower bed, immediately reposing on ¢, contains casts of a Cyrena? similar to what are found in the upper portion of the group d, fig. 3, where the beds and fossils indicate no such evi- dence of haying been aggregated by moving waters. Fig. 4.—Section of Kustenjeh Point. a TM | a i Tu i i ) = e,, Reddish marls. e,. Shelly sandstones, 7 feet thick. ec. Older Tertiary oolitic limestone, marine. On the older tertiary deposit, ¢, is a thinly stratified yellowish sandstone, e,, 7 feet thick, and composed almost entirely of frag- ments of shells and oolitic’particles. In it are bands and masses of casts of Cyrene? like those found in group d, figs. 3 & 5. This deposit, e,, from containing the oolitic grains and these bi- valves, seems to be composed of the debris of groups ¢ and d, under a sudden disturbance of the old lake, in which the rock ¢ formed per- haps an islet or shoal during its previous tranquil condition. The next bed, e,, is about 30 feet of red marl or clay, without any indication of fossils or foreign fragments, and is a small portion of the superficial marls, e, of the Steppe, which I shall have to refer to in describing more particularly the evidence of the separation between the marls d and e of fig. 3. This will perhaps be best done by giving a section (fig. 5) of a part of the cliff at about half a mile S.W. of Kustenjeh, where a fresh landslip or scaling showed me clearly the point of separation between the two series of marls, marked by the denudation of a por- tion of the lower group, as seen at a, and the subsequent filling up of the irregularities by the upper red marl series. This separation is difficult to identify where the upper series reposes upon a more indurated stratum of the freshwater series, as frequently occurs. 210 PROCEEDINGS OF THE GEOLOGICAL sociETy. [June 17, When both lie nearly horizontal, they appear to be conformable, as in the cliff about one mile south of Kustenjeh. Here I saw, in ascending order, Ist, 10 feet of a greenish-grey marl, with indurated nodules of marlstone, and sometimes chalky nodules, but not derived apparently from any foreign locality ; also crystals of gypsum, and casts of a Cyclas or Cyrena; 2nd, an indurated band, from 2 inches to 1 foot thick, filled with casts of a small Paludina; 3rd, 5 or 6 feet of grey marl, with bands of marlstone; 4th, 20 feet of greenish-grey marls, with broken layers of marlstone, forming slabs and nodules, © in which are found casts of a bivalve (Cylas?), also an occasional Fig. 5.—Section of part of the Cliff half a mile South-west of Kustenjeh. 3. Brown and reddish marls (continuing to the height of 70 feet above). 2. Dark-brown clay with chalky nodules. _— » Reddish-white light marl. 5. Greenish-grey marl with Helices. 4. Greenish-grey marls with Helix and Cyrenu? About 3. Grey marl and maristone. 30 feet. . Band of small Paludine. is] . Greenish marl, with nodules; Cyrena? Jif _ Heliz, similar to the one found in the freshwater deposits over Baljik* ; 5th, a more indurated stratum of the greenish-grey marls, from 2 to 3 feet thick, and replete with Helices. This is also some- times pisolitic, and its indurated character is evidently due to the ageregation of the fossils. The shells, probably, were not accumu- lated by any violent action of the waters from currents or drift, but lived at the bottom during a late period of the lake, when it seems to have been very shallow, and perhaps, in consequence, subject to stronger superficial currents, from local wmds and local torrents. Hence the associated land-shells and lacustrine shells were thus mingled together in accidental groups ; as no doubt must occur often at the bottom of shallow tideless waters proximate to land prolific with vegetation and land-shells. This condition must have existed on the old chalk-ridges that formerly bordered the lake not far from these * Quart. Journ. Geol. Soc. vol. xiii. p. 77. 1857.) SPRATT—DOBRUTCHA. 2 cliffs, as I have shown previously. Chalky downs are always highly favourable to the prolific development of land-shells, as is well known to all naturalists. And I digress for a moment to suggest that, in this view, we have an explanation also of the origin of the white marly character and great thickness of the Baljik freshwater deposits, as having been derived from the denudation of these great chalky ridges by the torrents of every season’s rain. Here also the land-shells (Helix) are as abundant in the upper series of the deposits as the bivalves and other freshwater shells that lived in the lake. Referring to the section, I have to add that the fossiliferous bands of the lower freshwater series thin out sometimes to a thick- ness of a few inches at distances of a few hundred yards on either side: such is the case towards Kustenjeh, where, being less indurated, they have been superficially denuded, as shown in fig. 5, a. At the locality where the last-described section was taken, how- ever, the greenish marls present a flat surface, upon which imme- diately succeed the reddish marls of the upper series, which I have before described as being stratified in thick beds of dark-brown, grey, or reddish marls ; they are nearly 100 feet thick in some parts. The upper marls are lighter and somewhat porous *. In closmg my remarks, I shall merely state that I have no doubt but that the continuity of the Kustenjeh freshwater deposits will be traced hereafter up to the elevated deposits of Baljik, as a con- tinuation of the bottom of the same lake. And I venture to suggest that they are also identical with those of Odessa and Kertch, neither of which, however, I have had an opportunity of examining. Their connexion is to my mind also certain with those of the shores of the Sea of Marmora, by the valley of Brujuk Tchekmijeh, where I some time since found freshwater fossils in its deposits, together with a band of lignite. Also the lignite and gravel-beds examined by Mr. H. Poole+ on the south side of the Sea of Marmora, near Brusa and Ismid, I believe to be of freshwater origin; and I connect them as indications of one great eastern freshwater lake that existed perhaps from the Miocene to a late Tertiary period. The actual limits of this lake westward as well as eastward have yet to be defined by - * The specimens from the “ Upper series of the Steppe deposits,’”’ sent to the Society, comprise—l. red marl; 2. soft, yellow, laminated, argillaceous sand- stone; 3. brownish, sandy, micaceous marl; 4. a brownish marl, like No. 3, but altered by atmospheric agency, perforated with minute irregular tubules (as is also No. 3), and containing small, soft, calcareous concretions; 5. like No. 4, but less calcareous, and redder ; also buff- and salmon-coloured calcareous concre- tions, and soft white marl. The specimens of the “ Freshwater series” comprise—1. shelly, cream-coloured, compact limestone, full of casts of Helices and a Bulimus; 2. hard, grey, shelly limestone (weathered), concretionary or oolitic, and crystalline, full of casts of bivalves (Cyrena ?), and containing a few casts of small univalves ; 3. marly lime- stone, full of casts of Cyrena ?, passing into a hard, grey crystalline limestone, with similar casts, and resembling No. 2; 4. greyish limestone, full of casts of Cyrena ?, interior of the casts sometimes oolitic; 5. grey limestone, full of hollow black moulds of a small Paludina ; 6. green clay, with a portion of an elephant’s tusk.—EpirT. . + Quart. Journ. Geol. Soc. vol. xii. p. 1, &e. 212 PROCEEDINGS OF THE GEOLOGICAL society. [June 17, determining the precise age of the great volcanic centres, that, from Ararat to Lemnos, and Santorin to Vesuvius, have from time to time uplifted or submerged parts of its expansive bed. In merely touching upon this view, [am induced to recall to mind the other isolated fragments of freshwater deposits that occur in Rhodes, Crete, Cerigo, and in the western basin of the Mediter- ranean, of Provence, Lombardy, Florence, Minorca, &c., as reviving an old idea of a chain of lakes having existed in the Mediterranean basin during this period, or rather during a portion of it. In the sections here given it will be seen, that the superficial red earthy marls of the Steppe-series cover rocks of all ages, and that the freshwater marls, d, are often wanting. The probable explanation is, if the former were deposited in freshwater also, that the old land surrounding the lake became suddenly submerged at the commence- ment of this red mar] series,—or that the level of the lake became suddenly raised by the escape of water from some more extensive and more elevated basin,—or that the waters were suddenly raised, having been pent up within more limited bounds, on account of the rising of some great mass of continent, such as a large part of Asia Minor, from out of the great eastern freshwater basin which I suppose to have existed. 12. On the FREsHwaterR Deposits of the LEVANT. By T. Spratt, Captain R.N., F.R.S., F.G.S. Tue brief account recently published* of the extensive freshwater deposits which exist on the western shores of the Grecian Archi- pelago calls for a notice of those within my knowledge on the eastern shores. . The freshwater tertiaries of Smyrna and Sciot+ have been traced by me as fragments along the eastern and southern coasts of Mity- lene, as well as on the coasts opposite,—the detached and disturbed condition of these deposits being due to extensive outbursts of igneous rocks that form large districts within this island and on the main land opposite to it. For instance, the Moskonisi and Aivali districts, the Assos Range to Cape Baba, Touzla, and Alexandria-Troas, and, in Mitylene, the north-eastern part of the island, mcluding Mount Lepethimus, as well as the entire peninsula west of Port Kelloni, are composed of volcanic rocks. Besides these there are several lesser protrusions of trap in numerous parts of the intermediate districts. The vicinity of Mitylene presents an interesting association of the trap and the freshwater deposits, particularly to the south, as shown in the following section, fig. 1. At Cape Vourkas we meet with the trap and tertiary strata in proximity, particularly on the east short of Port Kelloni, while the white freshwater marls are nearly vertical, and contain several speci- mens of a small Helix. * Quart. Journ. Geol. Soc. vol. xiii. p. 177. + Described in the Society’s Quarterly Journal, vol. i. p. 156. © 213 SPRATT—FRESHWATER TERTIARIES, LEVANT. 1857.] “A'S "BLOVIIG JAY “KIOISVUO J ULTIOIG vou ‘s]styos OUT[[eISA1O puB [eOAGA OY} Ur ‘azTUBIS Jo SUIDA *yf ‘oyUeIs O1ytAYdasod oaIsnaquT *f Vf ‘N 07 ,0¢ dtp {u9013 pue UMoOAG-yAep ‘saTVYS SNHOddROILA po}LOJUOD ‘a ‘oUOJSOWIT ‘p ‘sareys onfq pue Aots-yreq 9 ‘9 “WN 07 OG dtp ‘soyeys woat3-yaeq ‘g ‘Aauienb pouodo-A[mou @ UL UMOYS ‘9UOJSOUL] OUTT[LISALO VIL AA ‘yO “O[VYS YL poyt}esjs.tozUr ‘o[qavu poulon “Dv \); LANA ch ae % Y\ ns JO o8xIILA *‘DOMIO[C) “MN JO aBeqTIA “yBuy 4295 000% jo spaemdn ‘spit [e1zUID (‘812d 20g) ‘nuomunpy fo punjsy ay? fo ysnog 48944 a4) Hu0jw uorpvagI—'f “SLT *499F DOT ynoqe jo yy Srey & Surypovoa ‘ode Arepuooag jo ‘souo}sow'y “f ‘sqivd oUI0s UL SNOLOsITISSO} A] YS ‘QUOyspULS pu ‘oNO4S[TeUT ‘spreUA yoRly pue ‘Ko13 ‘UMmoOAG ‘OITY AA ‘YP ¢ DUaUAD B Jo s}svd Jo [INF ‘au04s -OUNT] ORAS Vy AA ‘9 *sudJIg pue s19}sKQ Surureyzuoo ‘favor ApuBs a} AA “G “SHOAIJITISSOF ‘OLY} 4997 OP ‘OUOJSIUUI] SHODDVUAE OILY AA “2 ‘sopauay fo punpsy ay7 f0 u01I0g9—'Z *B1yy *syoor snoousy “ff ‘souojsoutry *a ‘RIVLIS UMOIG PUL OUT AA ‘P ‘BIVAYS poPeBorIVa pUe II AA ‘9 ‘"[AVUL PUL DUOJSOUNTT SNODIVUDI YSIMOT[PA “G ‘[AVUI pue spues AdIDH ‘v 'N “uot SHUI ‘s ‘auajphgipy fo punjpsy ayz fo zt0d vo fo uo1sag9—' [ “By 214 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, The Island of Tenedos is still more interesting and instructive in respect to the relative position of the freshwater deposits, and for their greater development, as seen in fig. 2, p. 213. Here the freshwater deposits are found to be capped by about 40 feet of a white arenaceous limestone, containing marine shells of the present sea, both deposits lying nearly horizontal, and apparently conformable. The exact place of separation of these two groups is not easy to be detected; and it was some time before I discovered positive proof of the freshwater origin of the lower group of strata, ¢ and d in the section. Three-fourths of the island is comprised of these horizontal beds of freshwater and marine tertiaries, which together are fully 100 feet thick. The other fourth consists of a conical peak of trachyte (Mount Elias), rising like a dome over the extreme north-east cape of the island, and throwing off from its southern flanks ridges of secondary limestones and shales, somewhat frizzled by the contact ; these are succeeded or overlaid by horizontal strata of the Tertiary series, as shown in fig. 2. The fossils which I procured from the bed d areasmall Paludina, Planorbis, Neritina, Cyrena (?), Melanopsis, and a ribbed bivalve (Cardium) similar to the one found in the Dardanelles deposits near Meitos and over Nagara Point. The deposit a contains shells similar to those of the present sea; and, although they are upwards of 100 feet above the sea-level, they are apparently of a late Tertiary age (older or newer Pliocene), like the marine deposits which repose against the freshwater beds at the south-east extremity of the island of Cos. To the north of Cape Baba, near the River Touzla, there are some coast-cliffs of this late marine tertiary, from 30 to 40 feet high, in which the beds seem to repose on the adjacent igneous rocks. The latter extend northward to the mountains at the back of Alexandria- Troas, where a granitic trap predominates, and from whence columns, in early days, and stone-shot for the guns of the Dardanelles, in later times, have been quarried. These quarries occur near the village of Chimali. More to the northward, the blue semi-crystalline limestone and shales of the secondary group of rocks replace the volcanic rocks ; and then succeed extensive districts of horizontal strata of the fresh- water and marine tertiary deposits, as far as the Dardanelles, Sea of Marmora, and Constantinople, with an occasional protrusion of the trap here and here in the northern part of the Troad. Connected with these jets of trap, between the Gulf of Smyrna and the Troad, outlying from the great centres of eruption, is an in- teresting point which I observed many years ago when examining and surveying the topography of the plain of Troy, to illustrate the Homeric history, and when I was accompanied by my learned friend Dr. Forchhammer of Kiel, who wrote an account of our trip for the ‘Geological Journal.’ Several masses of basaltic rocks peep through the tertiary strata forming the hills surrounding the plain of Troy ; 1857. | SPRATT—FRESHWATER TERTIARIES, LEVANT. 915 but one of particular interest occurs at the site of Troy, where a ridge of volcanic rocks extends from the base of the Pergamus to the north-east of the village of Bounarbashi. The limestone-ridge, forming the Pergamus of Troy above it, and extending also to the ridges west of the village, indicates the effect of this voleanic outburst in the fissured condition of some portion of the mountain. But I refer particularly to the fact that the most copious and the most western of the springs which form the Scamander issues through two crevices or rents in a mass of red tufaceous rock that seems to be derived from and connected with these volcanic ejections. These two springs are the most copious of the whole at Bounar- bashi, and together are capable of turning a water-mill after being collected in a basin at the mouth of the fissures. These sources, coming through an apparent volcanic vent or rent, suggest most strongly that the water issuing from them in the Homeric time might then have been warmer by a connexion with the subterranean heat, although all the springs showed only 63° by the thermometer which I used in 1838. How beautifully, then, does Homer’s description, as rendered by Pope, apply to the long-disputed question of the hot and cold springs of the Scamander !— “This, hot, through scorching clefts is seen to rise,’ &c. Iliad, xxii. Curious and interesting, then, is this explanation of a long-doubted point of the Homeric description ; and I introduce it here, not being aware that it has been noticed by any traveller since my reflections on it im 1838, as a point of geological interest in connexion with the igneous eruption above alluded to. As the presence or absence of the above-mentioned great igneous centres have a marked influence upon the features of the country, I shall here notice that, excepting some trap-rocks, accompanied by slight local disturbances, as at Kefez Point, near the Arenkeui hos- pital and Chanak castle, none other occurs between the Artake Islands, in the Sea of Marmora, and Tenedos. This district presents a great development of freshwater marls and limestones, nearly horizontal, and extending from the Troad to Lampsaki on the south side of the Dardanelles, and from Cape Hellas nearly to Rodosto on the north side, and from Rodosto to Constantinople, on the northern shore of the Sea of Marmora. The strait of the Dardanelles entirely divides this great field of freshwater deposits, that have been apparently lifted in mass almost vertically, but divided asunder by the strait, as if separated by a great chasm ; for steep cliffs or banks terminate the ridges that line both shores of the strait, in some cases displaying these deposits in a series of horizontal strata of grey and green marls, brown sands and sandstone, fully 700 or 800 feet thick. As I never met with any marine fossils above the freshwater deposits of the Dardanelles, it appears that they were elevated above the newer Pliocene sea-level. 216 PROCEEDINGS OF THE GEOLOGICAL SociETy. [June 17, The localities* at which I have found freshwater fossils, in proof of my arguments, are as follows :—Cape Hellas, where the marls and sandstones contain Cyrena or Cyclas ; under Yenisher, on the Asiatic side, I have found cast of Uniones and Cyrene? in the neigh- bourhood of Arenkeui+; over Nagara Point, Unio and a ribbed bi- valve (Cardium) similar to that in Tenedos, with Paludina and Planorbis ; the same at Meitos with fossil leaves and other plant- remains. Also Unio and a Melanopsis similar to that in Tenedos are to be obtained in great abundance in a bed of sandy marl over Kiled Bahar, the European castle of the Dardanelles. [In a letter to the Assistant Secretary, dated June 12, 1857, Capt. Spratt states :— “In a walk up to the village of Arenkeui, over the site of our hospital, I found the deposits to be precisely similar to those on the north side of the Dardanelles, and to consist of thick-bedded yellowish-brown sands and sandy marls, with an occasional stratum of sandstone. Towards the top, they pass into peaty marls, marl- stone, and fine sands, brown, red, or cream-coloured. The fossils occur at different elevations, and comprise both the Cyrena? and Melanopsis which occur at Tenedos and Baljik. “The fossil teeth, found by Mr. Calvert, were taken from the lower part of the group of sandy marl immediately below the village.” | The following is a section across the Dardanelles, from the hill over * The specimens sent by Capt. Spratt from the Dardanelles and Sea of Mar- mora comprise—1. Blue sandy clay with Cordule (?), Cape Hellas, entrance of Dar- danelles; 2. yellowish earthy limestone, mainly composed of fine shell-grit, with plant-remains (like a portion of a leaf-scarred trunk), and Unio and Paludina, . from the European side of the Dardanelles; 3. hard, grey, earthy limestone, full of Cypride, Paludina, Unio, and fluted Cardiwm (Adacna), from the European side of the Dardanelles; 4. soft yellowish limestone, with 4dacna,—hard fer- ruginous, laminated sandstone, with Adaena, Cyrena (?), Unio, Melanopsis, oper- cula of small Paludine, and Cypride,—and soft buff shell-grit with Cypride, from Nagara Point; 5. buff-coloured shell-grit, with harder crystalline seams, containing Melania and Nerita, from Genokora Point, entrance to the Sea of Marmora; 6. white crystalline limestone with Cyrena, and subcrystalline, porous, and marly white limestone, containing casts of small bivalves and Melanopsis, and shells of Neritina retaining colour, from near Cape Stephano, Sea of Mar- mora; 7. from Ereke, Sea of Marmora, olive-green, irregularly laminated, mica- ceous sandstone, with dicotyledonous leaves and fragments of plants; 8. from Marmora Island, white quartzite (rounded fragments), whitish-grey syenite (waterworn fragments), and two varieties of mica-schist ; 9. from Kutali, Sea of Marmora, pinkish-grey syenite. —Epir. + Similar fossils, with numerous fossil bones, have been obtained by our Con- sul, Mr. Calvert; but I have not seen them, andI am informed that the Medical Staff and the Architect of the Arenkeui hospital have taken to England some of these Mammalian remains.-—T. S. Mr. Calvert, the brother of the Consul, has obliged the Assistant Secretary with the following particulars relating to these fossil bones. The sides of a ravine or valley between Arenkeui and where the Hospital was, and running down to the sea, are formed of horizontal beds of sand and sandstone ; in the former a portion of an elephantine jaw, with two teeth in place, was found; and on the higher ground, about 3 miles from the edge of the valley, some fragments of fossil ivory were found near the surface. The bottom of the valley appeared to be formed of sandstone débris, covering blue clay and red marl.—Epir. 1857.| | SPRATT—FRESHWATER TERTIARIES, LEVANT. 217 Meitos to Nagara Point, through an isolated tabular mass of con- glomerate, which here caps the freshwater marls at an elevation of about 100 feet above the sea, but contains no fossils. Fig. 3.—Section across the Dardanelles. W. E. Hill over Cham Tabia, near Meitos. Plain of Fort and Hill Abydos. over Nagara Point. Dardanelles. a. A conglomerate of rounded pebbles of limestones, schists, and shales, similar to rocks which occur near Lampsaki. b. Marls and sands, containing freshwater fossils. (500 feet thick on the west side of the Dardanelles.) This conglomerate, a, contains no fossils like those of the mass of similar conglomerate, 70 or 80 feet thick, which forms the Promon- tory of Gallipoli; the latter I have before noticed* as containing fragments of a large Dreissena and a Cardium, as well as being capped by a thin stratum of sandy marl, in which these fossils occur more abundantly, both entire and broken. The south shore of the entrance to the Sea of Marmora, from Lampsaki to Cape Karabournou, opposite Kutali Island, and around to the mouth of the Granicus, is composed chiefly of steep ridges of older rocks (limestones and shales), with volcanic protrusions, and detached fragments of the Tertiary deposits. The north shore from Gallipoli is composed of marls and sands, which seem to be identical with the freshwater series; and at Ganakhora, opposite to Marmora Island, about 50 feet of the marly deposits are capped by a bed of conglomerate, formed of rolled pebbles, with broken shells of Dretssena and Cardium, as at Gallipoli. In a hasty visit to Erekli and Scliori, to determine the proper sites for lighthouses on that shore, I observed the same marly and sandy deposits ; and amongst the ruins at the former locality, I found that some of the ancient buildings had been built of a concreted mass of bivalves like large Dreissene; I could not learn from whence it came, but I think Rodosto. I could find no shells in the sandstones and marls at Scliori to in- dicate positively its freshwater origin; but I procured some fossil leaves, which were abundant near the upper part of the cliff to the east of the town. All along this shore, the Tertiary deposits have frequently a dip from 5° to 15°, but with no constant direction. At Bujuk Tchekmejeh the marly cliffs contain a bed of lignite, with casts of freshwater shells in the associated marls. Cape Stephano is composed of white and yellow marls, about 25 feet thick, in some parts chalky and calcareous, with irregular nodules and concretions. I was doubtful whether this was not an early and lower member of * Quart. Journ. Geol. Soc. vol. xiii. p. 82. 218 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17, the freshwater series; but, as the quarries of Makri Keui not far distant are in a white lacustrine limestone, as Mr. Strickland long ago pointed out, I am inclined to consider the Stephano marls as freshwater also, since I have found no evidence of any marine ter- tiary in the shores of the Sea of Marmora. In some specimens which I procured from the quarries of Makri Keui are casts of a Melania, apparently resembling the one I procured from the neighbourhood of Vourla in the Gulf of Smyrna, figured in the ‘ Geological Journal,’ vol. 1, p. Lia, The above evidences of the freshwater origin of the deposits which line the north shore of the Sea of Marmora seem to justify my view of connecting the basin of the Sea of Marmora and the Archipelago, as having been a part of one great lake, which probably covered a great portion of the central part of Asia Minor, as shown by Hamilton and Tchihatcheff, penetrating by the valley of the Hermes and the other valleys separating the older chains and ranges, as Xanthus on the south, the Halys on the north, and the Hermes on the west. The lignite-beds, briefly noticed by Mr. Poole*, in the Nikomedian and Brusa valleys, are, I think, a portion of the same lacustrine series, which seems to represent a long portion of the middle and later Tertiary periods; although the relative age is difficult to determine precisely, on account of the great permanency of genera and species of the air-breathing Mollusca peculiar to the freshwater fauna. As the two basins of the Archipelago have each their central, but extinct, volcanos, or foci of eruption, in Santorin and Lemnos, so the Sea of Marmora has its focus in Pacha Liman and the Kutali Islands, which both seem to have been volcanos, from being entirely composed of granitic trap, and presenting a crater-like form. It is also an in- teresting fact, that, as there is very deep water in the neighbourhood of these sudden uplifts of igneous rocks, or abrupt uprisings of the bottom (as also occurs near Micero and Methana, two other evident volcanos of no very early date), so there is in the centre of the Sea of Marmora a sudden depth of 300 and 400 fathoms (representing, perhaps, a downcast proportionate to some neighbouring great uplift of the strata) ; and Marmora Island in its south-western half shows a large mass of granitic and porphyritic trap, associated with crystal- line limestones and micaceous shales and schists that resemble rocks of the earliest age. The section, fig. 4, p. 213, taken along the coast, and touching at several spots, tends to confirm these views. The marble-quarries of Marmora are celebrated; and I found them as extensive as the Pentelic Quarries of Attica, with the marble, in some parts, quite as white, pure, and crystalline as the Parian, but generally more resembling the cippoline of Carysto. As this condition occurs only when a volcanic dyke of the por- phyritic trap comes in proximity with the limestone, as seen in the section, it seems to show that these rocks owe the oldness of their aspect to their metamorphic condition ; and I am inclined to think that the eruption of igneous matter in contact with them may be of * Quart. Journ. Geol. Soc. vol. xii. p. 1. 1857.| HULL—TRIAS AND PERMIAN. 219 as late a period as that of Lemnos and the other volcanic centres which have torn up the bed of the lacustrine basin, because I observed the summit of one of the highest ridges of Marmora to be capped by horizontal beds of what appeared through the glass to be red and brown marls and gravels. These fragmentary remarks on the Dardanelles and Sea of Mar- mora, made for the most part during the commencement of the late war, although incomplete, will serve to call the attention of geologists to the interesting field of inquiry as to the boundaries and age of this great Oriental (if not also, in part, Mediterranean) lake or chain of lakes, as (it seems to me) indicated by detached freshwater deposits along the ancient margins. NovEeMBER 4, 1857. Robert White, Esq., West Cowes, was elected a Fellow. The following communications were read :— 1: On the Triassic and PERMIAN Rocks of the ODENWALD, in the Vicinity of HEIDELBERG, and the CoRRESPONDING ForMa- TIONS in CENTRAL ENGLAND. By Epwarp Huw 1, Esq., A.B., F.G.S. Tue resemblances and general relations of the Trias and Permian formations of the Thuringerwald and Hartz, with their representa- tives in England, have already been pointed out in the joint memoir of Sir R. I. Murchison and Professor Morris*. The present com- munication refers to a neighbouring range of hills, destitute, it is true, of that fine assemblage of paleeozoic rocks below the Permian, which have been shown to abound in the Hartz and Thiringerwald, but, in the case of the more recent formations, presenting many points of analogy with their contemporaries, both in the regions re- ferred to, and in Central England. It has been shown by Professors Sedgwick and King, as also by the authors of the memoir on the Hartz, that the Permian groups of Germany and this country can be strictly contemporanized, stra- tum for stratum. In visiting the Odenwald, it was partly my object to ascertain whether a similar parallelism might be observed in the case of the Trias. In doing so, however, occasion was taker to examine the Permian formation, which, though only sparingly repre- sented in the Odenwald, presents those peculiar lithological characters which appear to identify it, not only with formations in the Thirin- gerwald and Hartz, but also with the trappoid breccias of Worces- tershire. Since the establishment of three well-defined subformations in the Bunter Sandstone of England, a notice of which I had the honour of laying before the Geological Section of the British Asso- * Quart. Journ. Geol. Soe. vol. xi. VOL. XIV.—PART I. Q 220 PROCEEDINGS OF THE GEOLOGICAL society. [Noyv. 4, ciation in 1854, and which have been adopted by the Geological A Survey of Great Britain, I have felt desirous of ascertaining whether these subdivisions are represented in Germany. As far, however, as the present examination extends, there appear to be no grounds for subdividing the Bunter of the Odenwald. If, in England, this formation presents three successive stages, correspond- ing to the same number of periods in its history,—on the other hand, in this part of Germany, if we are to judge by uniformity of mineral character, there have been no cor- responding periods *. The Range of the Odenwald | forms a barrier to the valley of the . Rhine in a north and south direc- tion. It is traversed by the deep gorge of the Neckar, along whose banks good sections of the Red Sandstone of the Odenwald are ex- posed to view, especially at Neckar- stemer and Eberbach. Near the mouth of the gorge stand the castle and town of Heidelberg, on a boss of granite,—one of those isolated masses which frequently protrude at the northern extremity of the Odenwald, and in greater foree mm the neighbourhood of Freiburg. This granite consists of several varieties, considered by Sir C. Lyell+ as corresponding to suc- | cessive periods of protrusion ; but of its age, it can only be asserted that it is earlier than the Permian, and later than the Silurian epochs, as in the former case fragments of it are found in the brecciasof the Brook. Neckar. Heidelberg River Castle. Kénigstuhl. Granite surmounted by Permian Breccia and Bunter Sandstone. Distance about 34 miles. Ochsenbach. Section across the Kénigstuhl, near Heidelberg. Bunter. ’ Brook. Leinbach. Muschelkalk . * Since the above was written, the author has been informed by Sir R. Mur- | chison, that the German geologists have lately established a threefold division of | the Bunter in other parts of Germany. + Elementary Geology, 5th edit. River. Thairnbach. Keuper. p- 573. 1857.] HULL—TRIAS AND PERMIAN. 221 Roth-todt-liegendes, and in the latter, according to the hypothesis of Sir R. Murchison, the Freiburg gneiss is a Silurian slate, altered by eruptive granite of probably the same date with that of Heidelberg*. In the Odenwald this granite forms the basis upon which the superstructure of the Permian and Triassic formations has been raised. The geology of this Range has been illustrated by a map, accom- panied by a memoir, by Dr. von Leonhard, of Heidelberg+, who kindly accompanied me to some of the best sections in the neighbourhood, and to whose work I beg to refer those who wish to become well acquainted with the geology of the Odenwald and Schwarzwald, as the description here given must necessarily be brief. PERMIAN. The Roth-todt-liegendes of the Odenwald is finely exhibited in a road-cutting leading up the flank of the hill from the village of Handschucheim. A section of nearly 200 feet may be measured, and the upper surface is deeply covered by Loess, which rises on the flanks of these hills about 300 feet above the Rhine. The descrip- tion which Murchison and Morris have given of this rock in the Hartz, will apply equally here, and we might go farther and affirm that the same description would apply to the Permian trappoid brec- cias of Worcestershire. In the Odenwald this formation consists of unconsolidated breccia in a bright-red marly matrix, presenting only rude traces of bedding. The fragments are of porphyry and granite, the former in excess ; and the parent-masses are in immediate con- tact with strata to which they have supplied materials. At Raitbach and Sackingen, it has the appearance of a drift swept from off the Schwartzwald. At Baden, it is sometimes a coarse, sometimes a fine, breccia of granite, porphyry, clayslate, and gneiss, cemented by red marl. As in Worcestershire, the breccias of the Roth-todt- hiegendes may be regarded as a drift{ derived from the destruction of more ancient sub-aérial rocks, consisting of eruptive porphyries in the Odenwald and Germany generally, with which they appear - intimately associated. The resemblance of these beds to the trappoid breccias of Wor- cestershire cannot fail to have struck an observer acquainted with the formations of both countries. The resemblance is perfect, if we except the difference in the composition of the fragments, consequent upon the variations in the rock-masses from which they have been derived. The trappoid breccias of the Enville and Lickey Hills do not, however, form the basement-beds of the English Permian system, as similar breccias do in the Odenwald. In the former districts they are underlaid by several hundred feet of red sandstones and marls, with calcareous bands. For these beds we shall probably find repre- sentatives in strata described by Murchison and Morris, as occurring immediately over the coal-strata of the Thiringerwald, and below * ‘Siluria,’ p: 361. + Geognostische Skizze von Baden, 1846. t Of glacial formation according to Professor Ramsay ; Quart. Journ. Geol. Soe. ~vol. xi. p. 185. QZ 222 PROCEEDINGS OF THE GEOLOGICAL society. [Nov. 4, the breccias and conglomerates which form the grand mass of the Permian rocks in that region. The mineral characters bear out the analogy. They are described as “ argillaceous and thick-bedded sandstones, of a dark-red brick-colour,” a description which might be properly applied to what are here considered their representatives in England. Hence we may infer, that before the introduction of those littoral conditions of land and sea, accompanied by the outburst of volcanic. forces, which resulted in the production of the trappoid breccias of Germany, and, as maintained by Professor Ramsay, accompanied by glacial agencies in Britain, there appears to have been an introductory stage, in which deeper seas and more tranquil modes of deposition prevailed. In Worcestershire these basement-beds of purple sandstones and marls attain a thickness of 400 feet. They repose unconformably on the coal-measures near Bridgnorth, Enville, and Hales Owen, and are succeeded by the zone of the trappoid breccias and calcareous conglomerates, so prominently exhibited in the Clent, Lickey, and Enville Hills *. So far, the analogy in the order of succession of the Permian beds in both countries holds good. : Zechstein.—This formation is very sparingly represented at Hei- delberg, and is generally altogether absent. It consists of a band of yellow magnesian limestone, with imperfect fossils. As the mag- nesian limestone of the North of England is universally admitted to be the representative of the Zechstein, it will be unnecessary to dwell longer upon it here. TRIAS. Bunter Sandstein.—The sandstone of the Odenwald has given rise to considerable controversy regarding its age, doubts having been entertained whether it might not be referable to the “ Lower Bunter,” or ‘ Bunter Schiefer,”’: of the German Geologists, a forma- tion which Sir R. Murchison has truly shown to be of Permian age. An examination of this sandstone from its base at Heidelberg for miles along the valley of the Neckar, up to the point where it is overlaid by the Muschelkalk, leads me to the conclusion that the whole weight of evidence is in favour of its Triassic age ; and in this opinion I am borne out by the authority of Dr. von Leonhard, who has mapped and described it as such in his memoir on the Geology of Badent. At the Kaiserstuhl, which rises behind the town and castle of Heidelberg to a height of about 1300 feet above the Neckar, and 1723 feet above the sea, the sandstone attains a thickness of 1400 or 1500 feet. Throughout the Odenwald it is but very slightly inclined from the horizon, and gradually descends towards the boun- dary of the Muschelkalk at an inclination of 4 or 5 degrees. * See Maps of the Geological Survey of Great Britain, Nos. 61, S.E., and 54, N.W. + The Sandstone of Heidelberg is also marked as Trias in von Becker’s “ Geognostische Uebersichtskarte von dem Grossherzogthum Hessen,” and in Sir R. I. Murchison and Prof. Nicol’s Geological Map of Europe, 1856. 1857. | HULL—TRIAS AND PERMIAN. 223 In composition, the sandstone strongly resembles the conglomerate- beds of the Bunter in Lancashire and Cheshire, the difference being principally in the less abundance of quartz-pebbles in the case of the Heidelberg beds. The colour is bright red, and occasional partings of marl occur in the planes of bedding. Rounded quartz-pebbles, similar to those of the English quartzose conglomerates, occur spa- ringly ; and veins of brown iron-ore have been found,—a remark- able specimen being in Dr. von Leonhard’s collection. Several quarries have been opened at Heidelberg, Neckar-steiner, and Nussloch ; and the stone has been used with good architectural effect in the construction of Heidelberg Castle, and other public buildings of the country *. The composition of the whole formation is almost uniform throughout; and in this neighbourhood there is no part thereof which can be referred to the “ Lower Bunter Sand- stein,” or ‘‘ Bunter Schiefer,”’ as the beds immediately under the Muschelkalk are similar in all respects to those which rest upon the Zechstein and Roth-todt-liegendes. The Bunter is finely exhibited along the gorge of the Neckar, and im quarries in the neighbourhood of Heidelberg and Nussloch, near its junction with the Muschelkalk. Throughout its depth the com- position is uniform, affording no changes in mineral structure upon which to found sub-formations. In England, on the other hand, in Salop, Cheshire, and Lan- cashire, where this formation is most fully developed, we find three sub-formations preserving well-defined boundary-lines, and, from their differences of mineral character, producing landscape-features eharacteristic of each sub-formation. For these I proposed the names Upper Variegated Sandstone, Conglomerate-beds, and Lower Variegated Sandstone ; the middle member of the series separating the other two, which resemble each other strongly in mineral charactert. _ Now, it is to this middle sub-formation, or the ‘‘Conglomerate- beds” as they oceur in Western England, that the Bunter of the Odenwald bears the most resemblance: hand-specimens from the two localities could scarcely be referred with certainty to their ori- ginal beds; the only difference between them being the greater abundance of quartzose pebbles in the English sandstone. Guided, then, by mineral resemblance, we might infer that the Bunter Sandstein of England is more complete than in this part of Germany ; and that, of the three stages representing three epochs in the history of that formation in the one country, only the second of these was represented in the other. Considering, however, that the sandstone of the Odenwald attains a thickness which the three subdivisions m England never exceed, and masmuch’‘as the strata of both countries were certainly discon- nected at the period of their deposition, the evidence is not sufficient to warrant such an hypothesis; and I feel inclined to consider the formation in both countries as strictly contemporaneous. * The author cannot assent to the wish expressed by a celebrated poet,—that the sandstone of this fine old ruin were “ grey, and not red.’””—See ‘ Hyperion.’ + For descriptions of these sub-formations, see Rep. Brit. Assoc. 1854. 224 PROCEEDINGS OF THE GEOLOGICAL society. [Nov. 4, For these reasons, I have placed the three English sub-divisions so as to represent the whole mass of the Heidelberg sandstone in the annexed Tabular View. Muschelkalk.—This formation being unfortunately absent in Eng- land, I shall not dwell upon it here, referring the reader to Dr. von Leonhard’s work. It folds in undulating layers around the lower flanks of the Oden- wald, and is traversed by the Neckar near Mosbach. It consists of — thin- bedded bluish limestones with partings. It is only locally fos- siliferous, containing, amongst the more common species, the follow- ing :— Avicula socialis, Bronn; Ceratites nodosus, De Haan; Tere- bratula vulgaris, Brongn.; Encrinites lilizformis, Schloth. Hematite is extensively worked near Wiesbach. As this formation has no representative in England, it will be sufficient to state that its proper position, were it present, would be immediately under the Waterstones or Lower Keuper Sandstone.— (See Tabular View.) Keuper.—A true parallelism may be traced in the order of succes- sion of the beds of this formation in England and around the flanks of the Odenwald, and is confirmatory of the conclusion at which, with Professor Ramsay and Mr. Howell, I had long since arrived, that the strata of sandstones and marls, with a base frequently brecciated and calcareous, and which are known in the Midland Counties of England as ‘‘ Waterstones,” are to be referred to the ** Keuper formation.” In the Odenwald we find the representatives of these beds, com-. posed of brown and grey grits, with shales, altogether reaching about 100 feet in thickness. In one place, near Wiesbach, a remarkable bed of calcareous breccia occurs, containing fragments of granite, porphyry, and, what is more remarkable, of Bunter Sandstein. A specimen containing this fragment has been shown me by Dr. von Leonhard. These beds undoubtedly represent our ‘“‘ Waterstones,’ which may therefore be correctly termed ‘‘ Lower Keuper Sandstone.” The occurrence of this breccia in a position corresponding so closely with that of the breccias which in Worcestershire, Staffordshire, and Cheshire introduce the Keuper formation is interesting, as affording evidence of littoral conditions in both countries at the commencement of the Keuper period. These particular pebbles in the Keuper of Wiesbach, derived from the older rocks of the Odenwald, including the Bunter Sandstein, go far, I conceive, to prove unconformity to some extent between the two formations, arising from disturbances, accompanied by denudation, at the close of the Muschelkalk period. Similarly, it may be stated, that in some parts of Central England there are indications of unconformity between the Bunter and Keuper. I particularly refer to the neighbourhood of Ashby-de-la-Zouch, and of the Warwickshire Coal-field. In these districts there is an appa- rent independence or want of connexion between these formations ; the conglomerates of the Bunter appearing and disappearing suddenly without any reference to the position of the Waterstones. 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L eereccccccss soles poyesorie A ‘l ‘satqt]200°T "SUOISTATPQNS ‘SO1s1[200°T *SUOISTATPQNS *SUOTJVUIIOT ‘dNVIONG Ae ‘hunumiay pun punpbug fo syooy unuiag pun 208SDUl J ay) f9 Naiy LnINQD], “ANVWUGD 226 PROCEEDINGS OF THE GEOLOGICAL SociETy. | Nov. 4, filled up in Germany by the highly eventful period of the Muschel- kalk, analogy would lead us to infer the occurrence of physical changes of level sufficient to produce slight local unconformity. These Lower Keuper Sandstones are succeeded by a series of red shales and marls with gypsum, which compose the vine-clad banks around the villages of Rotherberg and Rauenberg, in thickness about 150 feet. 'To these succeed the Upper Keuper Sandstein, precisely similar both in mineral aspect and stratigraphical position to the beds which in Central England have for so long monopolized the title — of “‘ Keuper Sandstone.” They also contain Hstheria (Posidonomya) minuta. Near Rotherberg, in a lane-section, these beds are finely exhibited. They consist of several alternations of very fine-grained white sand- stone, with white, blue, and bituminous shales, in thickness about 10 feet. Near Ensheim~*, the same beds contain vegetable remams, amongst which the following may be mentioned : Calamites arenarius, Brongn.; Tenopteris vittata, Brongn.; Pterophyllum Jegeri, Brongn. The Upper Keuper Sandstein is succeeded by a considerable thick- ness of red, purple, and grey marls and shales, with occasional bands of sandstone, gypsum, and nodules of hematite. These beds cor- respond to the red marls which are superimposed on the “ Keuper Sandstone”’ of the central counties of England, and, while they com- prehend the more considerable mass of the formation, form the upper limit of the Triassic system of both countries. Summary.—A. Tabular View, condensing the remarks made in this paper, is given at p.225. I have adopted the division of the Permian group into three members, as already pointed out by Sir R. I. Murchison, as this formation, both stratigraphically and mineralogically, appears to assume a tripartite arrangement. In England, the lower member, or Roth-todt-liegendes, is confined in its distribution to the Western and Midland Counties, and consists of an areno-argillaceous series, separated into two by an horizon of breccias and conglomerates. It has been shown that each of these subdivisions has its representative in Germany. The middle member, represented in both countries by calcareous zones, 1s in England confined to the North-Eastern Counties ; and is immediately overlaid by the upper member, composed in England and Germany of argillaceous or arenaceous materials. Thus there are three physically distinct members, the lowest of which is itself capable of a ternary division. In the Bunter Sandstone we recognize three members in England, and, though we cannot observe any correspondence with them in the sandstone of the Odenwald, yet, recollecting the exact correspondence in the succession of the Permian and Upper Secondary formations in England and Germany, I do not despair of seeimg the whole ulti- mately parallelized. * Geog. Skizze von Baden, p. 60. + See Quart. Journ. Geol. Soe. vol. xi. p. 426, and Table, p. 448 ; : and ‘ ‘Sila,’ p- 424 et seq. 1857. | SMYTH—EXTINCT VOLCANOS OF VICTORIA. 227 The author regrets that it has not been in his power to extend these comparisons to the rocks of the Vosges on the opposite side of the Rhine valley. He hopes, however, that, unless anticipated, he may have the wished-for opportunity. 2. On the Extincr Votcanos of Victoria, AUSTRALIA. By R. Broves Smuyru, C.E., F.G.S., Member of Council of the Philosophical Institute of Victoria, &c. Tue district within which volcanic products and other evidences of recent igneous action are found extends from the River Plenty (a tributary of the Yarra), on the east, to Mount Gambier on the west. Its most northern point is McNeil’s Creek (a tributary of the River Loddon), in 37° south latitude, and its most southern Belfast, in 38° 21! south latitude (see accompanying Map, fig. 1). Its extreme length is 250 miles, and its extreme breadth about 90 miles. It is said that there are crateriform hills near Lake Omeo, on the flanks of the Australian Alps, and at Lake Tyrrell, near Castle Don- nington, on the River Murray ; but I have not such precise informa- tion as would warrant me to mark those as belonging to or connected with the district now under consideration. By referring to the map it will be seen that this district is bounded on the south by the sea, and on the north it crosses the Spur from the Australian Alps near the Ballaarat Gold-fields*. In the centre is a basin-like depression, the drainage of which is into Lake Ko- rangamite. The most distinctly marked crateriform volcanic hills are : 1. A hill near the source of the Merri Creek, on the dividing range, about 25 miles north of Melbourne. Respecting this, Mr. Selwyn, the Government Geologist, says :—‘‘ On the green hill north of the Kinlochue Inn, Sydney Road, the ancient crater is still distinctly visible. Several other and smaller hills of the same character, but on which no crateriform cavities are visible, occur near the source of the Merri Creek ; and there is little doubt that these hills are the true source whence the whole of ‘the basalt or lava which now occu- pies the country between the Plenty, the Yarra, and the Sydney Road has been derived.’”” And on referring to his recent map of that part of the country, I perceive that, m cutting a roadway, vol- canic ash and scorize were found. The altitude of this hill is about 700 feet. . 2. Mount Aitkin.—This hill is about 1500 feet above the level of the sea. There is no deep well or crater, but the evidences of recent volcanic action are complete and satisfactory. The summit is covered with masses of naked basalt extending in two parallel ridges; and the course of the streams of lava may be traced from the hill. The surface is strewn with fragments of light vesicular lava. The basalt at the summit is not dissimilar to the rock which * See Quart. Journ. Geol. Soc. vol. ix. p. 75, and ‘ The Golden Colony,’ 1855, chap. 16, for Mr. Wathen’s account of a portion of this volcanic district.—Epir. [ Nov. 4, PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 228 Ce, ie 2NONZGNVa 73 & Alm UO7T25 TWAS 2c. ull Fs Wj ““sganpoud 21uD9]0a ZUaIAL YZIM S)PFT W.L0fr1az04O {eee 7 Apis, oii Ww 62 u 3 Wo Sg, mS 1! ai nm in ae ZI 40 ‘sounaj0 4 gourjug ayz fo suorpisog ay, Gumoys ‘nr10,014 fo huojog ay2 fo und wv fo doyy-yozayg—' | *31q 1857.] SMYTH—EXTINCT VOLCANOS OF VICTORIA. 229 is commonly found on the plains; but at the base I found some labourers quarrying a hard, dense, bluish-grey basalt, with included crystals of quartz. The basalt through which the Saltwater River has cut a channel has undoubtedly proceeded from Mount Aitkin and the neighbouring peaks, and it now fills the old basin formed in the palzeozoic rocks; but it does not appear to have altered the physical configuration of the country very remarkably. Indeed, when we look at the Keilor Plains, and examine the thickness of the basalt in many places, the fact is apparent that the surface of the ancient sedimentary strata must have been moderately even and uniform when it was covered by the igneous rock. At Keilor a fine section of the basalt may be seen. Its relation to the paleeozoic rocks is shown in the section, fig, 2. Fig. 2.—Section at Kerlor. Saltwater River. .... Old bed of the river..... t i 7 ‘ t ' { : ’ 4 t 1 a 4 4 1 oo een ee ee woe ee, a. Basalt. 6. Hard quartzose conglomerate. c. Contorted Silurian rocks. The extinct voleano Mount Aitkin has broken through the Silu- rian rocks, and these may be seen in many places in its vicinity rising above the sheets of lava. 3. Mount Boninyong is immediately adjacent to the Ballaarat gold-fields. It has a distinct crater. Masses of very porous lava are found in the neighbourhood, so light that it is easy to lift frag- ments several feet square. The lava covers the older auriferous drift; and the newer drift, also containing gold, rests on the top. 4. Larne-baramul*, or Mount Franklyn, is one of a group of ex- tinct voleanos which are found both to the north, south-east, and west. On the steep side of the hill, the rock is in huge irregular blocks. Here, as in other parts of the district, the lava has fol- lowed the course of the channels which were already formed at the period of eruption, and the streams have extended to a great distance, much of the auriferous drift on the Loddon being covered up by the igneous rock. 5. The MS. plan given of Mount Rouse explains its general character. In the vicinity of the mount there are numerous springs and swamps, and caves of considerable extent have been found. * “ Home of the Emu.’”’ Manuscript plans of Mount Franklyn, Mount Rouse, Mount Leura, and of Tower Hill Lake, from recent surveys, accompanied this memoir, and are deposited in the Society’s Library.—Ep. 230 PROCEEDINGS OF THE GEOLOGICAL sociETy. _ [ Nov. 4, 6. On the west side of Lake Korangamite there are several hills which are crateriform. Amongst the best defined are—Mount Myrt- son, having a lake or swamp in the centre, Mount Wiridgil, and Mount Leura. ‘The ordinary voleanic ash and scorie are found on these hills. Lakes Gnotuk and Bulleen-Merri, situated to the west of Mount Leura, are also, I believe, ancient craters. Lava, similar to that ejected from active volcanos, is strewn over the surface of the hills. It is often curiously twisted ; and masses formed of regular concentric layers are found so similar in form to the trunks and branches of trees, that one was actually sent to me as a fossil tree. On the eastern side of Lake Korangamite there are other hills of an equally distinctive character, the most prominent being Mount Hesse, Mount Gelhbrand, and Warrion, or Labaam. In the Korangamite district we find the “Stony Rises.’’ These occupy a large area both to the south, east, and west of the lake. They consist of rocky, often conical piles, about 25 feet in height, generally rising at an angle of 15°, 20°, or 25°, and so close together that they are im- passable to wheeled vehicles, and only permit a tortuous and uneven path to the equestrian. 7. Tower Hill Lake is situate between the towns of Warnambool and Belfast, and close to the coast; see the accompanying plan. It bears some resemblance to Lakes Gnotuk and Bulleen-Merri. Fig. 3.—Sketch of Tower Hill Lake, near Warnambool, in the County of Villiers. eso . Y WN A NS (7 = ‘ 4 4 3 1 mile. 2 miles. 1857. | SMYTH—EXTINCT VOLCANOS OF VICTORIA. | 23] The water in the lake is, I believe, some 25 feet above the level of the sea. A large tract of swampy land, which appears to have been recently upraised, extends from the southern base of the hill to the sea. The average slope outwards of the hill is about 6°; and the inner slope, which forms the margin of the lake, is about 30°. In ‘the centre of the lake there is an island, irregular in form, on which there are several peaks or extinct craters. Mr. fl. Cadogan Campbell, C.E., of Warnambool, has kindly favoured me with a description of the strata sunk through in digging a well on the south-east slope of the margin of the lake (see plan). He says :—‘“‘ They first sank through about 3 feet of soil, and then for about 60 feet passed through layers of ash, alternately black and white, and of irregular thickness, though none above an inch or two. At the depth of 63 feet the workmen came upon the original surface of the ground, covered with the common coarse grass now found growing. It was not scorched, but merely like dry hay.” He says again :—‘‘ Tower Hiil is one of our most extensive volcanos; but it does not appear that much lava has been ejected from it. What has been thrown out has taken a course to the 8.W.. ‘An immense quantity of ashes has been thrown out, forming layers of a tufaceous rock,—the greatest quantity to the eastward of the mountain, that being the side towards which the wind generally WIOWA. < acu This I have also observed at Lake Purmbeet, where a similar rock is formed ‘from Mount Leura.”’ Underneath the ancient humus, the workmen sank 60 feet threugh a blue and yellow clay. Mr. Selwyn, the Government Geologist, has sent me the following note :— “ Geological Survey Office, 11th Aug. 1857. “ Dear Smytru,—I have just returned from a very hasty visit to the Western Ports and Tower Hill; and with reference to the recent discovery of frogs in sinking a well in that neighbourhood, it may be interesting to you to know that Tower Hill is certainly the most recent voleanic vent I have yet seen in Victoria. “It appears, at least during its later eruptions, to have emitted vast quantities of ash and scorize ; and these are seen near Warnam- bool, resting on beds of shell, sand, and earthy limestone containing numbers of the living littoral species of mollusca. “Tn all other localities where I have examined the large sheets of lava which are so widely distributed over the colony, I have never found them resting on beds of newer date than upper miocene, but have frequently found them, as is the case at Portland, overlaid by beds apparently precisely similar to those which underlie at Warnam- bool the ash and scorize of the Tower Hill crater. “Yours faithfully, “ALFRED R. C. SELwyn.” _ Kimmerid ge Oolite. Cale-Grit Oxfordia mu. | M Oxford l ! WWI a € VECRERED EG! ‘ECS, ah Sections and Fossils of Shotot evil: ean ao, 1857.) PHILLIPS—ESTUARY SANDS, SHOTOVER. 241 from Kimmeridge Clay well characterized by fossils. On the Kim- meridge Clay, abont a mile to the north-east, Iron-sands are seen to rest ; a little further, in the same direction, Portland-beds come be- tween the Kimmeridge Clay and the Iron-sands, and the series of Shotover is complete. In the district between Swindon and Ayles- bury the strata between Oxford Clay and Gault are subject to irre- gularity of thickness and local discontinuity ; in a general sense they may be said to overlap to the north-east, in which direction the Cale-grit, Oxford Oolite, Kimmeridge Clay, and Portland-rock dis- appear one by one, but the Ivon-sands are continuous. It is to be hoped that the Geological Survey, in its progress to the north-east, will furnish new data, and especially additional evidence from organic remains, for the determination of the physical condition of this region in the later Oolitic period. I regard it, however, as certain, that much of the so-called “ Iron-sand”’ on the northern outcrop of the London Basin must be ranked among estuarine deposits. EXPLANATION OF PLATE XIII. Fig. 1. Vertical section of the strata in Shotover Hill. Fig. 2. Section from Oxford to Shotover Hill. Fig. 3. Unio Stricklandii, Phillips. [The lighter tint indicates the restored por- tions at the extremities. ] Fig. 4. Unio subtruncatus (?), Sowerby. Fig. 5. Cyrena media, Sowerby: a, oblique view, enlarged ; 4, side-view, nat. size. Fig. 6. Paludina Sussexiensis (?), Sowerby. Fig. 7. Paludina (?) subangulata, Phillips. 8 . Paludina? 2. On the Patzxozorc Rocks and Fosstus of the State of New York. Part I. The Mineralogical and Paleontological Cha- racters of the Strata. By J. J. Biessy, M.D., F.G.S. [This communication is printed further on. ] DECEMBER 2, 1857. SPECIAL GENERAL MEETING. A proposition for the alteration of the Bye-Laws respecting the Admission-fees and Contributions ta be paid by future Fellows having been proposed and seconded, and an Amendment, to the effect of postponing the consideration of the proposition for twelve months, having then been proposed and seconded, a ballot was taken, and the President announced that the Amendment was carried. ORDINARY MEETING. James Russ, Esq., Canonbury Park ; John Mansell, Esq., Dorset- shire; Edward Meryon, M.D.,Clarges Street; Major Anthony Charles Cooke, R.E., Ordnance Survey Office, Perth; James Templeton, Esq., St. David’s Hill, Exeter ; and Christopher Lonsdale Bradley, Esgq., Prior House, Richmond, Yorkshire, were elected Fellows. 242 PROCEEDINGS OF THE GEOLOGICAL society. [| Dec. 16, The following communication was read :— On some Peculiarities in the MicroscoricaL Structure of Crystaxs, applicable to the Determination of the AquEous or Igneous OrtGin of MineRALs and Rocks. By H. C. Sorsy, Esq., F.R.S., F.G.S. [The publication of this Paper is unavoidably postponed. | (Abstract.) In this paper the author showed, that when artificial crystals are examined with the microscope, it is seen that they have often caught up and enclosed within their solid substance portions of the mate- rial surrounding them at the time when they were being formed. Thus, if they are produced by sublimation, small portions of air or vapour are caught up, so as to form apparently empty cavities ; or, if they are deposited from solution in water, small quantities of water are.enclosed, so as to form jluid-cavities. In a similar manner, if crystals are formed from a state of igneous fusion, crystallizing out from a fused-stone solvent, portions of this fused stone become entangled, which, on cooling, remain in a glassy condition, or become stony, so as to produce what may be called glass- or stone-cavities. Applying the general principles resulting from his examination of these phenomena to the study of natural crystalline minerals and rocks, the author showed that the fluid-cavities in rock-salt, cale- spar, gypsum, and some other minerals usually indicate that these minerals were formed by deposition from solution in water at a tem- perature not materially different from the ordinary; also that the constituent minerals of mica-schist and the associated rocks contain many fluid-cavities, indicating that they have been metamorphosed by the action of heated water, and not by mere dry heat and partial fusion. From the study of the stone- and glass-cavities in slags and lavas, and from the examination of the microscopic characters of quartz- veins and felspar, which contain both fluid- and stone-cavities, the author arrived at the conclusion that granite is not a szmple igneous rock, like a furnace-slag, or erupted lava, but is rather an aqueo- igneous rock, produced by the combined influence of liquid water and igneous fusion, under similar physical conditions to those existing far below the surface at the base of modern volcanos. DECEMBER 16, 1857. Charles Wright, Esq., Wigan; John W. Woodhall, Esq., Scar- borough ; and Dr. Eugene Francfort, Clapham Road, were elected Fellows. Dr. H. Abich, St. Petersburgh, was elected a Foreign Member. The following communications were read :— 1857. BUNBURY—NEUROPTERIS. 243 1. On a remarkable Specimen of Nevrorreris; with Remarks on the Genus. By C.J.F. Bunsury, Esq., F.R.S., F.G.S. THE rarity, in a fossil state, of the young unexpanded' or half- expanded fronds of Ferns has been remarked by more than one botanist. Fern-fronds in that early stage of development are very easily recognized by the peculiar and beautiful manner in which they are rolled up, forming a spiral curve, like the head of a crosier. This circinate vernation, as it is called, appears to be universal in all Ferns, with the exception of the small tribe of Ophioglossacee ; and, in those numerous kinds which have perennial or evergreen foliage, fronds in this state may be observed at most seasons of the year. Their rarity as fossils is therefore rather remarkable. That they do occur is evidence, as Dr. Hooker observes*, ‘‘ that the evolution of the fronds followed the same law then as now.”’ Adolphe Brongniart has figured, in his great work‘, a fine specimen of such a circinate frond belonging to Pecopteris Miltoni ; two are represented in Gop- pert’s ‘Systema Filicum Fossilium’ {, and one in Geinitz’s beautiful work on the Coal-formation of Saxony§. But all these belong to the genus Pecopteris; I am not aware that a similar state of any Neuropteris has yet been recorded. I therefore wish to lay before the Society a description and drawing of a specimen in my own col- lection, which may perhaps contribute to settle our notions of the true affinities of that genus. Upper portion of a Young Frond of Neuropteris from near Oldham, Lancashire. — a. The crosier-like frond, terminal part. - 6. Outline of a leaflet. * Memoirs Geol. Survey, vol. ii. part 2. tT Histoire des Végétaux Foss. pl. 114. fig. 1. {PIC a6. foe 8, § Pld. fig, 10. 244 PROCEEDINGS OF THE GEOLOGICAL society. [ Dec. 16, The specimen was procured from Glodwick Colliery, near Oldham, in Lancashire, and formed part of a set of fossils sent to me by Mr. Wright, at the request of Mr. Horner. The material is a dark- coloured, hardened, ferruginous clay, very slightly schistose. The frond in question is unfortunately (as almost always happens) incom- plete, the lower part of the stalk being broken away ; but otherwise its state of preservation appears to be as perfect as that of any speci- men of the kind hitherto noticed. We see the rhachis or main stalk of the frond exhibiting the graceful crosier-like curve so characteristic of the young fronds of Ferns; and the leaflets, regularly ranged along its concave side, successively overlapping one another from below upwards, and becoming progressively smaller and more crowded towards the extremity of the fragment. Their veins, which are well preserved, and as much as can be seen of their outline, in particular the shape of their base, agree with those of the numerous leaflets of Neuropteris which are scattered through the same stone. The species appears to be Neuropteris gigantea, Ad. Br., or a variety of it. The N. gigantea, indeed, in the most complete specimens, shows a doubly pinnated frond, whereas this fragment is merely once pin- nated ; but it may be only a portion of a frond; and, besides, it is not very uncommon to find the same Fern varying with pinnate and bipinnate fronds, as is the case for instance with Péeris hastata, Swartz, Gymnogramme tomentosa, and some Adiantums. The rhachis of the specimen is not so well preserved as the leaflets, but appears to have been hairy. This specimen is, I think, interesting, as affording a strong confirmation of the opinion that the fossil Newropterides were true Ferns. Some have been tempted to doubt this, because of the constant absence of their fructification,—a fact certainly remarkable, when we consider the abundance of their fronds in many coal-fields. But, in addition to their venation and form, which are truly those of Ferns, we now find that they have the very remarkable and charac- teristic vernation of that order. Let the specimen here described be compared, in particular, with the young frond of Nephrolepis exal- ‘tata, Presl (Aspidium exaltatum, Swartz); it will be found that the position of the young leaflets relatively to one another and to the stalk is almost precisely the same. . This character shows, I think, conclusively, that Neuropteris has nothing to do with the Coniferous order, in which there is never any approach to a circinate vernation. Even in Salisburia, the leaves of which are in form and veining so much like those of Ferns, their arrangement in the young state is quite different: their lobes are folded together, and somewhat rolled inwards; but they are erect from the first, without the least curvature of the stalk. The only phanerogamous plants that resemble Ferns* in the vernation of their leaves, are some Cycadee+ ; and in the absence of fructification it is * Perhaps I ought to except the genus Drosera, in which also the leaves are truly circinate in vernation; but, as they are otherwise totally unlike Ferns, and can never be confounded with them, they do not enter into this comparison. t+ The Cycadee are described, at least, as having circinate vernation; but Dr. Hooker informs me that this character is not constant inthe family. I have not myself had much opportunity of observing them in a living state. 1857. | BUNBURY—NEUROPTERIS. 245 certainly not very easy to prove positively that the Neuropterids may not belong to that family. The leaves of Cycads have generally, indeed, simple veins; but in those of Ceratozamia Mexicana the veins are occasionally, though not generally, dichotomous. In the curious and anomalous Stangeria, a true Cycad, the leaves have so perfectly the characters of Ferns, that the plant was originally taken for a Lomaria, the veining and other characters of the leaves being exactly those of that genus. If the leaves of the Stangeria had been found fossil, in the imperfect state in which fossil plants generally occur, it would, I believe, have been impossible to show that they did not belong to a Fern. The leaves of all known Cycads, however, are simply pinnated, whereas those of the Neuropterids, in all cases where they are pretty completely known, are doubly pinnated. In their apparent texture, moreover, in the characters of the leaf-stalks, in the variations of form of the leaflets in different parts of the frond, and in their whole appearance, the Neuropterids of the Coal-measures are so completely Ferns, that, in the absence of any evidence to the contrary, we may safely consider them as such; and I have little doubt that their fructification will in time be found to confirm this: conclusion. If we inquire to what recent Ferns the fossil genus Neuropteris was most nearly allied, we shall hardly, I fear, arrive at any very certain conclusion. The older writers compared the commonest Coai- measure species to Osmunda regalis, but merely because of a general vague resemblance. A venation nearly approaching to that charac- teristic of Neuropteris is seen in the Pteris hastata, Swartz (Allosorus hastatus, Presl), and some nearly allied species. These Ferns have also a general resemblance in form to many species of Neuropteris, and particularly in the great differences of outline and form in differ- ent leaflets of the same frond. But a similar veining occurs in some of the broad pinnuled species of Gymnogramme, such as G. tomentosa, Ferns widely different in their fructification from Allosorus. Again, while Allosorus hastatus and A. flecuosus have nearly the venation of Neuropteris, Allosorus calomelanos (a very near ally of these two species) would, if found fossil, be referred to Cyclopteris. The veins, in fact, afford but slippery characters, although the best that are generally within our reach, for the arrangement of fossil Ferns. We know, moreover, that in those cases where the fructification of fossil Ferns has been found in a good state, it has often indicated affinities quite different from those which would have been inferred from the veins or the outline. Thus, the Alethopteris aquilina has a striking resemblance in form and venation to some species of Péervs, yet its fructification, as shown by Geinitz, seems to place it in quite a different tribe of Ferns, namely the Gleicheniacee. Again, the Pecopteris exilis, Ph., with the aspect of some small Polypodium or Nephrodium, has (as I have elsewhere shown) the peculiar spore-cases characteristic of the Schizeacee*. I should not, therefore, be sur- prised to find that the Neuropterids differ considerably in their real * Quart. Journ. Geol. Soc. vol. vii. p. 188. 246 PROCEEDINGS OF THE GEOLOGICAL society. [ Dec. 16, affinity from those recent Ferns to which they have most likeness in outline and veining. . I have scarcely seen a genuine Neuropteris from any formation more recent than the Triassic age. The beautiful and curious fern from the coal-field of Richmond, Virginia, which I described * under the name of Neuropteris linneefolia, can hardly be considered as properly belonging to this genus ; its leaflets have no trace of midrib, nor has it the general appearance of a Neuropteris. It agrees better with the technical characters of Cyclopteris or Adiantites ; but it appears to have no very close natural affinity to any other fossil Fern yet known, and will probably hereafter form the type of a new genus. With respect to the age of the deposit in which it was discovered, I learn from Sir Charles Lyell that the most recent observations tend to refer the Richmond coal-field to the Keuper rather than to any member of the Jurassic series. The Neuropteris ligata, and N.recentior of the “ Fossil Flora,”’ from the Jurassic strata of Scarborough, have evidently nothing to do with this genus, but were very properly referred by Professor Phillips to Pecopteris. Indeed the WN. ligata is identical with Pe- copteris denticulata, Ad. Br. The Neuropteris lobifolia, Ph. (N. undulata, L. and H.) is more ambiguous in its characters, and may fairly enough be referred to this genus. It cannot, however, be con- sidered by any means as a characteristic Neuropteris. In saying that I do not know of any well-characterized Neuro- pteris from a formation later than the Trias, I purposely leave out of the question the enigmatical Anthracitic formation of the Alps, which many geologists refer to the Liassic period. It contains several forms of Neuropteris, to all appearance identical with those of the Coal-formation. If really Jurassic, it is altogether ano- malous and exceptional in its palzeobotanical characters. Since my paper} on the subject was read before this Society, I have had the opportunity of examining some additional specimens from this Alpine Anthracite deposit, and from a different locality ; and I must still say of them as I said before, that all which are in a fit state for ex- mination belong to forms elsewhere characteristic of the Coal, while there is an entire absence of all the characteristic Jurassic forms. Professor Heer, after a careful examination of very ample materials, came to the same conclusions§. Until this anomaly be satisfactorily explained, it is evident that we cannot safely rely on fossil plants as certain indications of the age of any formation. The five beautiful and rare species of Neuropteris discovered in the Grés bigarré of the Vosges (see Schimper and Mougeot’s Mono- graph, plates 36-39), agree perfectly with the artificial characters of the genus, though they may, not improbably, be considerably removed in natural affinity from the Carboniferous kinds ||. * Op. cit. vol. ili. p. 281. tT See Quart. Journ. Geol. Soc. vol. v. p. 130. + Namely, from Mont de Lans, in the Department of the Isére. The specimens were shown to me by Dr. Ewald, at Berlin. § See his excellent paper on this subject, translated in Quart. Journ. Geol. Soc. vol. vii. 2nd part, p. 91. || Schimper and Mougeot, Monogr. p. 76. 1857. | BUNBURY—NEUROPTERIS. 247 I will conclude with a few remarks on some of the species of Neu- ropteris. But first I must observe that the number of described species is probably much too great, and that the greater proportion of them would probably be found, if completely known, to be varia- tions or modifications of a few real specific types. Many of them have been described from very imperfect specimens, often indeed mere fragments. Now in those kinds of Neuropteris which are best known, we see that (as in very many recent Ferns) the size, outline, and position of the leaflets vary very much in different parts of the same frond. In some of those recent Ferns which I have compared with them, we see a remarkable degree of variation, both in the same frond, and in different fronds from the same root. In making use, therefore, of such imperfect materials as we most often have before us in the case of fossil plants, we are exceedingly liable to create false species, and to describe under several distinct names different frag- ments which may even have grown originally from one root. I doubt whether any judicious botanist would venture to establish new species of recent plants from materials so scanty as those on which very many fossil species have been founded. I may take this opportunity of observing that my Odontopteris subcuneata* is probably the terminal portion of the frond of some large Neuropteris, though I cannot positively assign it to any de- scribed species ; at any rate, a species ought not to be founded on so imperfect a fragment as the only one I have seen of this supposed Odontopteris. In the absence of a midrib, it resembles the Neuro- pteris auriculata, a plant the extreme variableness of which has been well shown by Geinitz+. This author has pointed out, that some of the many various forms of leaflets belonging to that species have been described as belonging to the genus Cyclopteris. In like man- ner the round lateral leaflets of Neuropteris cordata, which I have figured{ from Cape Breton specimens, have altogether the charac- ters of Cyclopteris. Those common Ferns of the Coal-measures which have generally been referred to Cyclopteris (Cyclopteris obliqua, C. orbicularis, C. dilatata, and some others), and of which Brongniart has formed his genus Nephropteris, are most probably, as that author has remarked, young or anomalous fronds of different species of Neuropteris, ana- logous to the barren fronds of the recent genus Platycerium. 1. Neuropteris gigantea, Ad. Brongn. I believe.the N. Martini of Goeppert (the Phytolithus Osmunde regalis of Martin) to be identical with this species, which is one of the most common in the Derbyshire coal-field. Among the specimens received from Mr. Wright, from Oldham, Lancashire, I find a variety (as I believe it) of N. gigantea, having the leaflets remarkably curved upwards, almost hooked, or what botanists call scimitar-shaped. It occurs intermixed with the common form, with which it agrees in all other characters that can be observed. I call it Neuropteris gigantea, var. falcata. * Quart. Journ. Geol. Soc. vol. iii. p. 427. + Steinkohl. in Sachsen, p. 21. t Quart. Journ. Geol. Soc. vol. iii. pl. 21. fig. 1 A and 1 B. é —————— 248 PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 16, 2. Neuropteris flexuosa, Ad. Brongn. After the examination of a great number of specimens of this, from Somersetshire, Savoy, Spain, Pennsylvania, and Cape Breton, I am unable to satisfy myself whether it be permanently distinct from N. gigantea. They are indeed in general easily enough distinguished by the form of the base of the leaflets, whet in NV. flexuosa is more oblique and less symmetrica! than in the other, with its lower margin extended into a decided angle or auricle, while the upper one is rounded off. The wavy main stalk is also a usual characteristic of NV. flexuosa. But both these characters vary in degree, and I have seen specimens in which they are quite ambiguous. The character on which Brongniart lays so much stress, that of the closely-placed overlapping leaflets, is (as I long since remarked) by no means constant. Whether the NV. gigantea and N. flexuosa be truly distinct or not, they seem to have inhabited differ- ent localities, for I am not aware that I have in any case seen well- characterized specimens of both from the same coal-field. As they may in general be pretty easily distinguished, though intermediate forms do now and then occur, it will be convenient for the present to keep them separate. M. de Verneuil lately showed me specimens of N. flexuosa from the province of Palencia (in the kingdom of Leon), Spain. It seems to be most abundant in the coal-mines of North America. The only well-characterized British specimens that I have seen are from the Somersetshire coal-field, and from that of Pembrokeshire; while, on the other hand, the VV. gigantea seems to abound particularly in the Midland coal-fields of England. 3. Neuropteris rotundifolia, Ad. Brongn. I cannot but believe this to be a mere variety of NV. flexuosa, as I have seen on the very same fragment leaflets corresponding with the characters of both. The analogy of innumerable instances among recent Ferns (of Péeris rotundifolia, Swartz, for one) shows us how little importance ought to be attached to such variations in the outline of the leaflets as those on which the distinction of these two species is founded. At any rate, the N. rotundifolia is much too doubtful a species to be of any value as a geological characteristic. Nor, with respect to locality, is it peculiar to the Calvados; there is a good specimen of it from Northumberland, in the museum of this Society. 4, Neuropteris rarinervis, C. Bunbury (Quart. Journ. Geol. Soc. vol. iii. p. 425.). I suspect that this species is not uncommon, and that it has often been confounded with N. tenuifolia. The two are certainly much alike ; but, if we may trust to the figure and specific character of WV. tenuifolia in Brongniart’s great work, they differ materially in their veining. Some of the specimens labeled NV. tenuzfolia in the Society’s collection, namely those from Merthyr Tydvil, seem rather to belong to NV. rarinervis ; and I am inclined to refer to the same species some fragments that I possess from the district of Osnabrick. If this plant be compared on the one hand with WN. tenuifolia, and on the other with the Pecopteris (Cladophlebis) pteroides, we shall see how they connect together the two artificial genera Neuropteris and Pecopteris, 1857. | PRESTWICH—BORING AT HARWICH. 249 and how difficult it is to draw a line of distinction between the two. Neuropteris rarinervis has perfectly the general aspect of a Neuro- pteris ; indeed, if the difference of its veins were overlooked, it might easily be taken for a variety of N. flexuosa, with smaller leaflets than usual. Cladophlebis pteroides has more the appearance of a Peco- pteris ; yet in venation the two agree almost exactly. 5. Neuropteris Loshiit, Ad. Brongn. The plant from Felling Colliery, figured as N. Loshii in Lindley and Hutton’s ‘ Fossil Flora,’ is separated by Sternberg and Goeppert under the name of N. Lind- leyana; chiefly, it would seem, because its leaflets are not cordate at the base. Considering how variable a character this is in recent Ferns, I cannot think it a sufficient ground of distinction in this instance ; and I have little doubt that Lindley and Hutton’s plant was rightly referred to N. Loshz, which seems to be a widely-spread fossil Fern, very abundant in the coal-fields of the Midland counties of England. Neuropteris Loshii is found also in the Permian system, sonitely: in the red sandstone (Rothliegendes) of Saxony ; there are fine spe- cimens of it from that formation in the museum at Dresden, some of them showing, more satisfactorily than any others that I have seen, how very distinct it is from the N. heterophylla. Gutbier and Geinitz, in their work on the Permian fossils of Sax- ony, have noticed and figured * specimens of N. Loshiz, showing what they consider as appearances of fructification ; but there is so much irregularity in the position of these markings, that I cannot help doubting whether they are really of that nature. 2. On the Bortne through the CuaLx at Harwicu. By JosepH Prestwicu, Esq., F.R.S., Treas. G.S. Ow1nce to the insufficient supply and indifferent quality of the water at Harwich, several attempts have from time to time been made to improve that supply by means of deep wells in the Tertiary sands and the Chalk. None of these having been attended with the desired success, although in 1824 and 1826 two borings were carried down to a depth of 293 feet and 192 feet in the Chalk, a public work of great spirit has lately been undertaken under the superintendence of Mr. Peter Bruff, C.E., to bore deep into, and, if necessary, through the Chalk. I saw this well in August 1856. It had not then traversed the Chalk. In November last, however, the Rev. J. H. Marsden informed our Assistant-Secretary that the boring had been success- fully + carried through the Chalk, Upper Greensand, and Gault, and that immediately beneath the latter a ‘‘ black rock”? had been found, of which he sent up a specimen. Mr. Marsden shortly afterwards favoured us with the following section (Column 2), on which, as the geological results are so curious and important, I purpose making a * Verst. Perm. Sachs. pl. 4. fig. 2. + So far as the work was concerned, but without, I regret to say, having at present found a supply of water. 250 PROCEEDINGS OF THE GEOLOGICAL society. { Dec. 16, few remarks, as well as on a suite of specimens which Mr. Bruff kindly submitted for examination. The well, which is situated near the Pier and a few feet only above the level of the river, was commenced in July 1854, and in May 1857 had reached.its present great depth. Section of the Boring at Harwich. 1 rer 2 Feet ‘ ALD. cpccemwewinnnanicaemewammedenselis 10 Drift. servsveisiraverens sey REGioF AVE] isc. csseds- see eaeee tas 15 (London clay “......7...cnetqe eens 23 | Coarse dark gravel...........sces0e: 10 Plastie:elayiewsts.cie0cediete dace 7 rt ) ECGS Dace: ols los Bluish clay with green sand...... 35 | Green and red sand intermixed... 5 LeDLLE CLAY: stats essancnee seemenenes 3 Chalk with*fimts: “icc2eseontecses 690 Challe wisteeetaastan- laces 888 ft.4 Chalk without flints ............... 160 Chalk, rocky, in thin layers ...... 38 Greensand and Gault............... 22 Opie NCEE SGT Gs 1 Gantt WithOUt SANG. ses: scseeeeee 39 Black ‘slaty YOK... -sssses=-aareners 443 1070 It thus appears that, after passing through the Chalk and finding the Upper Greensand well marked and in regular order, and then the Gault, but im diminished thickness, the workmen came, at a depth of 1025 feet, to a mass of strata denoted as a black slaty rock. Un- fortunately this rock, as far as I have examined it, contains no fossils ; we have therefore only its mineral and physical characters to guide us. These however are tolerably marked. The Upper Greensand is very calcareous and rather argillaceous. The Gault also consisted of the usual calcareous clay ; but the under- lying rock does not effervesce at all with acids. It also has a rough slaty fracture, and becomes harder and of a darker grey in descend- ing. It contains a little mica. Some portions, however, have a more glossy and greenish hue; but the greater part is a common grey clay-slate. The specimens brought up by the boring-tools consist of round cylinders, abont 3 inches in diameter, which break so as to show the lines of bedding or of cleavage, or possibly of both; for I find that three specimens, from depths of from 1040 to 1060 feet, split at angles respectively of 55°, 53°, and 58° with the surface, whereas one specimen from a depth of 1066 feet and another of similar character, but without depth mentioned, give angles of about 84°. In one of the latter specimens there is also a trace of another divisional plane with a slight variation of mineral character more resembling lines of lamination or bedding ; and, on measuring the angle formed by these two lines in this specimen, I find it to be about 30°: and, as the three specimens higher up give only one divisional plane, which is inclined with an average dip of 55° to the level furnished by a line at right angles to the axis on the vertically bored cylinders, this would seem to show that there is one set of parallel divisional planes throughout, and that there are traces of TSD7.| PRESTWICH—BORING AT HARWICH. 251 another inclined to the first at an angle of 30°; and, allowing for the smallness of the specimens and the difficulty of very exact deter- minations, it seems probable that these two planes may possibly be, the one a plane of dip of about 55° and the other a rough cleavage- plane of about 84° to the horizon. Of the direction of the dip I have no evidence. The overlying beds themselves here have a not unimportant dip; for in an old well in the vicinity the chalk is 64 feet deep, and in another 70 yards north, and on the same level, it is 88 feet deep, showing that the chalk and tertiary strata here dip about 9° southward,—a fact further corroborated by the cireum- stance that the chalk rises out at sea at the distance of a few miles southward, off Walton. These facts render it almost certain that this rock cannot belong either to the Cretaceous or the Oolitic series, but probably belongs to some of the older slaty rocks. This Harwich well has an important bearing upon the character of the evidence furnished by the Kentish Town well. The discovery there, under the chalk, of greenish and red sandstones and clays was so unexpected, that, although it was evident that they closely reserhbled some parts of the New Red Sandstone (and, without evi- dence to the contrary, such similarity of lithological character must be accepted as the best proof that could be obtained), still the ques- tion could not be considered as fully settled without some more positive evidence, the more especially as M. Jus showed me some fragments of cretaceous Ammonites and Belemnites brought up with the red clays; but, as I then observed, they might have fallen down the side of the bore-hole from the cretaceous beds above. Some clay which I had washed on purpose yielded no fossils*. Nothing further has been done to the Kentish Town well; but the evidence which we have now obtained from the boring at Harwich, combined with that of the Calais boring, is corroborative, and of such weight, that I do not hesitate to modify materially my former opinion of the continuous range of the Lower Greensand under London, and to adopt in great part Mr. Godwin-Austen’s very in- genious and philosophical hypothesis of the extension of an under- ground tract of the older rocks, ranging from the mountains of the Ardennes in Belgium to the Mendip Hills in the West of England. Before the result of the Kentish Town well was known, Mr. God- win-Austen had arrived at the conclusion that a tract of old rocks underlies the Wealden; but he probably was as little prepared as I was for so remarkable a confirmation of his hypothesis as that furnished by the well at Kentish Town, as there, not only were all the Oolitic series wanting, but the Lower Greensand itself was absent. I fear, therefore, that there is, under the central part, at all events, of the London Tertiary area, a tract or ridge of the older rocks imme- diately underlying the Chalk and Gault, on different portions of which the three wells of Calais, London, and Harwich have touched, the one on the Carboniferous series, the other on the New Red Sandstone, and the last on some slate-rock to which, in the absence of organic ‘remains, it is not yet possible to assign its exact position in the pale- * Quart. Journ. Geol. Soc. vol. xii. p. 10. VOL. XIV.—PART I. s 252. PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 16, ozoic series. Atthe same time I must observe that it was impossible, without actual experiment, to have arrived at this conclusion; for the Lower Greensand crops out with so much regularity in the dis- tricts immediately south and north of London, and with characters so much alike, that it was not possible to infer @ priori the interruption caused by the old underground ridge, nor can I even now believe that there is a total want of continuity. It is evident that the Lower Greensand must be continued underground to some unknown distance between Reigate and London on the one side, and Woburn and Lon- — don on the other, and also that the Lower Greensand of Cambridge must range for a certain distance in the direction of Ipswich. It is a question of what was the size of the old paleeozoic land— was it a ridge, with breaks in it at intervals, or a broad tract? The first is, I think, the more probable; for I cannot imagine but that, from the very peculiar mineral character of the mass in Bedfordshire and Surrey, there must have been, in places, continuity between these areas, and I therefore infer that the Lower Greensand may yet be found under the Chalk at many places, and that, although not immediately under the north of London, it yet will be found at no great distance both to the north and south of that spot. Note.—Mr-. Bruff has just sent me up a specimen of the slate (from the depth of 1050 feet), containing an impression of what appears to be a large Postdonia. If so, that will remove all doubt as to the age of this rock, as this shell is, with the exception of one species which occurs in the Lias, confined to the Palzeozoic rocks.—April 1858. 3. On a Boutpver of Granite found in the “ Wuitr CHALK,” near Croypon; and on the Extraneovus Rocks from that Formation, By Rospert Gopwin-Austen, Esa., F.R.S., G.S. Part I. CONTENTS. . Introduction. i tes Locality and Position of the Croydon Boulder. Previous notices of extraneous materials in Chalk. Description of the specimens exhibited. ' Form of the Boulder. Character and composition of the Boulder, and of the associated Sand and Greenstone. Observations and Inferences. Part II. . Mode of deposit, extent, and nature of the Fossils of the White Chalk. Means of transport of extraneous materials in the Cretaceous Sea. Form and composition of the Land of the Cretaceous Period. Part I. Introduction.—So recently as 1811, when Mr. James Parkinson published his work on the ‘Organic Remains of a Former World,’ petrifactions of animal- and plant-structures were called “‘adventi- tiovs”’ or “ extraneous,” whilst all mineral materials, whatever their character or the composition of the beds in which they occurred, would have been considered as properly belonging to such beds and in their natural positions. _A true perception of the origin of the 1857.] GODWIN-AUSTEN—BOULDER IN CHALK. 253 sedimentary strata of the earth’s crust has produced a complete change in such views; the remains of animals, such as Mollusca, are inseparably connected with the deposits formed beneath the areas of water in which they lived. Materials, whether organic or inorganic, can be said to be ‘ ex- traneous”’ only with reference to the special conditions of accumulation implied by the beds in which such materials occur. A solitary deep- sea mollusc amidst an assemblage of shallow-water forms is an “‘extraneous’’ one ; and, on the other hand, the boulders and shingle of a coast-line, or ponderous shells from the marginal zone, are foreign to deep-sea sedimentary beds. Such is the sense in which the term “ extraneous”’ has been employed in the following pages. Whenever, in the examination of old sea-beds, such phenomena as these present themselves to the geologist, their investigation will be attended with interest and advantage: the solution of such ano- malies invariably conducts to some further knowledge of the conditions and agencies of the period when such things happened. The evidences of abnormal agency are to be met with in the sedi- mentary deposits of all periods. Locality and Position of the Croydon Boulder.—The Boulder which, together with some other associated materials, forms the sub- ject of the present communication was found in a chalk- pit, worked by Mr. Pettiver, by the side of the old London and Brighton road, near Purley, about two miles south of Croydon. The road at this place runs along a deep valley in the chalk ; and it may be here observed that the upper and higher surface of the adjacent district is much eroded into furrows and covered with detritus, but that the sides of the valley are altogether free from either. The valley is one of those which have been excavated since the removal of the lower tertiary strata from off the district. The bottom of the valley is filled with a thick accumulation of gravel, being an extension of that which is to be seen near the Croydon Station, but which gravel does not rise to the level of the floor of the quarry where the boulder was found. The portion of the Chalk-formation in which the pit is worked, is the lower part of that containing flints. The boulder in question was originally discovered by the men employed in the quarry, who exposed it in raising chalk for lime ; it was removed and put aside, but the place it had occupied would not seem to have been much disturbed. The first person to whom it was subsequently shown was Mr. Simmonds, who, judging from its external ochreous appearance, took it for a huge nodule of iron- pyrites. He accordingly recommended the men to break it, when, to his astonishment, he found it to be a mass of crystalline rock resembling granite. In an account of the discovery, lately communicated to Mr. Rupert Jones, Mr. Simmonds says: “ Thinking it sufficiently interesting, and _ never having seen anything of the kind myself after considerable experience in the Chalk, I thought it right that others should be witnesses of the fact whilst the hole from whence it came was open. s2 254 PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 16, I accordingly invited my friend Dr. J. Forbes Young to accompany me to the place, which he did. ‘We set the men to work round the spot ; and they found at the bottom a quantity of coarse sand-like materials, which on examination proved to be decomposed rock of the same kind. They also dug from the same place several large fragments of greenstone in a state of decomposition and surrounded by debris of their own class.” It was after this, and some time in the month of August, that I received a communication from my friend Mr. Rupert Jones, re- specting the discovery in question. I lost no time in visiting the locality indicated ; and from what I then saw, as well as from the evidence I collected, I felt perfectly satisfied that the boulder, together with its associated materials, when first discovered, was fairly im- bedded in the solid chalk, and that their mode of occurrence was suggestive of various considerations deserving of notice. Previous notices of extraneous materials in Chalk. — Though I cannot find that the occurrence of such materials as these has ever been made the subject of any special communication to this or any other like Society, yet it must not be understood that ex- traneous materials in the body of the White Chalk formation have not been noticed. I have several times had such specimens brought to me; they are also to be met with in numerous private collections ; and some of them I am enabled to exhibit here this evening, through the kindness of their possessors*. Major-Gen. Portlock has noticed several remarkable examples of blocks of hard black basalt, isolated in the Chalk of Ireland (see ‘Report on Londonderry,’ &c., pp. 93, 94). In 1840, Mr. Griffith also called attention to the occurrence of flattened spheroids of syenite in the Chalk of Antrim. There are also two other short recorded notices. ‘In this country,” observes Dr. Mantell (‘Geology of the S.E. of England,’ p. 78), “the Chalk very rarely contains traces of older deposits. ” The only instances of extraneous rocks that have come under my observation are pebbles of quartz, and some fragments of green schist.”’ Mr. Dixon (‘ Geology of Sussex,’ p. 69) says, “Small pebbles and large rolled fragments of sandstone and quartz-rock are occasionally discovered in the centre of the Upper Chalk. Mr. Coombe found one specimen weighing near fourteen pounds at Houghton, Sussex; and I have seen others from the same pit of two and three pounds weight ; several also have been sent me by Mr. Catt from the pits near Lewes.” Description of the specimens exhibited.—I may here observe, that shortiy after the published notice of the verbal communication I made of the Purley discovery to the Geological Section of the British Asso- ciation at Dublin, I was informed by Mr. W. Cunnington, of Devizes, that a specimen of slate imbedded in flint had been fuund in Wilt- shire. I had next an opportunity of examining a collection of extraneous materials from the Chalk, belonging to this Society, and * Specimens from the Museum of the Geological Society, and from the Collec- tions of the Rev. T. Wiltshire, F.G.S., W. Cunnington, Esq., F.G.S., W. Harris, Esgq., F.G.S., and H. Catt, Esq., were exhibited when the paper was read. 1857. ] GODWIN-AUSTEN—BOULDER IN CHALK. | 255 others the property of Mr. W. Harris. These were interesting, as, in addition to the crystalline rock-pebbles, there are some small spe- eimens which have the appearance of being volcanic scorie. Dr. Forbes Young also kindly communicated some facts relating to the Purley discovery, and placed at the disposal of the Society the seve- ral materials which he had collected at the pit; the largest frag- ment measures about 12 inches in each of its two longest diameters, and weighs upwards of 24 pounds. Mr. Catt’s collection contains three specimens of rather soft, marly, micaceous sandstone, of a greenish-grey colour, one pebble of opake quartz, two of transparent quartz, and one of coloured quartz: these are all small. There is a much larger sub-rhomboidal fragment of dark clay-slate, with the angles rounded, and lastly, a block of fine-grained sandstone (quartzite), weighing thirteen pounds fourteen ounces. All these fragments have been derived from old sedimentary (palzeozoic) strata. The largest block shows the bases of several attached bodies, such as Diblasus or Isis, a Serpula, a Bryozoon (Diastopora ramosa?), and the lower valve of a Spondylus lineatus. This block had been rolled about on a beach, after these forms had attached themselves. Mr. Cunnington’s specimen consists of a fragment of thin fissile slate (very like common roofing-slate) imbedded in a chalk-flint. The slate has apparently been broken in the direction of the cleavage, and at the time when the flint was broken, so that the original form of this fragment cannot be determined. As the cases where the occurrence of such materials has been observed are likely to be far less numerous than those which have escaped observation, or not been recorded, and as the pits where chalk is quarried present only a most trifling portion of its mass when com- pared with the horizontal extent of that formation, we may fairly infer that the differences of such extraneous materials must be much greater than we have heretofore supposed. Form of the Boulder.—When I visited the Purley chalk-pit, I was informed that the large block had been still further broken up at the time of Dr. Young’s visit, so that the destruction of the principal mass was then almost complete; some portions had been carried away by various persons, whilst others had been put into the kiln, by way of experiment, for the purpose of ascertaining whether they would burn into lime, like the chalk. The largest fragment which I was able to secure rather exceeded five pounds in weight. On the spot where the blocks had been broken up, I found a con- siderable quantity of loose fragmentary materials identical with one of the larger portions, and derived from the more decomposed parts. According to the account given by the quarrymen, the block, when first exposed, presented a rounded surface,—a statement which is confirmed by the appearance of all the fragments which have been preserved, which also show it to have been boldly ege- shaped. When I first visited the quarry, I was told that the cavity (or the lower part of it) which the block had occupied remained in the same condition as when it was first lifted out of it. On carefull removing the loose chalk that had fallen m, there was presented a 256 PROCEEDINGS OF THE GEOLOGICAL sociETy. [Dec. 16, basin-shaped depression in the hard chalk, measuring rather more than a foot across ; the slight depth of this cavity compared with its diameter, showed that it was the cast of the lower portion of the boulder. The original form of the boulder may be also shown by fitting on the larger fragments to the remaining principal mass ; it will then be clearly seen that it is a rounded water-worn block, just such as may be met with by thousands on any coast-line of our own seas, which is composed of rocks of*like mineral character, as about the Scilly Isles, the Channel Islands, or those of Brittany. Character and composition of the Boulder, and of the associated Sand and Greenstone.—The Purley boulder is a crystalline granitoid rock, having its components very uniformly distributed: those now remaining are quartz and felspar, from which, perhaps, some other mineral has been removed; what this may have been will be con- sidered in the sequel. Whether the rock-mass here in question had or had not undergone such a change before it was imbedded, can- not now be determined with any certainty. It will, however, be observed that the Purley block, which is by far the largest mass which as yet has been found imbedded in the Chalk, and which therefore, as far as size is concerned, would be well fitted to resist the process of decomposition and the removal of one component, presents a cellular character throughout, whereas the smallest pebbles and fragments of other granitoid rocks exhibit no such structure. On showing a fragment of the large Purley block to Mr. D. Forbes, he thought that he recognized it as corresponding in composition and external characters with a peculiar granitic rock which was intro- duced into the Scandinavian sedimentary series about the later palzeo- zoic period. On the whole, therefore, I am disposed to consider that the rock was in precisely the condition in which it is now seen at the time it was imbedded, and that, if it has experienced any de- composition, it was previously to its removal from its original site. That all the extraneous rocks which had been met with in the Chalk should have occurred as isolated fragments, was somewhat remarkable; and the only case of an approach to anything like definite relative position amongst them was the discovery of several about the same time at Houghton, in the same pit, and whilst the men were at work on the same bed; so that the fragments there may have been scattered about at the same time: but in the case of the Purley boulder the case was very different. I will first refer to Mr. Simmonds’ account, quoted above, p. 254 ; he notices the occurrence of sandy granitic matter, and fragments of decomposed greenstone, associated with the boulder. When I subsequently visited the spot, the Chalk-rock had not been so widely disturbed but that I was enabled to observe what offers a direct corroboration of the previous statement. The large boulder had left a clean and distinct cast of a part of its rounded surface in the compact Chalk. Some of the larger fragments of greenstone according to the description of the pitmen, “had been stuck about it, and over it ;” but on looking closely, I saw that there was a mass of sand extending from the level of the cast of the boulder and beneath the solid chalk. Instead of removing the sand, I got the 1857. ] GODWIN-AUSTEN—BOULDER IN CHALK. 257 workmen to raise off the chalk with a pick: in doing this, some of the sand separated with the raised chalk ; but the principal portion remained, and showed that at one part it had been in close juxta- position with the block, and that it ended abruptly in the chalk at the opposite end of its mass; in this sand there was a fragment of greenstone much decomposed, and which has since fallen to pieces. From the account of the workmen, and from what I saw, as well as from the materials which have been preserved, it is clear that, together with the larger granitic boulder, there was also a collection of blocks of smaller dimensions; and all these were also water-worn. Most of them were composed of a peculiar and very different rock, consisting of augite, with tabular double crystals of felspar, such as might be called a melaphyre or porphyritic augite: the largest of these, from the portions which remain, must have been of consider- able size, weighing as much as twenty to twenty-five pounds, but, in common with all the other specimens of the same rock, it was much decomposed ; there was a central portion which was only partially so, and from which the compact specimens now exhibited were derived: the smaller pebbles were wholly decomposed, and readily fell to pieces, forming a sharp sand. Most of the loose material lying on the floor of the quarry, where the blocks had been broken up, consisted of this decomposed greenstone, but which, from the iron in the original rock, was of a browner colour, and had not been derived from the larger granitic boulder. In the specimen of greenstone from this spot, which I myself found, it was clear that the process of decomposition, with respect to these fragments, had been subsequent to inclusion, as, in their decomposed condition, they could not have been rounded as we there found them. In addition to these large portions of rock, there was also a com- pact mass of siliceous sand. Some of this had been thrown aside as of no interest ; but a portion was still 2 s¢¢u, and included a small de- composed fragment of greenstone: when the sand was broken down, this last so fell to pieces and mixed itself with it, that it was natural that a casual observer should have supposed, first, that these crystal- line rocks were all alike in composition, or granitic, and, next, that the finer materials were only its decomposed portions. An examination of this portion of the mass of materials will be sufficient to establish that it is fine water-worn beach-sand, derived from the waste of a coast-line of some crystalline rocks. Observations and Inferences.—Referring to the whole suite of smaller rock-specimens from the White Chalk which have been met with from all quarters, we may determine thus far, that, in respect of form or condition they have this in common with the larger speci- mens from Purley, they are all water-worn, either in the form of shingle or rounded boulders,—that, as regards their mineral cha- racter, they have been derwed largely from granitic and greenstone masses ; whilst they differ in this, that they have occurred as zsolated blocks or pebbles*, with the exception of those of Houghton (Sussex), where they were met with scattered over the same level or sea-floor, * M. Deslongchamps, of Caen, pointed out many years since, that modern Cro- codiles are in the habit of swallowing pebbles ; and he suggested that certain 258 PROCEEDINGS OF THE GEOLOGICAL sociEty. | Dec. 16, These several considerations have distinct bearings. The marginal sea-belt is under all circumstances both well-defined and distinctly marked. It commences from the lowest range of wave-oscillation, where that meets the line of sea-bed, and extends upwards to the utmost reach of breakers at high water. The power exerted over this space commences at the point where the wave becomes one of translation, and increases progressively to where it breaks ; from this its moving power decreases, being that only which is exerted by the upper portion of the wave as it is dashed forward. In all seas, therefore, the breadth of this zone will be primarily dependent on the slope of the sea-bed, and next on the range of the local tides. The amount of power thus exerted is very variable; and it is applied under very different combinations of the foregoing conditions ; so that it happens that the materials of the marginal zone are unceasingly being transferred one way or another upwards and outwards, at intervals corresponding to those when the forces are brought to bear in those directions. It is in this way that in tidal seas we have two distinct divisions of the marginal zone,—an upper, which is constantly disturbed, and composed of clean shingle ; a lower, consisting of like materials as to size, and which is only occasionally broken up. In the intervals the constituents of this lower marginal zone become covered with its characteristic animals and plants. The conditions under which portions of the submarginal zone are transferred upwards, though variable, are yet to be easily observed from any part of a coast-line. On our own shores abundant materials will always be met with in the upper track, which bear marks about them of having belonged for some previous time to the submarginal zone. These marks or characters have a bearing on the history of some of the pebbles found in the Chalk. To this zone belongs the great belt of marine vegetation which attaches itself to the shingle and gravel, as also do certain species of Balanus, Serpula, Anomia, and small Oysters; and such pebbles, even long after they have been washed up ae the lower to the higher zone, retain the traces or some remains of these incrusting forms. Of the smaller specimens of shingle which have been taken from the White Chalk, some are in the condition of clean pebbles, whilst others have still adhering to them some portions of such shells. So far as the evidences of the zone of origin of all the extraneous materials of the Chalk can be indicated from such characters as we have here been considering, we may feei sure that they all have belonged to the upper marginal zone,—that, though in some cases they may have travelled down, and found a temporary resting-place in the submarginal region, yet their subsequent place was at the upper level, before they started away to find their ultimate position in the deposits of calcareous mud. Ordinary wave-disturbance along the marginal sea-line cannot dis- smoothly rounded stones, which are occasionally found in the fine-grained oolitic strata of Normandy, may have been voided by Crocodilians of that period. I am indebted to Mr. Bowerbank for the information that Sharks also swallow small stones ; hence another agency by which the shingle of the White Chalk period An! have been transferred to areas of deep sea. 4897.] | GODWIN-AUSTEN— BOULDER IN CHALK. 299 perse the coarser materials of that zone beyond the limits of depth which have been here indicated. Parr IT. Mode of deposit, extent, and nature of the Fossils of the White Chalk.—It next remains that we should consider what are the con- ditions which are indicated by the White Chalk. Two naturalists lately lost to us, and both well fitted to give an opinion on such a subject — A. d’Orbigny and E. Forbes, have said that the pure White Chalk must have been the deposit of a deep and open sea. Apart from the evidence to be derived from its included animal remains, there is also that of its mineral composition, dependent on the specific gravity of its component particles, and which shows that it belongs to the extreme outward zone of distri- bution, as compared with the sand-zones, or those of ooze or mud. In these fine sedimentary beds, and in the isolated blocks and shingle which they occasionally include, we have the two terms of the series of mechanical products of all seas and of all periods, namely the abyssal and the marginal ; and from the presence of these two we may feel assured of the co-existence of every other intermediate form of sea-bed. The White Chalk had its equivalents of mud-depths and sand-zones ; and its own remarkable extent as a deposit is due solely to the peculiar condition of the ocean of that time, which furnished so much calcareous material for abrasion and removal. Systematic geologists have been so disposed to describe the White Chalk as an independent portion of the cretaceous series, that the occurrence of these extraneous materials is of as much use in showing that it is merely one subordinate member of an assemblage of marine deposits, as the materials themselves are in indicating the physical and geo- graphical arrangements of that remote period. The area over which that uniform deposit of pure calcareous matter known as chalk was deposited may be accurately defined. It will be unnecessary to follow it over the whole of its extent ; but in Western Europe it included the south-eastern half of Britain—from Devonshire to Yorkshire as far as a line much in advance of the present chalk-escarpment. In Denmark it occurs in Lelland and Moen, whence it trends south-east, across Prussia and Northern Russia. In France the area of true White Chalk extends south from Cal- vados to the Loire, and from the whole of the Paris Basin eastwards; in Belgium it appears under precisely the same characters asin France and England. Beyond this area, the deposits which were synchro- nous with the White Chalk put on other mineral characters. In every sea or ocean the zones of sedimentary deposit hold a general parallelism to one another, so that if the form or direction of one can be ascertained, that of the rest necessarily follows. It is by the evidence of the included fauna that we are certified that dis- tricts surrounding the area which we have here defined were its equi- valents in the Cretaceous series. For the present, the form of the area of deep and open sea deposits during the period of the Upper Cretaceous series may be taken as here drawn. 260 PROCEEDINGS OF THE GEOLOGICAL SOciIETY. [Dec. 16, The period of the Upper Chalk and its equivalents corresponds to that of the greatest extension of the area of the cretaceous sea or ocean; and the only means we have by which to define the extreme boundary-line of this area is by following out the gradation of sea- bed in the direction in which it passes into sands and coarser accu- mulation, but preserving at the same time its characteristic fauna. Marginal beds of this age occur on the southern portion of Norway and Sweden. In Westphalia and Rhenish Prussia, sands are the equivalents of White Chalk. On the west of the European area the cretaceous strata of Valognes, though composed of sand and siliceous conglomerate or shingle, are yet Upper Chalk. Such is also the case with the sands of the West of England, which form the extreme limit of the cretaceous series about the Bovey Valley. In this way not only the form and extent of the cretaceous ocean in its greatest range, but also the character and composition of its coast-line, can be determined with approximate certainty, for a given number of points. Belemnitella mucronata, which makes its first appearance in our Upper White Chalk, marks the equivalent of the White Chalk in other places, whatever the mineral composition of the beds may be. I have elsewhere shown * what was the extent of that first portion of the cretaceous sea which gradually extended itself from the Medi- terranean area, across France, or what. is now part of the south-east of England. From this first stage, the history of the cretaceous for- mation consists of a progressive increase of area in water, together with a change in time of its inhabitants or fauna; so that, over the whole of the cretaceous area, the lowest beds show littoral or shallow- water conditions, both mechanically and zoologically : and what is known as the grouping of forms characteristic of the great subdivi- sions of the formation disappears when the marginal beds are carried out to their widest range or limit, and holds good only for the central portions of the area, where the series of depositions represents both the changes which are due to the successive conditions of depth as well as those which animal forms exhibit in time, and where conse- sequently the results of these changes are presented in order of superposition. In this way it happens that the assemblage which figures in our lists as the fauna of the White Chalk is truly that of the upper or newest cretaceous period,—but in part only, and is not characteristic of those marine conditions of which that deposit is the result. The remains met with in the pure White Chalk area belong for the most part toa much higher sea-zone. This view of the character of the remains met with im the Chalk must have often suggested itself to naturalists who may themselves have collected from that forma- tion. Thus the stony remains of the Anthozoa have all been broken off at the base, and are without any support in the beds in which they occur. The Bryozoa belong to a condition of sea-water very different from that of those calcareous mud-beds. The Echinoderms show characters of having undergone decomposition. Again, the most common and characteristic forms of the White Chalk are frag- * Quart. Journ. Geol. Soc. vol. xii. p. 68. | 1857. | GODWIN-AUSTEN—BOULDER 1N CHALK. 261 mentary, as regards the Testacea more particularly ; and taken alto- gether they imply a drifting power, whereas the nature of the sea- beds indicates only conditions of tranquil deposition. Recognizable forms from the Chalk bear so small a proportion to its mass—the formation nowhere throughout its vast thickness presents old sea- floors over which a fauna lived *—that I am disposed to consider the greater part of the animal remains which it contains as having been raised off shallower zones, floated away, and scattered outwards over the deeper ones. This view of the Chalk-deposit—namely, that all the larger materials which it contains, whether organic or inorganic, belong to a higher sea-zone—is one which admits of a great amount of illus- tration, and deserves separate treatment. It may be sufficient for the purpose for which the view is here imtroduced, to state that all those forms of Bryozoa which, when living, are fixed at the base ° ‘only, such as Idmonea, Pustulopora, Desmeopora, and many others, all occur detached in the body of the Chalk. This is also well seen with respect to the Anthozoa: the examination of a large collection of Monocarya centralis showed me that they all had been broken off before they were imbedded. With respect to the zone from which the Chalk forms have been mainly derived, it is sufficient that it should have been a higher one, where the accumulation of mineral matter was necessarily very dif- ferent to what it was at extreme depths. I will therefore only call attention to a few Chalk forms, and which also belong to sand- deposits usually considered older than the Chalk :— Stellaster elegans, Forbes. In Chalk. Sussex. In sands below the Chalk at Folkestone, and in the sands of Blackdown. Serpula plexus. Chalk, and abundant in the Blackdown and Haldon sands. Pecten equicostatus. Chalk, and abundant in the Blackdown and Haldon sands. Plagiostoma parallelum. Greensand, Gault, Chalk. Considering the poorness of the White Chalk fauna, the proportion of bivalved Mollusca having a byssus is remarkable. Such shells are now widely distributed by floating weed. The occasional occurrence of large dead shells of Dolium or Cas- sidaria, of which a single specimen is as yet recorded from our White Chalk, requires for its explanation an agency at least equal to the transport of ordinary shingle. The species seems to be identical . with one from the cretaceous sands of Mans, where it is scarce. Dolium would not belong to such a zone; but the animal has the power of swimming by inflating its disk, and in this way it may occasionally be floated away from the marginal sea-line, and so perish, and sink in deeper water. The form Dolium evidently belongs to _ * The occurrence of a large block of Coral in the White Chalk caused me to form at one time a different opinion. I have now no doubt but that it was a transported mass from some distant reef. Proc. Geol. Soc. vol. iv. p. 169. 262 PROCEEDINGS OF THE GEOLOGICAL society. [ Dec. 16, the southern cretaceous fauna, as do also the fragments of Hippu- rite which have been found in the Chalk of Sussex and Kent. Means of transport of extraneous materials in the Cretaceous Sea.—The nature of the White Chalk formation, and the fact of the presence there of extraneous blocks and pebbles, lead naturally to the inquiry as to the agency by which they have been conveyed there. Most geologists will doubtless at once call to mind the account which Mr. Darwin* has given of a rounded block of greenstone which he found on the outer coast of a small atoll belonging to the Keeling group. The Keeling Islands are 600 miles from the nearest land (Sumatra) ; they consist wholly of coral-formation, and Mr. Darwin came to the conclusion that the block (which was rather larger than a man’s head) had become entangled in the roots of a tree which had been washed into the sea, floated ‘thus far, and finally liberated on the beach where it was found. If only one single block could have been conveyed thus far by such an agent, much more similar material must have been dropped and lost than ever reached so remote a coast-lme. The sedimentary deposits of open oceans, such as the Indian or Pacific, where so many of the lines exposed to coast-abrasion consist of coral-formation, must be identical in composition with our White Chalk, so that the rocks which are being conveyed away from the mainlands of those seas may be presented at some future time under precisely the same conditions as the extraneous materials now are in our Chalk: the correspondence between the two cases is so close, that it is difficult to avoid the consequence, that one case explains the other, and is evidence of like agency at very distant times. Mr. Darwin’s Keeling observations would fully account for the presence of all the extraneous materials which have been met with in the White Chalk and other deep-sea sediments up to the time of the Purley discovery. The peculiarities of this case are these:—-Apart from the large boulder there was a smaller one, weighing upwards of twenty pounds, some coarse shingle, and a quantity of loose sea-sand ; and these had all sunk down together without separating: for this they must have been firmly held together, both during the time they were being floated away, as also whilst falling from the surface to the depths of the cretaceous sea. If we suppose, in the case we are now considering, that all the coarser materials were so firmly bound up in the knitted roots of some tree which which had grown on a sea-margin, as afterwards to be carried about, until the tree became water-logged and sank, it is difficult to conceive how the finer sand should not have been washed out ; and, as wood is well preserved in chalk, we might expect that traces of the tree itself (and it must have been a considerable one) would have been discovered in immediate juxtaposition with these materials : such, however, was not the case}. * Journal, 1839, p. 549. t Fossil wood, and even lignite, has been found by Mr. Simmonds in the chalk of the neighbourhood. ; : : : | : { 1857. | GODWIN-AUSTEN—BOULDER IN CHALK. 263 The conditions which have to be satisfied in this particular case are, the removal of a large boulder, together with coast-line shingle and sand, and their transference to a deep and distant sea-bed, in precisely the same relative positions in which they lay together in the parent beach. Sir C. Lyell, who had his attention drawn to the fact of the oc- currence of pebbles in chalk by Mr. Catt, has adopted* the observa- tions of Mr. Darwin, in preference to such other means of transport as floating weed or floating ice. Sir Charles’s objection to the agency of floating ice is, that it is inconsistent with the conditions of climate indicated by a sea abounding in chambered Cephalopods. At all past periods the globe must have had its climatal zones ; and, taking Mollusca as our guides, we know that, for the secondary and tertiary periods at least, the order or gradation was placed very much as it is at present. We know, too, what is the distribution of the extinct Cephalopods over the European area; and on these joint grounds it may be stated confidently that no sure conclusion as to climate can be derived from the Ammonites and Belemnites of our secondary formations. For the Oolitic period (Lower Mesozoic) the geographical distribu- tion of Cephalopods is rather northern than southern, whilst for the Upper Mesozoic (or Cretaceous) they decrease, both as species and individuals, towards the upper chalk. Apart from these considerations, the fauna of a sea is no indication as to whether ice from polar regions may not occasionally be floated into it. All that is requisite is that the area of water should have an extension into polar regions; and then the liberated ice must at all times have been distributed according to the same laws as influence it now. Polar ice, it must be remembered, is now occasionally floated down, and its load scattered, as low as the Azores and Canaries, where its detritus becomes imbedded in deposits containing the forms of the South Lusitanian fauna. The condition of one hemisphere of our globe at the period of the greatest extension of the Cretaceous ocean, represented in the map - exhibited to the Meeting, shows—1st, how, as far back as the creta- ceous period, the waters of the great and old Atlantic valley extended into the Polar basin; and next, what was the extent and character of the subaérial surface, the coast of which supplied the mineral mate- rial for the sedimentary beds of those seas over the European area. I know only of two other agencies by which the coarse materials of the marginal sea-zone can be conveyed away so as to be distributed over the deeper sea-beds, viz. sea-plants and coast-line ice. Sea-plants being lighter than water, it happens that, when the sea- bed of the zone of Fuci or Laminarie is composed of loose materials, such as shingle, the mass of weed attached to small blocks or pebbles becomes buoyant enough to float them ; in this way, when the plants have attained their full growth, and gales of wind set in, the plants lift great quantities of deep shingle from off its bed, and carry it into the upper sea-line. With a gale and a falling tide, the weed may, in * See Manual, 5th ed. p. 243. 264 PROCEEDINGS OF THE GEOLOGICAL Society. [Dec. 16, like manner, convey marginal shingle outwards; but the transport in this direction is far less in amount than it is in the other. Such a process as this has been in operation at all geological periods ; and some years since I indicated it as the only one by which large detached valves of such shells as Oysters (Hxogyra gryphea) could have found their way into the fine sandy beds of the Lower Greensand formation. Sea-plants have their limits of growth ; and the bulk of each mass will be limited by the support or surface of attachment: conversely, therefore, there is a limit to the size and weight of the materials which can be lifted by such an agency. As far as my own observa- tions go, the floating power of large masses even of Bladder-fucus does not disturb shingle-stones weighing much above 1 lb. A good deal of the extraneous shingle from the White Chalk is undoubtedly under this weight, and so far therefore admits of being thus accounted for: but the agent becomes wholly inadequate when considered with reference to blocks of 12 and 14 lbs. weight, such as have occurred in Sussex; still less could any conceivable mass of sea-weed have ever carried the Purley boulder. But, even if it be assumed that sea-plants of that time could have lifted the largest boulder, and that a tangled mass of them could have floated away at the same time all the smaller stones associated with it, the difficulty as to the mass of loose sand still remains. Sea-plants, when detached from their proper zone, are constant agents in transferring the animal forms belonging to it, as well out- wards as upwards ; and it was in this way most probably that the White Chalk acquired the very peculiar assemblage which it contains. This agency, like that of floating trees, is not to be excluded with refer- ence to past times, and may possibly have been engaged in trans- porting some of the smaller pebbles, which are met with in beds into which they could not have been drifted. Naturalists, who are well aware how many forms are to be found amidst the roots of sea- plants when these are washed up to the marginal zone, will see that these must act as the distributors of the fauna of the same sea-zone when the plants are drifted away outwards. Masses of ice floating at sea have two distinct sources of origin ; and, as a consequence of this, they are also distinct in the external characters of the records they leave. The larger masses known as icebergs, which are the terminal portions of the glaciers of Polar regions, which have reached down to the sea, have been reported by a long list of observers to be laden with detritus: in this case the detritus is sub-aérial, and its form angular. Yet I have not seen a single angular fragment from the White Chalk, nor from any part of the Cretaceous series. There is another form of floating ice, in which, though it is far less imposing im respect of its mass, it is of infinitely greater power as a means of transport. This ice has its origin along the coast-lines of Polar lands ; it incorporates itself with all the materials of the beaches to which it is attached; it acquires increased buoyancy from the snow-ice which collects on its surface ; and, when the annual 1857.] GODWIN-AUSTEN—BOULDER IN CHALK. 265 period of the breaking up of the coast-ice arrives, great masses are drifted away, bearing with them in their under surfaces compact masses of frozen beach, which separates itself as the ice decays. We have only to imagine a case where a portion of such a floe, so laden, should have wasted as it travelled into warmer regions, so that it no longer retained sufficient buoyancy to float the mass of boulders, shingle, and detritus attached to it; and what remained would then sink together, and become buried in whatever the sub- stance of the sea-bed beneath the spot might happen to be. Geologists have long since become aware of the power of coast-line ice aS a moving agent: even in our climate and country its mode of action is exhibited ; it may be well seen every winter over the north- ern European area, whilst for its fullest powers, as displayed in high northern regions, we have graphic pictures in the narrative of Dr. Kane. I know of no other agent but that of coast-ice by which a mass of incoherent materials could have been held together, as a characteristic portion of a sea-beach, and so deposited at a vast distance from the nearest land. Such, I conclude, was the nature of the agency by which the assemblage discovered in the chalk at Purley was kept together and conveyed. Form and composition of the Land of the Cretaceous Period.— The upper Mesozoic group (cretaceous) in its northern expansion outspanned the limits of the lower Mesozoic (oolitic). We have abundant evidence that strata of Great Oolite and Oxford Clay entered into the coast-line of the Lower Greensand sea; but the materials carried into the area of the chalk-deposit have as yet consisted mainly, if not exclusively, of Crystalline and Paleozoic formations. Such was the character of the dry land which bounded the cre- taceous gulf or bay extending west from the Cotentin, across our south-eastern area, towards Sweden: It remains only to notice, and that most cursorily, the composition of those areas of land which existed as such at the time of the greatest extension of the Cretaceous ocean, and which continue as such at the present time. On the west the cretaceous strata of Noirmoutier indicate littoral conditions, as also do those of Aix (oolitic) or Charente Inférieure. Such is the case also with respect to the sands, shingle-beds, and calcareous strata of the Cotentin. The intervening country between these two localities, which forms the western district of France, consists of gneissic and granitic rocks, with old sedimentary slates and sandstones (quartzite). The west of England is similarly composed. We may place the whole of the area between these two adjoining peninsulas in the condition of land-surface at the end of the Cretaceous period, and may extend this old land far into the present Atlantic area. The small outlier of Cretaceous sand near Bideford shows that the Cretaceous sea must have had an extension considerably to the west of its present limits. The course ofthe outline of this sea across our island may be passed over for the present, as the extraneous materials in the White Chalk do not resemble any of the crystalline rocks of our series. In the south of Sweden, on the contrary, the cretaceous beds 266 PROCEEDINGS OF THE GEOLOGICAL society. | Dec. 16, along a line drawn from Engelholm on the west, to Karlskrona on the east, rest on granite, gneiss, claystone-porphyry, and old sedimentary slates and sandstones. It perhaps may be thought by some that, by the aid of such a col- lection of extraneous materials as has been now brought together, it would have been easy to have determined almost with certainty the precise portions of the old cretaceous coast-line from which they had been derived ; such, however, at present is not the case. M. Brongniart has noticed the very great resemblance which exists between the crystalline rocks of the Cotentin and Scandinavia ; and either district could have furnished the large block of quartzite now in Mr. Catt’s collection. On the whole, however, and guided mainly by the peculiar greenstone-porphyry, and the condition of the large boulder from Purley, from which the mica has been removed, as it has from great masses of a Scandinavian granite, I am disposed to look to that quarter as the source of the extraneous materials of our Chalk-formation. } There is a difficulty, however, which I feel will suggest itself to some, with respect to the agency.of floating ice in transporting the materials imbedded at Purley: it may be asked whether in such case we should not long since have become familiarized with the opera- tions of such an agent with reference to the Chalk-period, seeing the extent to which that formation is quarried. Such an objection is in part negative only: much evidence akin to that at Purley may have presented itself, and yet not have been noticed. But, even should the assemblage met with at Purley be the first of its kind that has ever been met with till now, we may feel sure that thousands of like cases are concealed in the mass of the Chalk, from the incalculable im- probability which exists that the Purley phenomenon should be the only one of its kind throughout the formation. It is only with refer- ence to such mixed assemblages of boulders, shingle, and sand, that the agency of ice is required. The physical arrangement of the circumjacent portions of the earth’s surface at the Cretaceous period preclude the idea that floating coast-ice could have been either a constant or a very powerful agent of transport with reference to the White-chalk area of Europe. The line of coast, from which it has been suggested that the Croydon boulder was derived, lay a little to S. of the 60° of north latitude ; and, though coast-ice is a powerful agent there at present, the inten- sity of cold must have been modified then by the expanse of sea that lay immediately to the south. The requisite degree of cold need not have been greater than what has occasionally been experienced on our own eastern coast, when ice has lifted and floated away far greater weights. Many general results will some day be arrived at from the study of the extraneous mineral materials of our old oceanic deposits ; by their means we shall certainly arrive at a definite outline for the ocean of the Cretaceous period. 1857.] | HUXLEY—CEPHALASPIS AND PTERASPIS. 267 JANUARY 6, 1858. The Rev. Arthur W. Ingram, M.A., Hawington, and Timothy Curley, Esq., Hereford, were elected Fellows. The following communications were read :— 1. On Cepuaraspis and Preraspis. By Tuomas H. Hux ey, F.R.S., F.G.8., Professor of Natural History, Government School of Mines. [Plates XIV. XV.] Tue genus Cephalaspis (Agassiz) was originally established to in- clude four species of Devonian fishes,—C. Lyellu, C. rostratus, C. Lloydii, and C. Lewisit ; but the differences between the first and the last of these species were so great, that the founder of the genus himself suggested the probability of their future separation. The two groups of species are said by Prof. Agassiz to be con- trasted not only by their forms, but also by their minute structure. In regard to form, the cephalic disc of Cephalaspis Lyelli is stated to possess an almost semicircular anterior outline, while its postero- lateral angles are greatly prolonged backwards. The middle part of the occipital region, Prof. Agassiz adds, is cut off almost square (coupée presque carrément). As regards this last point, however, my own observations are at variance with his description. Several specimens in the museum of this Society show that the middle of the occipital margin is not truncated, but is greatly produced backwards, the margins of the produced portion being concave. ‘The same peculiarity is clearly distinguishable in the specimen of C. Lyelli now in the British Museum, and figured by M. Agassiz, pl. 1. a. 2: mdeed the artist has faithfully depicted the real contour of the occipital margin in the figure cited. The well-known occipital spine is supported by this produced portion of the disk. The discoid bodies, corresponding to all appearance with the cephalic dise of C. Lyell, wpon which alone the species C. Lewisiz and Lloydii were established, differ widely from C. Lyellu, beg oval in contour and not prolonged into postero-lateral cornua. The structural differences observable in the disk of C. Lyell on the one hand, and of C. Lewisti and Lloydii on the other, are thus stated by Prof. Agassiz :— “In C. Lyell the head is covered with a pavement of polygonal plates, altogether similar to that which covers the head of Ostracion. Each plate is convex in the centre, and is marked by radiating grooves ending at the margin in denticulations, by which the scales interlock. _ These scales appear to be osseous and to have their external surface enamelled. At the circumference of the disk they become con- founded together, and the enamel presents wrinkles parallel to the edge.” Elsewhere these plates are said to be “true scales juxta- posed.” In the ‘ Recherches,’ M. Agassiz describes ‘‘ fibrous bones of the VOL. XIV.—PART I. Tt 268 PROCEEDINGS OF THE GEOLOGICAL society. [Jan. 6, | head’ under the “scales,” and he particularly mentions and figures the radiating direction of these “‘ fibres ;”’ but in the ‘ Monograph of the Old Red Sandstone Fishes’ I find the following general remarks applied to the whole of the Cephalaspide :— «It would appear from the condition of the specimens preserved, that all the cranial bones were only protecting plates, which covered ‘ a cartilaginous cranium similar to that of the Sturgeons ; at least I have never been able to discover any cranial bones deprived of that characteristic granulation, which indicates that the plates were ~ in direct relation with the integument. Therefore, I think there can be no doubt that all these granular plates rested by their inner and smooth surface on a cranial cartilage, such as is found in cartilaginous _ fishes and in the embryos of osseous fishes.”,-—Monog. Grés Rouge, p- 3. Nevertheless, in speaking of the genus Cephalaspis, a few pages further on, Prof. Agassiz states that he has nothing to add to his previous account of the genus; so that I am puzzled to know what view I ought to ascribe to him at present. We shall see by-and- by that the last-quoted is the only one warranted by the facts of the case. The disk of Cephalaspis Lloydii is said to consist of an external striated enamel, of a middle layer “ composed of granules similar to those of the bones of Chondropterygious fishes,” and of an internal layer made up of superimposed lamelle. Prof. Agassiz considers that this structure “‘ singularly recalls that of the test of the Crustacea.” Notwithstanding these, partly real and partly imaginary, differences — between his different species of Cephalaspis, Prof. Agassiz found in Cephalaspis rostratus (a species which I have had no opportunity of observing) a form and structure of so transitional a character that he included them all under the same genus. That so close an affinity obtains between all the species of Cepha- laspis has, however, been disputed latterly by M. Rudolph Kner, who in 1847 published a memoir in Haidinger’s ‘ Naturwissenschaft- liche Abhandlungen’ for the purpose of proving that C. Lloydi and C. Lewisii are not piscine remains at all, but that they are the internal shells of a Cephalopod allied to Sepia, for which he pro- posed the name of Péeraspis. M. Kner’s reasoning is based upon his examination of the structure of a fossil (evidently closely allied to C. Lioydii) from the Silurian rocks of Gallicia. The form of this fossil, says M. Kner, is very similar to that of C. Lloydit ; but it is larger, having a length of about four inches by a width of two. It consists of three layers. The innermost is shining, bluish-green, enamel-like, and presents four or five distinct lamelle. This layer forms one continuous surface marked in the centre by a longitudinal depression, smaller at one end than at the other, and by obscure radiating lines. The upper part of the conical depression is covered with minute pores or depressions, which are visible in the deeper as well as in the more superficial layers, but become evanescent in its lower part. Between the layer of enamel and the prismatic layer which 1858. ] HUXLEY—CEPHALASPIS AND PTERASPIS. 269 succeeds it, there lies a thin dull layer, in some places of a brownish colour. This is followed by an excessively delicate lamina of enamel which lies upon the prisms. The layer of prisms is one line thick, and in section presents a number of more or less hexagonal disks. The enamel passes for a short distance between the prisms. Externally the prisms lie on a © granular layer, to which the outermost very delicate ‘ epidermic ”’ lamina marked with parallel striz succeeds. M. Kner asserts (supporting his statement by the authority of Heckel) that in no known fish does any such epidermic or prismatic layer exist, and assuredly no such continuous internal enamel-layer, as in the fossil; and he then proceeds to compare the latter with the cuttle-bone. M. Kner would hardly have published his views, had he sub- jected his sections to a more minute and careful microscopical exami- nation. But, even apart from the characteristically piscine structure of these disks, very strong objections suggest themselves. In fact, to get at any sort of resemblance, M. Kner has to compare the outer layer of the fossil with the inner of the cuttle-bone, and vice versd ; and even the superficial resemblance in the striation of the two bodies is anything but close. In Dunker and Von Meyer’s ‘Paleeontographica’ (B.iv. H.3.1855) Roemer gives an account of a fossil, which he refers to the Sepiade, under the name of Paleoteuthis. Whether this body is or is not a Cephalopod, is a point I will not enter upon here ; but Roemer in referring to Kner’s Memoir, expresses the opinion that the Pteras- pides are Crustacea. Mr. Salter and myself described two new species of Cephalaspide allied to C. Lloydii (Ag.), in a note* appended to a paper read before this Society by Mr. Banks, in December 1855. Without acceding to Kner’s views respecting the zoological affinities of such Cephalae- pids, we adopted his name. The facts to be detailed in the present paper will, I believe, fully justify this step ; and I shall hereafter speak of C. Lloydii and its allies under the generic name of Pteraspis. ' Professor Pander+ has recently described two Silurian species of Cephalaspis (C.verrucosus and C. Schrenckii) both trom Rootsikille. The former somewhat resembles C. ornatus (Egerton), having a highly ornamented and tuberculated upper surface. In the broad tuberculated antero-dorsal plates, separated from the head by a suture, it foreshadows Auchenaspis, Eg. C. Schrenckit has hexagonal orna- mented plates upon its disk. Professor Pander appears to think that the margins of the disk re- present jaws, being led to this conclusion, apparently, by their produc- tion into short quadrate serrations, which he regards as teeth. Sections of these “‘jaws”’ and ‘“‘teeth,’” examined microscopically, exhibited “a homogeneous base, in which clear and dark cells of the most various forms—rounded, elongated, and angular, with fine radiating branches, lay scattered, and were frequently disposed in concentric * Quart. Journ. Geol. Soc. vol. xii. p. 100. + Monographie der fossilen Fische des Silurischen Systems. 1856. TZ ek 270 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 6, layers, where a tubercle rose above the general surface. Although they have not the same regular form as ordinary bone-lacuneze (such as occur in Pterichthys and Coccosteus), yet they can hardly be called by any other name. The very thin narrow teeth, closely united with the margins of the jaws, and coalescent with them, have a porous basis, and shining, broad, sharp upper and lateral edges. If both surfaces are carefully rubbed down, the basis is seen to consist for the most part of a homogeneous transparent mass, full of small dark cells, from which the very fine tubuli radiate in all directions, branch out, unite with the neighbouring ones, and by their many anasto- moses form a most complex network. Towards the shining surface, as well as anteriorly and posteriorly—at least, certainly, towards one sur- face—the cells cease ; the tubuli, winding irregularly in the base, take a straight course, and ascend apparently with an enlarged diameter, without convolutions and rarely branching, towards the external sharp angle.” (/. c. p. 46.) Lam not aware of the existence of any other account of the minute structure of Cephalaspis and Pteraspis beyond these; and I will therefore now proceed to the immediate subject of this paper, which is, to describe that structure more fully and, I hope, more accurately than previous observers have done,—to compare Pteraspis and Cepha- laspis, pointing out their real differences and resemblances,—and finally to consider the bearing of the structural facts upon the ques- tion of the zoological position of these ancient fishes. CrepHaxaspis. (Pl. XIV.) In but few of the specimens of Cephalaspis Lyellii which I have i had the opportunity of observing, has the external surface of the ce- phalic shield been well exhibited, or preserved over any considerable surface. Where best shown it is somewhat uneven, and presents that curious apparent division into polygonal (usually hexagonal) areze which has been described by Professor Agassiz. On examining the apparent sutures closely, however, they have not presented to my ob- servation precisely the appearance figured in the pl. 16. fig. 2. of the ‘Recherches.’ They appear rather as if short, delicate, reddish- © brown lines had been ruled across the line of junction of the sides of the hexagons, for some way towards the centre of each hexagon; and these lines are so gently convergent as to seem nearly parallel. Neither do I remember to have met with such strongly marked cen- tral elevations as those represented in the figure cited. The inner surface of the disk has presented itself well preserved in more than one specimen. It never exhibits any trace of the apparent sutures of the outer surface (compare Agassiz’s ‘Recherches,’ pl. 1 4. fig. 3, where this fact is clearly shown), but appears whitish, enamel- like, and very smooth where it is not furrowed by certain shallow and narrow depressions which radiate from the region of the orbits and occiput. towards the margin, before reaching which they repeatedly subdivide and anastomose. I do not doubt that these are the impressions of the vessels which ramified under the disk during life. Sometimes, by the elevation of the substance of the disk into'a 1858. ] HUXLEY—CEPHALASPIS AND PTERASPIS. 271 wall on each side of one of these depressions, the latter may become almost converted into a canal, so as to retain a portion of the matrix. This however is a rare occurrence. When the concave inner surface of a disk and the convex cast of another specimen are compared, it is at once seen that the “ radiating fibres” of the one correspond with the grooves and furrows of the other. The surface of the cast is remarkably darker than the sur- rounding matrix, and might not unreasonably at first be supposed to be of a different nature. When the inner surface of the disk is carefully examined with a magnifying glass, a number of reddish- brown minute dots appear scattered irregularly over its surface. It will be seen immediately that these are the internal openings of vas- cular canals which enter the substance of the disk. If a vertical section of the cephalic shield of Cephalaspis Lyellii is carried through the orbits and perpendicularly to the axis of the body, it will be seen that the disk is exceedingly thin, hardly anywhere attaining =4,th of an inch in thickness, except at the margins and the spine, which are thicker. At the lateral margin the thin lamella is bent abruptly and aimost horizontally inwards for about a quarter of an inch. It then suddenly thins so much as to be little more than a flexible membrane, which in the specimen now under description is pressed up into close proximity with the dorsal part of the shield (fig. 4). the thinness and fragility of the disk of Cephalaspis render it difficult to obtain good sections for microscopical examination. The best I have seen (Pl. XIV. fig. 1.) is taken at an angle of about 45° ' ‘to the longitudinal axis of the head, and intersects the occipital spine just beyond its origm. The section of the spine is in the best con- dition, and may be described first. It is about th of an inch thick in its thickest part, which corre- sponds with the median ridge of the spine, and presents three regions or layers, distinguishable from one another partly by their minute structure, and partly by the different mode of distribution of the vas- . cular canals by which the tissue is permeated m each. The inner- most or deep layer (d) is made up of superimposed lamelle not more than 5,),,;th of an inch thick, each of which sometimes ap- peared to be still more finely laminated. Interspersed among these, at greater or less distances, are numerous osseous lacunze, whose long axes are parallel with the planes of the laminee (fig.3). The length of these lacunz varies greatly, but may be taken at ,),;th of an inch on the average ; some, however, are twice or three times this length, while others are much less. The transverse diameter is equally variable; but none that I measured ex- ceeded =;1,;th of an inch in this direction. The form of the lacunz | is very irregular in consequence of the long branching and anasto- mosing canaliculi which are given off not only from their ends but from their sides. In some parts the innermost layer appears almost black when viewed by transmitted light, in consequence of the quan- tity of air retained in the multitudinous lacune and canaliculi. ; J.erge vascular canals, measuring from yjpth to zhpth of an inch | 272 PROCEEDINGS OF THE GEOLOGICAL SsOcIETy. ([Jan. 6, in diameter, whose inner openings correspond with the brown spots on the inner surface, traverse the innermost layer very obliquely, in their course towards the middle layer (fig. 1, e.) Their branches are few, and for the most part run parallel with the main trunk ; but they give off a great multitude of minute canaliculi, which anastomose with those of the nearest lacunz. Such of these canals as I have seen in section were oval, their long diameters being parallel with the planes of the lamelle. In the specimen described the walls of the canals are lined with a reddish matter (like oxide of iron); anda similar substance obstructs many of the canaliculi. The middle layer (c) is distinguished from the inner by the rarity or entire absence of the lacunze, and by the indistinctness of the lamination as compared with that of the deep layer. Such stria- tions of the nearly homogeneous base as seem to indicate lamination are, in the middle and inner parts of the middle layer, so disposed as to be nearly perpendicular to those of the deep layer, appearing to follow the course of the vascular canals. | The latter are continuous with the large vascular canals of the deep layer, but they are smaller and form a close network. Each of the large canals, on reaching the middle layer gives off several branches, which run nearly parallel with the surface (and there- fore greatly inclined to the course of the great canals), and anasto- mose with those around, above, and below them. In this particular part of the disk, in fact, a large canal gives off as many as three tiers of these lateral branches, separated from one another by not much more than their own diameter, and all ramifying and anastomosing with one another. These lateral vascular canals have at first a dia- meter of about z1)th of an inch; but many of their anastomotic branches are much smaller. Sooner or later all these branches appear to end in a close “‘ super- ficial network,” 6, which lies in the boundary between the middle and the superficial layers. The latter or third layer of the disk (a) . sometimes appears structureless, at others presents an obscure vertical striation, as if it were, like enamel, made up of minute fibres. The superficial vascular network sends into it a great number of minute short processes, which branch out abruptly at their ends, like a thorn- bush or a standard rose-tree, and end in excessively fine tubuli, like those of dentine. The tubuli appear empty and are much finer than the vascular processes, which are usually full of the dark red matter before referred to. Hence, when the section is viewed by transmitted light, the vascular canals are very distinct, and appear to end abruptly in the deep half of the superficial layer, while the tubuli have the aspect of fine, clear, sparsely ramified lines, by no means so readily visible. In some cases they seem to open on the surface. This substance, it will be observed, corresponds very closely in structure with the ‘‘cosmine”’ of Professor Williamson. I have been unable to find any trace of a ‘‘ ganoin”’ layer external to it. The superficial layer does not form a continuous whole, but is seen in the section to be divided mto masses of various length by inter- spaces or gaps, which extend as far as the superficial vascular net- 1858. | HUXLEY—CEPHALASPIS AND PTERASPIS. 273 work, the canals of which appear indeed to open into the bottom of the interspaces. _ A structure in every essential respect similar to that just described is to be found in all other completely ossified parts of the cephal!e shield, whether dorsal or ventral. In other regions of the dorsal part, however, the lamination of the inner layer is far more marked ; and as a general rule the middle layer in these parts of the shield is thinner and contains fewer layers of lateral vascular ramuscules. The like is true of the inner part of the ventral region, in which only a single layer of close-set vascular canals makes its appearance (Pl. XIV. fig. 5). The flexible part of the ventral layer appears to be composed of the lamellar inner layer only ; and the thick margins of the disk resemble the spine in structure. The structure of the ventral layer, enclosed as it is on both sides by the matrix, is usually very well displayed in sections, and the better, on account of the dark reddish-brown hue which is acquired by the matrix, for some little distance from its line of contact-with the ani- mal substance. But neither in these nor in any other sections can any trace of bony substance be discovered beyond that whic h enters into the composition of the thin cephalic shield itself. I believe, therefore, that the so-called “fibrous bone”’ is nothing but the sur- face of the matrix impressed by the inner surface of the disk, and stained ofa darker colour than elsewhere. If flakes of the inner layer of the shield be detached and well soaked in hot Canada balsam, they become transparent, and their structure is well displayed in a superficial view (fig. 3). At their broken edges, the lamellee of which they are composed are seen cropping out one beyond the other; but their most striking feature consists in the long lines of lacunze which lie in parallel and equidistant series in each layer, so that under a low power it appears to be composed of broad flat fibres arranged side by side. ‘The axes of the lacunz of each layer are directed nearly at right angles to those of the layers above and below, so that under a low power the section appears cross-hatched by a series of dark lines. The great vascular canals are well seen traversing the successive lamellee very obliquely. In flakes of the disk similarly treated, but containing more of the middle and outer layers, fig. 2, it is obvious that the great canals divide into the branches of the middle layer which have already been seen in the vertical section, chiefly, if not only, along lines corresponding with the apparent sutures between the so-called “ polygonal scales.” The canals of the middle layer are very singularly arranged, passing from their origin, across these sutural lines and nearly parallel with one another, towards the centre of the adjacent “‘scales.’’ The appearance of distinct “scales,” and of the curious lines along their boundaries, is entirely due to this vascular distribution, the canals with their reddish lining showing very distinctly against the whitish general substance. In these views, again, the fissures by which the superficial layer is interrupted in the sectional view are seen to be nothing more than the expression of the valleys between the irregular and inconspicuoug tubercles into which the superficial layer is raised (Pl. XIV. fig. 2). 274 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 6, Preraspris. (Pl. XV.) A fragmentary specimen of Pteraspis Banksii (belonging to Mr. Marston) affords by far the best view I have yet met with of the general structure of the shield of this genus. A cast of the outer surface is exhibited, and for the greater part of its extent the sub- stance of the shield is absent ; but in the centre a patch is left, ex- hibiting all the layers in their natural condition and relations (fig. 2). The innermost layer (d@) is composed of a reddish-white nacreous substance, exhibiting a distinct appearance of lamination at its free edges: its surface is somewhat uneven, and presents scattered rounded apertures about z},th of an inch in diameter. The edges of these apertures were not unfrequently somewhat raised ; and their cavities were full of a reddish matter. External to the innermost layer is the middle layer (c), composed of vertical plates of a laminated substance of similar appearance to the inner layer, and varying in thickness from ztjth of an inch downwards. These plates are so disposed as to form a network, oe polygonal (4—5—6-sided) cells of an average diameter of about =,th of an inch. The inner ppd aces of these cells are closed by the inner layer. Externally, they are also closed by a substance of the same nature as their walls, but perforated by a variable number of apertures some- what smaller than those in the inner layer (6). The inner surface of this substance presents in many cases a striation more or less parallel to the sides of these apertures ; and when it is broken away the thickness of the layer which closes the outer apertures of the cells is seen to be permeated by numerous small canals which give it a sort of worm-eaten or reticulated appearance. I will call this the “reticular layer.” Lastly, outside the reticular layer is a white substance, very imperfectly visible in this specimen, in which no canals are visible, and which constitutes the external layer (a). A view, the precise complement of that just described, is afforded by another of Mr. Marston’s specimens of Pt. Banksi. This ex- hibits, for the most part, a cast of the mternal surface ; but towards the edge a considerable portion of the shield is left in a very perfect state of preservation, and with its external surface intact. The external layer is produced into strong ridges, the summits of which are turned outwards and their bases juxtaposed. The summits of the ridges are as much as;4,th to;7;th of an mch apart. In some cases they were sharply angular, in others more rounded. Where this layer was broken away, the reticular layer beneath it, and the polygonal cells of the next layer were well displayed. The bottoms of these cells were seen to be closed by the inner layer, and in this apertures were visible, corresponding with those on its inner surface. I have not examined transverse sections of this species; but the structure of Pt. Lloydiiis so similar, that its transverse section perfectly elucidates the appearances presented by P. Banksi. | I have seen no specimen exhibiting the unaltered externa! surface of Pt. Lloydi ; but its internal surface and its other layers, where the inner one is broken away, are well displayed in two specimens belong- 1858. | HUXLEY—CEPHALASPIS AND PTERASPIS. 279 ing to the Geological Society. The inner layer is thin, whitish, and nacreous, and presents, scattered over its surface, apertures of a similar character and size to those shown by Pt. Banksit. The next layer appears, at first, to be very different, inasmuch as it seems to be composed of irregular reddish prisms with white inter- spaces. The prisms have a diameter of -,th of an inch, more or less. The reticular layer is hardly distinguishable in this view ; but when the apparently prismatic substance is broken away, either a thin filmy outer substance is visible, or a peculiar striation. A thin sec- tion of the shield of Pt. Lloydii (fig. 1), taken perpendicularly both to its plane and to its long axis, exhibits the followimg appearances when viewed with a low power by reflected light.' The total thickness of the section is about -),th of an inch, and of this amount about ;4+,th of an inch is occupied by the inner layer, rtoth of an inch by the second layer, 4th of an inch by the next, and s4,th by the outermost layer. The outer layer (a) appears to consist of a series of papillary eleva- tions which have a broad free end, and are attached by narrow bases, so that a triangular interspace with its apex outwards is left between every pair of elevations. The matrix filling these interspaces, and for some distance in the immediate vicinity of the outer surface, is much darker than elsewhere, and has a deep brown hue. The attached ends of the elevations pass into a whitish substance, which, under this power, looks similar to their own. Itis traversed by many reddish canals, which send diverticula into the elevations (6) ; and hence this substance clearly represents the “reticular layer”’ of P¢. Banksit. At intervals of about =4;th to ;45th of an inch or thereabouts, thin septi- form processes are given off from the reticular layer, and pass perpen- dicularly inwards to the inner layer ; they thus subdivide the second layer into a series of irregularly quadrate spaces, corresponding with the prisms seen in the superficial view. The inner layer is, like the rest, whitish, and is traversed parallel with its surface by four or five much whiter streaks, so that it appears to be composed of only a corresponding number of lamelle ; but on allowing the light to pass through the section, it is at once obvious that each of these apparent lamelle is in reality made up of many of the primitive laminze which constitute the inner layer, and that the bright and dull white streaks are due entirely to a difference of texture or composition in the successive groups of lamine. Under a high power the laminz are seen to have a thickness of about =,';pth of an inch, and to run nearly parallel with, and closely applied to, one another. They present an indistinct vertical striation, but exhibit no canals nor lacunze. The septa of the second layer are composed of similar laminz, but less distinct, and curved in various directions, usually more or less parallel to the walls of the large cavities which they bound. A fragment of the inner layer (fig.4), rendered transparent by Canada balsam, and viewed by transmitted light, shows that it contains no lacune ; nor have I been able to detect any di- stinct structure in its lamine, unless an obscure and very delicate striation, visible here and there, may be regarded as such. 276: PROCEEDINGS OF THE GEOLOGICAL society. {[Jan. 6, A similar disposition of curved laminz can be traced in the “ re- ticular layer ;” but in the elevations of the external layer, such laminee are no longer distinctly visible, although here and there traces of them may be seen. Lach elevation, in fact, nearly resembles the tooth or dermal defence of a placoid fish. It contains a central cavity, commonly filled with a dark red matter, which usually occupies the centre of the basal half of the elevation and then suddenly ends in a number of excessively minute branches, which pass towards the surface, ramifying as they go, and closely resembling the canals of dentine or cosmine. ‘They appear to terminate on the surface, on which I have been unable to discover any trace of laminated struec- tureless ganoin. The central canals of the elevations open internally into the network of vascular canals which lies in the reticular layer. These canals rarely exceed 74,th to ,}>th of an inch in diameter, and they are rendered particularly obvious by the dark red granules with which their walls are dotted. Internally they open directly into the interspaces of the septa which connect the reticular with the inner layer, and the granules are con- tinued on to the walls of the septa, which are themselves occasionally traversed by short canals. The interspaces (e) are full of a more or less transparent inorganic matter, identical with that of the matrix. It follows, therefore, that the ‘‘ bony prisms” or ‘‘ granules” which have been described have no existence, these so-called prisms being nothing but the matrix which has filled up the cavities of the poly- gonal cells, visible im their natural empty condition in Pt. Banksii. Canals resembling those of the reticular layer, as I have said, traverse _ some of the septa and put their chambers in communication. In the section under description, the inner layer is for the most part devoid of canals; but one (/’) is exhibited very beautifully. It has in the middle a diameter of about s¢pth of an inch, but is wider at both ends, and traverses the inner layer almost perpendicularly. The lamine are bent outwards for a certain distance, where they impinge upon its walls. The structure just described is that of the central part of the section. At one of its ends, near the margin of the disk, the arrangement of the vascular channels is more like that in Cephalaspis,—the reticular layer assuming a much greater development, and the areolar character of the sinuses of the second layer becoming greatly obscured. On comparing together the appearance of a section with those pre- sented by the internal and external views of Pteraspis, there can be no doubt that the elevations of the outer layer of the one are the sections of the ridges of the other; and it is remarkable that there should be so striking a difference in the form of these ridges in Pé. Banksii and Pt. Lloydii. The ridges seen in concave casts probably always correspond with the whole interspaces between the ridges of the cuter layer in Pé. Banksii ; but it is quite conceivable that in Pt. Lioydii the ridges, in consequence of their peculiar form, might sometimes be held by the matrix and sometimes not ; so that at one time the ridges of the cast would be very narrow, corresponding only 1858.|) © HUXLEY—CEPHALASPIS AND PTERASPIS. Lie with the intervals between the summits of the ridges of the disk, some- times broad, and corresponding with the intervals between their bases. Comparison of PreRaspis and CEPHALASPIS. If the exposition which has just been given of the structure of Cephalaspis and Pteraspis be correct, it follows that neither the resemblances nor the differences in the structure of these two genera have hitherto been rightly apprehended. The sole important differences consist, Ist, in the absence of osseous lacune in Pteraspis—their presence in Cephalaspis; 2nd, in the different general character and arrangement of the vascular sinuses ; 3rd, in the different mode of arrangement of the external layer. These differences appear to me to be in themselves fully suffi- cient to warrant a generic distinction, but not more; for they are not greater than may be found among closely allied genera. It will be observed that the account of the structure of Pteraspis given by M. Kner coincides, so far as it goes, with mine; and the ex- amination of one of his Pteraspides (of which Sir Philip Egerton, with his usual liberality, has permitted me to have a section made), though not so satisfactory as I could have wished, still leads me to entertain no doubt that his fossils are really Péeraspides, and closely allied to Pteraspis Lloydit. 3 In this specimen, however, the histological characters which have been described are almost all undistinguishable. All that remains of the Pteraspis is a yellowish substance, without any definite struc- ture, which appears in the section to form loops broader at their free than at their attached ends, and to send in longer or shorter reticu- lated processes of a similar character into the interior of the matrix. The interspaces of the loops are filled up with crystalline masses of carbonate of lime (‘). The length of the loop-like processes is about ;+,th of an inch, and the breadth of their wide end about the same; the width of their necks is not more than ;4)th, or thereabouts. Now these are, as nearly as may be, the average dimensions of the sections of the ridges of Pteraspis. No one can, I think, hesitate in placing Pteraspis among Fishes. So far from its structure having “no parallel among Fishes,”’ it has absolutely no parallel in any other division of the animal kingdom. I have never seen any Molluscan or Crustacean structure with which it could be for a moment confounded. Its relations with Cephalas- pis, on the contrary, are very close. In each the shield is excessively thin, and composed of three or four layers :—Ist, an “internal,” composed of lamellze parallel with the surface, and traversed more or _ less obliquely by vascular canals ; 2nd, next to this is a ‘‘middle layer,”’ containing the network of wide canals or areole; 3rd, the “ reti- cular layer,’ described in Cephalaspis as part of No. 2, from which _ it is not distinctly marked in that genus; 4th, the “external layer,” consisting of a cosmine-like substance raised into ridges or tubercles. _ The “ bony granules,” or “‘ prisms,”’ supposed to be. characteristic 278 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 6, of Pteraspis, the ‘‘ polygonal ossicles” and the “ fibrous bony layer,” supposed to be peculiar features of Cephalaspis, have, as I have shown, no existence. Supposing that the shield of Pteraspis, like that of Cephalaspis, covered the animal’s head (though there may be some ground for entertaining a doubt on this point), then it may be said that the presence of orbits in one, and their absence in the other, indicates a wide difference between the two genera. It must be remembered, however, that there is precisely the same difference between Pterichthys and Coccosteus, which are admitted by all to be closely allied. : Though I have had no opportunity of examining the Russian species, I believe I do not err in regarding what Pander describes as the teeth of Cephalaspis as merely an excessive development of the marginal tubercles of the outer layer. It does not appear to me that there is any evidence that the mouth was situated at the margin of the shield; on the contrary, the inward prolongation of the re- flected ventral layer leads me to suspect that the under surface of the head of Cephalaspis resembled that of Loricaria or of Acipenser. Zoological position of CEPHALASPIS and PTERASPIS. Leaving for the present Professor Pander’s “‘ Conodonts”’ out of view, Cephalaspis and Pteraspis are among the oldest, if they are not the very oldest, of known fishes ; and it is therefore highly inter- esting to inquire into their position in the scale of ichthyic nature. Paleontologists in general, following Agassiz, classify them as “* Ganoids ;” but it is to be feared that few persons who have not paid special attention to recent Ichthyology and to Comparative Anatomy have a clear conception of what is meant by the term ** Ganoid.”’ ; The founder of the Order, allowing himself to attach an undue weight to mere secondary characters, included under the head of “‘ Ganoidei”’ a heterogeneous assemblage of Fishes characterized by very few common characters, save their hard and shining scales, and the abdominal position of their ventral fins, but embracing the Silu- roids, the Gymnodonts, and the Ostracionts, while the genus Amia was allowed to remain among the Clupecde. If these are all Ganoids, and if such are the characters of the Order, then doubtless Péeraspis and Cephalaspis are Ganoids. Since the publication of the admirable and philosopnica re- searches of Johannes Miller, however, the term Ganoidez has been received in a very different sense by the great mass of naturalists. Miller showed that the great majority of the recent Fishes classed as Ganoid by Agassiz, viz. the Siluroids, the Gymnodonts, the Ostracionts, &c., were in no essential respect different from the T'eleostez, or true bony fishes, while the true recent Ganoids formed a small but extremely remarkable assemblage, characterized by a structure in many respects intermediate between that of Teleostet and that of the Elasmobranchii (or what are commonly called cartilaginous fishes). Miller showed, _ furthermore, that the character of the surface and the histological texture of the scales are of little systematic value, and reduced the - 1858. ] HUXLEY—CEPHALASPIS AND PTERASPIS. 279 diagnostic marks of a Ganoid, visible in the external skeleton, to two —the presence of ‘fulcra”’ and the articulation of the scales by gomphosis. The rest of the essential characters of the Ganoids are entirely derived from the soft parts—the brain, the heart, the branchiz, and the air-bladder. A Ganoid is in fact distinguished from any other fish by the following peculiarities. The optic nerves form a chiasma; the bulbus aortz is rhythmi- cally contractile, and provided with several series of valves ; the branchiz are free ; there is an air-bladder connected by an open duct with the intestine; the ventral fins are abdominal. These essential characters are shared by only six genera of existing fishes—Lepzdos- teus, Polypterus, Amia, Acipenser, Scapirhynchus, and Spatularia —which are no less singular in their distribution than in their ana- tomy. All are essentially freshwater fishes; all are found in the northern hemisphere; three—Lepidosteus, Amia, and Spatularta—are exclusively North American; Polypterus is only known in the Nile, while Acipenser is common to Kurope, Asia, and North America. Now what evidence have we that either Cephalaspis or Pteraspis are in the proper sense Ganoids? ‘There is nothing about their dermal covering peculiarly characteristic of Ganoids; and as to the rudiment- ary state of ossification of the vertebral column, there are Teleostean fishes (e. g. Helmichthys) quite as imperfect in this respect as any Ganoid. Without doubt there is a singularly close resemblance, in the struc- ture of the dermal plates, between Cephalaspis and Megalichthys— the last being very probably a true Ganoid ; but the point of differ- ence is noteworthy: 7z¢ is precisely the characteristic ganoin-layer which is absent in Cephalaspis. On the other hand, the arrangement of the hard tissues in Péer- aspis reminds one almost as strongly of Ostracion, an undoubted Teleostean. The existing fishes to which Cephalaspis presents the nearest resemblance in form, viz. Loricaria and Callichthys, are Siluroid Teleosteans, and not Ganoids; and, if we take the immediate allies of Cephalaspis and Pteraspis, viz. Coccosteus and Pterichthys, their analogies with Siluroids, such as Bagrus and Doras, are as strong as those with Acipenser. A careful consideration of the facts, then, seems to me to prove only the necessity of suspending one’s judgment. That Cephalaspis and Pteraspis are either Ganoids or Teleosteans appears certain ; but to which of these orders they belong, there is no evidence to show. If this conclusion is valid, it is clear that the ordinary assumption, that the earliest fishes belonged to low types of organization, falls to the ground, whatever may be the relative estimation in which the different orders of fishes are held. . But it is said that the great development of the dermal skeleton, combined with the rudimentary condition of the endo-skeleton, shows ~ that these early fishes occupied a low place within their own group. Mere a-priori argumentation on such questions as these would be a waste of time; but, happily, we can put the principle involved in 280 PROCEEDINGS OF THE GEOLOGICAL socieTy. [Jan. 6, this reasoning to the test by direct observation. This principle clearly is, that the development of the exo- and endo-skeletons stands in some ratio to the general perfection of the organization of a fish. Now the existing genera of Ganoids are, as I have said above, characterized by certain anatomical peculiarities common to all; and, in every essential of organization, no one can be said to be superior or inferior to another. The same kind of brain, heart, and respiratory organs are to be found in all; nevertheless, Nature seems to have amused herself with working out in this small group every possible variety and combination of endo-skeleton and exo-skeleton. Lepidosteus has a greatly developed exo-skeleton, and the most Salamandroid vertebra known among fishes. Polypterus has an equally well-developed exo-skeleton, and a well- ossified but piscine vertebral column. Amia has scales as thin and flexible as those of a carp, with a well-ossified skeleton like that of an ordinary Teleostean fish. Acipenser and Seapirhynchus have large enamelled dermal plates, constituting a well- developed Pee ee ES) with a cartilaginous yer- tebral column and persistent chorda dorsalis ; While, finally, Spatularia, with its mainly cartilaginous endo- skeleton, has a smooth skin, without dermal plates at all. In the face of these plain anatomical facts, what is the value of the argument from the development or non-development of the skele- ton to the grade of organization of a fish? EXPLANATION OF THE PLATES. PuiaTe XIV. Cephalaspis. Fig. 1. Vertical section of the shield of Cephalaspis, magnified 100 diameters. a. Outer layer. 4. Reticular layer. c,d. Middle and innermost sub- stance. e. Vascular canals. f# Matrix. Fig. 2. Horizontal section of the same, viewed from the outer side, showing the peculiar arrangement of the vascular canals along the so-called “ su- tures,” magnified 50 diameters. Fig. 3. Thin scale of the inner substance showing the osseous lacunez of two laminz, magnified 200 diameters. Fig. 4. Outline of a vertical section through the shield of Cephalaspis, showing its inflected margin (a) and inferior flexible wall (4), magnified 2 diameters. Fig. 5. Section of the inferior wall at the point of transition of the ordinary sub- stance of the shield (a) into the thin flexible under layer (4), magnified 100 diameters. PLATE XV. Pteraspis. Fig. 1. Vertical section, magnified 100 diameters. a. “ Enamel ”’-ridges forming the outer layer. 4. Reticular layer. c,d. Middle and inner substance. e. Cavity filled with matrix—one of the supposed “ ossicles.” # Vascular canal. g. Matrix. Fig. 2. Portion of the shield of Pteraspis Banksii, viewed from within: letters as in fig. 1: magnified 10 diameters. Fig. 3. Vertical section of inner layer of Pteraspis, showing the laminz and one of the vascular canals, magnified 100 diameters. Fig. 4. A flake of the inner layer viewed from within, magnified 25 diameters. a. Vascular canals. WeY. 7 I ot as / Fa Se y cea pian LB . CEP RAGA SP IS WY MY Ky Y ff aS vy Yj Y Wp ae, Wy 3 wil : +H “2 5 5 3 PAVE e oe bo oda ut. 3 1858.) HUXLEY—PLESIOSAURUS. 281 2. On a New Species of Piestosaurvus from STREET, near GLAs- TONBURY ; with Remarks on the Structure of the Atuas and Axis VERTEBR&, and of the CRANiUM, in that Genus. By Tuomas H. Hux ey, F.R.S., F.G.S., Professor of Nat. Hist. &c. Tue locality where the Plesiosaurus, which forms the subject of the present brief notice*, was obtained is already famous for its richness in such remains. In fact, the limestone beds of the Lower Lias at Street have already yielded at least three species of Plestosaurus— P. Hawkinsii, P. macrocephalus, and P. megacephalus ; and it seemed so unlikely that a fourth species should have inhabited the same area, that I was for a long while unwilling to admit the distinctness of the form at present under consideration. The evidence which I shall bring forward, however, seems to me to admit of no other conclusion. The specimen is a remarkably fine one. The limestone matrix in which it is imbedded being hard and free from pyrites, every part is well preserved ; and the value of the fossil is further enhanced by two circumstances :—first, the very slight amount of disturbance which the bones have undergone, so that the vertebrze from the third cervical to the last caudal are all in their natural positions ; secondly, the perfectly lateral view of the body which is presented. The only important defects are the absence of the paddles, and the flattening and apparent loss of the lower jaw which the head has suffered. The total length of the skeleton is about 71 feet. The left side is exposed, and the neck and ‘tail are strongly bent upwards, as if the creature had died in a state of opisthotonic rigidity. The head is twisted, so that its upper surface only is visible, and it is at the same time bent back, at right angles to the neck. In consequence of this, the occipital condyle and the atlas are well separated. The two anterior cervical vertebree were originally partially covered by the crushed right os quadratum ; but by removing the latter both atlas and axis have been very clearly exposed. . As the Museum of Practical Geology is indebted to the judgment and energy of my friend and colleague Mr. Robert Etheridge, F.G.S., for the acquisition of this fine Plescosaurus, I think I cannot do better than name it after him, P. Etheridgii. The following are the most important characters of this species :— 1. The length of the skull (measured from the end of the pre- maxillaries to the occipital condyle+) is less than one-thirteenth of the whole length of the body. As the anterior teeth have nearly disappeared, it is not certain that the skull may not have borne a slightly larger proportion to the body; but the anterior slope of the premaxillaries clearly shows that the allowance to be made on this ground, if any, must be very small. * The specimen will be fuily described and figured in the Decades of the Geo- logical Survey of Great Britain. + The “length of the head” measured from the end of the snout to the poste- rior extremity of the lower jaw is commonly taken as the unit of comparison. But the end of the os quadratum and the lower jaw are so readily displaced as to render this anything but a safe standard. id 282 PROCEEDINGS OF THE GEOLOGICAL society. [Jan. 6, 2. There are thirty cervical vertebree—vertebree, that is, which present facets for articulation with ribs on the lower half of their centrum ; the ribs being short and compressed superiorly, or hatchet- shaped*. 3. Three times the length of the skull equals the length of the anterior twenty-three cervical vertebree ; four times the same length equals the anterior twenty-eight cervical vertebrae. It follows there- fore that the neck is between four and five times as long as the skull. 4, There are about 90 vertebrze, of which 30 are cervical, 23 dor- sal, 2 sacral, and 34 or 35 caudal. | _ 5. The humerus and the femur are as nearly as may be equal in size. 6. The vertical diameter of the centra of the anterior cervical ver- tebree is greater than the longitudinal, the proportion being at least as three to two in the third cervical. In the thirtieth cervical the two measurements are nearly equal, though the vertical predominates alittle. So far as they are visible in the transverse sections exposed by fracture of the limestone slab, the articular faces of the centra are nearly circular. 7. The cervical costal pits are elliptical, about half as long verti- cally as longitudinally, and from the third to the twenty-sixth inclu- sive are divided lengthwise by a well-marked longitudinal depres- sion; but there is no subdivision into two distinct facets. In all these vertebree the pits look outwards and a little downwards, their axes are parallel with those of the vertebree, and they are completely sessile. In the last three cervical vertebre the costal pits are directed more and more backwards as well as outwards, and take the form of flattened facets. At the same time their anterior edges are raised up by an outgrowth of the body of the vertebra. 8. The articular facets of the anterior dorsal vertebree are nearly circular. In the anterior eight or nine dorsal vertebre the transverse processes arise partially from below the level of the upper margin of the centrum. In the tenth they appear to arise completely above it, their upper margins being on a level with the upper edges of the posterior zygapophyses. In the eighteenth they begin again to de- scend, so that in the first sacral more than half the root of the trans- verse process is below the level of the superior margin of the body. 9. The neural spines of the cervical vertebre are inclined a little backwards, and have their anterior edges bevelled, so that their apices are more or less pointed. Those of the dorsal and sacral vertebrze are vertical, with their anterior and posterior margins parallel and their apices squarely truncated. 10. The articular faces of the caudal vertebre are nearly round, and their centra larger vertically than longitudinally. The neural spines slope backwards a little, but their anterior edges are straight * The neurapophysial sutures are not visible ; but as there is reason to believe that the neurapophyses do not extend upon the bodies of the cervical vertebra beyond their dorsal half, the character of a cervical vertebra here used is probably —_ equivalent to that employed by Prof. Owen (loc. cit.). a a ; 4 1858. | HUXLEY—PLESIOSAURUS. 283 and their ends truncated. The three or four last caudals have ap- parently neither spines nor neurapophyses. There are more than thirty named species of Plescosaurus. Of these, however, far more than half are founded upon detached bones, and I am not aware that entire, or nearly entire, specimens of more than four species, viz. dolichodeirus, Hawkinsii, macrocephalus, and brachycephalus, have as yet been described. This point is worthy of notice, when we consider that the proportion of the head to the body constitutes an important datum im the determination of the species of this genus. I will compare P. Etheridgii first with those of which complete or nearly complete skeletons have been ob- served. : In P. brachycephalus, according to Prof. Owen, the head equals one-eighth of the body in length ; in P. macrocephalus the length of the head equals one-half that of the neck ; they are therefore at once excluded. The classical authority on Plesiosauri, Mr. Conybeare, states that the head of P. dolichodeirus equals one-thirteenth of the entire body, or one-fifth of the neck, while the head and neck together are to the body as six to seven*. These proportions approach those of P. Etheridgii. But they are not the same; and besides, the neural spines of the cervical vertebree of P. dolichodewrus are quite differ- ently shaped from those of P. Htheridgu. And though the total number of vertebre in P. dolichodeirus is the same, viz. 90, 35 are said to be cervical, 27 dorsal, 2 sacral, and 26 caudal. Clearly then the specimen described has nothing to do with dolichodeirus. Plesiosaurus Hawkinsii approaches it much more closely in size, form, and general proportions. Several magnificent specimens of this species are to be seen at the British Museum, and afford excellent materials for the determination of its distinctive characters. Nevertheless the account of its charac- ters in the ‘ Report,’ already cited, presents some difficulties to the reader. At page 57, for instance, it is stated that in this species ‘the neck equals three lengths of the head, and the neck and head together equal the trunk and tail.’ If this be true, of course the length of the head must equal one-eighth of that of the whole body. Nevertheless, at page 61 of the same ‘ Report,’ it is said that the head equals less than one-tenth part of the body. Again, at page 61 (and by implication at page 637), P. Hawkinsii is said to possess twenty-nine cervical vertebree ; but at page 57 the * In his well-known memoir (Geol. Trans. ii. 1, 1824) Mr. Conybeare states at page 382, “the neck is fully equal in length to the body and tail united ;” but at page 385 he says, “‘ taking the head as 1, the neck will be 5, the body as 4, and the tail as 3: the total length being, as before remarked, 13 times that of the head.”’ Prof. Owen, in his ‘ Report on the British Fossil Reptilia,’ quotes Mr. Conybeare’s first statement, but omits to refer to the last. Prof. Owen further states (Report, p. 61) that in Pl. dolichodeirus the head is four times the length of the neck. I suppose this to be a misprint, and that what is meant is, that the neck is four times the length of the head ; but even this is at direct variance with _Mr. Conybeare’s assertions and figures. VOL. XIV.—PART I. U 284 PROCEEDINGS OF THE GEOLOGICAL society. [Jan. 6, number given is thirty-one* ; and thirty-one is stated to be the number in this species in the same author’s memoir on P. mac7o- cephalus (p. 523). No less contradictory are the statements as to the number of dorsal vertebree. At pages 57 and 58 of the ‘ Report’ they are by implication estimated at twenty-five; but at page 66 they are said to be twenty-three. I can nowhere find the slightest indication that Prof. Owen imagines the number of ¢ervical or dorsal vertebrze to be variable in the same species of Plesiosaurus. The opposed statements which I have quoted are wholly devoid of the comment which would have been naturally evoked by the discovery of so remarkable a fact. The specimens of Plesiosaurus Hawkinsit, on which the description of the species, contained in the ‘ Report on British Fossil Reptilia,’ is chiefly based, are, I believe, those now contained in the Collection of the British Museum. Of these specimens three, viz. that num- bered 2°? and figured by Mr. Hawkins in his plate 24, that num- 18 bered 14,549 and figured in plate 28 of the same work, that num- bered 14,541 and figured in Hawkins’s plate 27, are but little dis- turbed, and retain the head and neck 77 situ. In a fourth specimen, 14,550, which is in many respects e€x- tremely valuable and instructive, the head is unfortunately displaced and the anterior cervical vertebrze are absent. Besides these four specimens, there is a fifth Plestosaurus, num- bered 2000 and named dolichodeirus; it is however certainly either Hawkinsu or Etheridgii, and I believe the latter, although the ab- sence of the head and anterior cervical vertebree renders it hazardous to give a confident opinion. I will speak of these specimens in the order here named, under the heads of Nos. 1, 2, 3, 4, and 5. But I must first remark, that no one of them affords the means of determining the number of the dorsal vertebree with so much certainty as in P. Etheridgii. To ascertain the number of the dorsal, or dorso-lumbar, vertebree in any vertebral column, it is obviously necessary that we should be able to assure ourselves of these facts :—I1st, that we know which is the last cervical; 2nd, that we know the first sacral; and 3rd, that we know how many vertebrze intervene between these. In No. | the vertebral column is so obscured by the ribs and pec- toral and pelvic girdles, that no one of these points can be ascertained with accuracy. In No. 2 the anterior part of the sixth vertebra from the skull is gone, and it is impossible to be certain that a whole ver- tebra may not have disappeared ; at the same time an uncertain number of vertebre have been displaced from the middle region of the back. * At least, this is the only conclusion consistent with the definition of a cer- vical vertebra ai page 58. Prof. Owen there proposes to consider as cervical those vertebree whose centrum exhibits the whole or a part of the costal articular sur- face. At page 57 he states with respect to P. Hawkinsii, ‘‘In the first or ante- rior 31 vertebra the centrum supports the whole or part of the costal pit.” Therefore, according to the definition, these 31 vertebre are cervical. 1858. | HUXLEY—PLESIOSAURUS. 285 In No. 3 the dorso-sacral vertebre are hidden in the same way as in No. 1. In No. 4 the head and anterior cervical vertebree are removed, and the dorsal region is dislocated, the hinder part of the vertebral column overlapping the anterior. No. 5 alone exhibits the posterior part of the cervical and the whole dorsal region undisturbed. Either the sixteenth or the seventeenth vertebra in the series, counting from the first (broken) one, is here certainly the first dorsal—I believe the seventeenth. The forty-second vertebra is certainly caudal ; hence as there are two sacrals, 42—(17+2)=23, which is the number of dorsals in P. Etheridgii, to which this specimen has in other respects a close resemblance. Under these circumstances I can only suppose that Prof. Owen has some other evidence than that mentioned in his ‘ Report’ for the following statement :— “From the 32nd to the 56th vertebra inclusive, the costal arti- cular surface is wholly impressed on the neurapophysis.””—(Report, p: 37:) Now, as Prof. Owen states in his memoir on P. macrocephalus (p. 527), that in the sacral vertebree of P. Hawkinsii “a small part of the costal articular surface is contributed by the centrum,” it necessarily follows that these twenty-five vertebree (32nd to 56th in- clusive) are neither sacral nor cervical, but dorsal. It is true that at page 66 of the ‘ Report’ Prof. Owen affirms that there are only twenty-three dorsal vertebre ; but I cannot venture to set this cur- sory contradiction against a definite anatomical statement like the foregoing. I have been most desirous to arrive at a clear understanding of Prof. Owen’s definition of the species P. Hawkinsii ; but after long and careful study 1 can only arrive at the following alternatives :-— Either 1. The apparently contradictory statements which I have quoted have been made through the use of a double definition of a ** cervical vertebra,’’—meaning thereby in one case a vertebra witha certain kind of rib, in the other a vertebra with a certain kind of costal articular facet ;— Or 2. Believing the number of cervico-dorsal vertebree to be con- stant in the same species, Prof. Owen conceives that the special dorsal modification may commence either at the 30th or at the 32nd vertebra, according to individual variations. | On this hypothesis it must be assumed that the smaller number of dorsal vertebrze assigned to this species was found in that individual which exhibited the larger number of cervicals, and vice ver'sd. The numbers in the one case would be 31+4+23=54, in the other 29 + 25=54. Or 3. Prof. Owen imagines that the total number of cervico-dorsal vertebrae may vary between 52 (29+23) and 56 (31+ 25) in dif- ferent individuals of the same species. I am not aware that a shadow of evidence exists in favour of the occurrence of so remarkable a variation as the last-named in any ver- v2 286 PROCEEDINGS OF THE GEOLOGICAL society. [Jan. 6, tebrate animal so highly organized as the Plesiosaurus. If the second be the right mterpretation of Prof. Owen’s views, then P. Hawkinsii will always have the same number of cervico-dorsal ver- tebrze, and that number is according to Prof. Owen at least fifty-four, and at most fifty-six. I have shown, however, that in P. Htheridgu there are only fifty-three cervico-dorsal vertebree. I beg to repeat, however, that I can find no proof of the existence of fifty-four cervico-dorsal vertebree in any P. Hawkinsii in the Bri- tish Museum. Under these circumstances it became necessary to in-— quire whether the proportions of the head, body, and neck might not furnish the needful marks of specific distinction. Measuring these in the same way as P. Etheridgii, I find with regard to No. 1 that— 1. Taking the length of the skull (from the occipital condyle to the end of the snout) as 1, the whole body measures between 10 and 11. ‘Taking the head from the end of the snout to the end of the lower jaw as 1, the whole body measures between 8 and 9. 2. Three times the length of the skull equals the anterior 25 ver- tebre ; four times the same length equals the anterior 31 vertebree. In No. 2 the end of the tail is gone, and therefore the proportions of the skull to the entire body cannot be ascertained ; but three times the length of the skull measured along the neck reaches the middle of the twenty-fifth cervical vertebra, and four times equals the 31 vertebree as before. In No. 3 the length of the skull-is rather less than one-eleventh of the whole body ; while the length from the snout to the angle of the jaw is rather less than one-ninth of the whole body. The propor- tions of the head to the neck are as in No. 1. In No. 1 the rib of the 29th cervical vertebra is hatchet-shaped ; the shape of the ribs of the 30th and 31st vertebree is not certainly discoverable, nor can the character of their articular surfaces be clearly made out. In No. 3 the rib of the 29th vertebra is truly hatchet-shaped. Those of the 31st vertebra cannot be made out clearly, nor can that of the 30th on the left-hand side. On the right side the head of a rib lies against the posterior part of the neural arch of this vertebra ; and, though its produced angle is more or less broken, its hatchet- shape can be clearly distinguished. The costal articular facets of both the 30th and 31st vertebre are traversed by the neurapophy- sial suture. In No. 2 the condition of the posterior cervical vertebree is such as to render it very unsafe to speak decidedly as to the character of either the ribs or their articular facets. So far as these specimens go, then, they favour the idea that P. Hawhkinsii has 31 vertebre cervical in.Prof. Owen’s sense of the term, and they assuredly do not countenance the notion that these vertebree may vary in the same species. But if Plesiosaurus Haw- — kinsit has 54 or 56 cervico-dorsal vertebre, and if 31 of these are cer-. vical, then P. Ltheridgii differs from it in the following particulars :— 1. The number of cervical vertebre is at least one less. 2. The number of cervico-dorsal vertebre is one or three less. 1858. | HUXLEY—PLESIOSAURUS. 287 3. The head is shorter in proportion to the body. 4, The head is shorter in proportion to the neck. I think then there can be no doubt as to the specific distinctness of P. Htheridgii from all the Plesiosauri as yet mentioned. With regard to the other species, I judge from the descriptions and from such specimens as I have seen, that P. Htheridgii is very different from megacephalus, macromus, pachyomus, arcuatus, sub- trigonus, trigonus, brachyspondylus, costatus, dedicomus, rugosus, trochanterius, and affinis. I doubt at present whether it would be possible to distinguish the detached vertebree of P. Htheridgit from ‘those of P. Hawkinsii ; but I believe, having examined the series of vertebree in the College of Surgeons’ Museum, on which some four- teen species have been founded, they are all different from those of P. Etheridgii. The measurements of the different parts are as follows, in inches and tenths :— Head. in. tenths. From end of intermaxillary to end of occipital condyle....... Heese GIES End of intermaxillary to anterior margin of orbit ......é00...seeee a2 Le End of intermaxillary to anterior end of parietal foramen......... 4 2 ea LG OLUTM aise k oss aeeseeek eas accdebcbaeedalcadscsacned deadaceaenscavs 2 Length (oblique longest diameter) ..............sceecscenteseeereceees ho Extreme length of head from end of intermaxillary to end of PUI APACAC TIN fe rctoacicuisis sist aicniaicinaslaiietecnaieni Prapinaeoe vidsasadscinwse settee a Oe S Neck. Length of first seventeen cervical vertebra, measured along their BD LE Sea Fort sanae se ce maannee dat sciacio te sc sastiossentvieseemsersedeues os ZnS Length of following CHUTECCDL Waeeacdac ction tooscnnaesieidues ain alaweue'ea ave Lome’! Giving as entire length of neck ..... esa, 20 U Stxteenth cervical vertebra. Centrum.—Longitudinal diameter ..........scsececeeseecsenceceerens ig Vertical to base of neurapophysis* ..........se.sseeeees Ligiea Thence to top of neural Spine ...........sesecsessceesees 1 4 Neural Spime -VErLiCally J. .2cccascacovwseeoss.cecsess-sases 0 8 Neural spine longitudinally .......cccec.sssesscesssseeees Orin 7 Costal pit.—Longitudinal measure ..... Spevitedsdsensadesidect=eueos esas 0 5 WertiGal MEASULE Ws nenassotensonssistedeusacacdeseusccecves 0 3 Costal pit to base of neurapOPhySisS.......se..eseereseeeseesescees bite) Ors @ Dorsal region.—Total length .....+..scsccscsevssccercesccees csuewanes 26 5 Sixth dorsal vertebra. Centrum.—Longitudinally ..........ssccseesccseeeseeesens mart accisteoa a 1 25 Wertically, (anterior face))) ca. 2-..cecesenssnassssseusen 1 3 SEFATISVOCESELY ) santas vacsewc cade scatmiaaseedesesdacasess Leeds ees 1G Neural spine: — Vertically, ..cecapsnceastencocendoeeacascsocccescececsenuc el Longitudinally .......... bicpc toaserearavcswscadaccasdeels Oo Transverse Pprocess.——eneth 212. ....scconeeceveededencwcaserecssasees 0 75 Antero-posterior diameter .......0+..+ See ele Vertical: diameters: cas: Jit cancsencits paeienes 0 75 Sacral region.—Total length ...... Seabamiusattenadaetsuccsrdmsunnsases 25 il. * Reckoned as the deepest part of the depression under the zygapophysis, no suture being visible. 288 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 6, First sacral vertebra. iene? Centrum.— Vertically ....ccccescccsssscccccsccsrosoeees esi fenieg@oae ih ae TLAHSVEISELY an ecine <2: -.0.s2000-0-]e0-]0./Ed longissimumf ...... Soc bescode. 4 aneligee Pe magniventrumy and var.,....|...|++.|...| * multitubulatumt............66 CF ee BEQEGWOTING T, c500-fveacsonccete|asolesa| sus loue WAEEIGHOAUUIN | ease ocete|del-celan- lod. = MIME OLALUN . dacaconcesaese|sta|ss-leds loos — strangulatum ............ saalvealneaiees — tenuitextum ....... esas cpee' leeal dee subcentrale ...... aavaaueotieseee|nee| sh) Ea GGMBNGCETAS! SP: WG.” —..eascvecleie|oss|ete|ac~{sestete|-solssellsaleow| onl | EL BNMOECLAS, AACEPS «0.0. .00.0.ceccsofec|ose( Ed Lituites convolvans ........0....0.(ss.|->-|EL WOGAGUS, | vosc-tneeesnc SHO an Croe Na] nae mactene | © Oncoceras constrictumt .........]...|...[-.+/-..({H CRMNANISUIN © Beccameenacsed scvodsefiee}sbe[sdelesuieeelese|ace| os» lesolpealark ep gibbosumt ........ Pee eee bl Sivptal sasleee|obia|e si sai [awa tal SHPreGHUI | 2.3.3 .5eeceess wisisjcteiclc i Bo ea (ns (ee ae eel ee ee H Ormoceras crebriseptum .........|...[e+/eee {eee [eeefee{ Hl SrACH Ete ech censors mnieeenicte Sethe | cated EM moniliforme....... aR a hate Sree tel al tela H H H %K ww caotonm tenuifilum .......... aitie eels Bens eielistare Vala GIStalis Sec wuccckessecsenc tt baer vertebratum ..... MAceihmeicnecttepelsielscclemellteialinke Eee eeil ete eretch ed Orthoceras abruptany <- 56.05. ...006]:s.|seehese|.es|oe|~20]20e]>0e||a05|00- H equale......... AOA ee eee Met i aelee dle sal sea fh eae amplicameratumt ......scces/...Jeee[ece[ooe[Ed foecfeoe|ere|fece|ecelase|foes|ooe]| % RAMEE GPLIAN Ooiog du Some vciels Soeaeck man Hewalk Moleasiaes bowelavelose||saeteme) ROI EL 418 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Fossils. articulatuml!. rectiannulatumt ......ssssccuss TORGUET | fos facts Coaster ee ace sp. ind. e@eeeeneee PeeCeeeeest esses Phragmoceras, sp. ind. ............ Trocholites ammonius ...........- | | | BVCHURY | Wusicceeteastecinsnis cueves al eaalaes ; bilineatum and var............|--- se litell Caneellatuimt chs sccasatccseatcelseeter.| haces: GlAGN PACU ec sotcensies endac scales lecleadees Glavatmienh ycoteksice cokpenecocea see COFALIPEHOMSic.cedceeosnencecere|wacleor lesions Cuphex: 2. sc Sat cantscsisemeeceretice| sae AUSHOTIDET? Lccchecccesitessooneceleea|aelecs GM VIGATN 2”. cocecewcssccesioes|onelsnelnealaeelee PUNO TNE T isin oc sincle na swmtaian aie] ede endnotes H TEV .co.csiecs MES RSCENU He Arsh aatt An lone Ss lamellostimil . s.cbtedewacdssees|caelae aibey laqueatumt and var. ...... ee ee latiannulatumT ...... Ligemenenal as scaled multicameratum ...... Raeeeesie late lataloce lees WUC MCACUIT £2 cc cnce deen some cs hosel anloes MMMISE PLUM vi cve.aceceae ace eal sa EDs PLUMILENMIONY 2.6.00... sccece|=*- TEMUISEPEOM: Jt) ceases asBegg|ier PEREtHOLMIST side acer cat cee xeia|eecl-mslacel see planorbiformis...i.5.00-00s.s00l- ; a -, | Chazy Black-River Limestone. | Potsdam Sandstone. | Calciferous Sandstone. ECCUCAMETACUIN Loccececccseccclucslaceless subarcuatumyl ........00ce<.» eolemal eae sirigatumt ...... Paeeaducetany ee pwediane Trentonense........ Rigen bie ce alcanlaeehacelt WEELEDEAIOT aos. bascdecatovaes soe eanlamelace VEELEDEALDIEY | ecaseeenacwtescns let. Saul etoan WI PAGE cneaecccwmswastcwcen sacl ease Virgulatumil s..0c.2-[o0-|s2-[o-2] as H PISHOFIMIS............+60 Sah, 2 iS ae ae os ee *? TOT Cau Seema ae ti eeeeeres Ba Boe oe elemolans * Arges phlyctenodest ..... ocean |ueeleon tone eealsao[ewe| xmel-esl aedae- bass * ae NEE OR eon cv donee cencs|see|=a=[ecdona|.0-| veo] caalvon| bes lane| V || Me lacdieen) OE Tee symmetricat ............ eae deel cea lnen| Jo Aeee lane leas) ssaleedloaabienlect| EeCEUS NEAATENSIST) | |. -<-+-u.uleoe]--=|eoe]o-|-cn]---|can|ene|fone[nee]a--| ubMe tts AL RIONSAS son. . 0. .casncesfes|-0-|a-2]arelanefees|:ca|->=[lana|ows|oanlEL Trentonensis ......... SP ee a BO hae tS A ih ar DE ng i 4 RE A ES (De | Fa H KGalyMiene BECK fs. cecileisenanccs|ose]eos oos|2--|4 JH Blumenbachii ......... peee aes Boe Ber fee ey al Gall Gs re Wekins NEAPALCUSAN 203.56 concmns|- le IS 6 [S/S |Z SIS IE IS ala lo Cybele punctata... anieeesepingalaicslese)vactadaledaless woltnel Ed Dikelocephalus Meniskaensis wee| granulosus ........:. aalsisleate'ge * Minnesotensis .......ec.cseceres * Eurypterus remipes | CO UHI ade Oona ee eealcelocelerellorclnes| acai |mecl elias: Leperditia cylindricat . Faaleaaledal’ ais | PEAS catrmcdeodens aSiewhiis dal ctmasie oleae itn eetalewalladel aie : SIPs MG oes eraeidas ob sions efeinialsiniewarsliarde | oetsie de H Cytherina ? spinesal ..:..0..0.s00-|edcloceloas leas Pe alee ieca ae Homalonotus delphinocephalus .. ata eanleas *|H Pikeenus ALEGOKUS! weccdeveswosdessecladalacs H CTASSICAUA?.......s0e0e000 dele oleal de late V |.../H latidorsatust c.seresedeas Pe nichisl Mlle dslecelecnt as Ovatus .....06 Sajctoin'e Saanielovals cmos foals daleant@ PECHLONENSIS, bins Heden wesc weeal’s sHlagaldee * |E Isotelus canalis ...... sideictaided Soot] Agel (C PISAS. sews denetienowieds Saacioat ssnineladeladstedaloay EAA} ba EL PAWNS oes oAseaedsn cocesceceeelsssleceleeelooe| MICH AS BOM ONIT wcSciionds anid oc ninw teelebal ede |ueeloan lege laeslaeeteds nual anal eae lacihiata, ...00.+6. ceeaeR we oadesle: wdeloaelaee V Os yea? VELUSLA:. ce daséscenmetiances|sealecstecs H Olenus asaphoides!........+.......06/... Suldeloke hoes leila undulostriatus ........... isdn a atalats lapafesegaeleee H Platynotus Trentonensis ......... Pian Pas as ere Giicds less se Phacops callicephalus Maer owidoateaelacaladal ees EL PAICAOMA | Rawtolvecneneveieetenls es eaalaen| oe! bd Bir WTS. 6. ckiae Seinen tana wal Seehadalosale | ar Soh ex FLRESIAANMN, ictok shinee dncvcsenal tales lacahessleaaler aval DalmManDbews icc cecnts See epee Meal aes hide alicia macrophthalmus see.sesevesslscsleselose ai as | ok WBDIER 2.00308 035 dc 55 0 pags] oe) | Roe REMICER oc: osc 26 aScdwonids: eSB dtloe 2 (Stroph.) grandis.........| * | * | * Orthis parva...........+5. ey CH Ne aie i Ot eo testudinaria ....... salstwedss| S| SE-ibeck striatula - foshaes * WUNASEPEUM, serccerssaaceveas Beil se as ek * | Bucania trilobate ...0..sceesecc0ses (a IB) re eee ao * | * * | Calymene Blumenbachii ......... C. Bea ick | ket oatoe * || Platynotus Trentonensis ......... C; * cantlicts Phacops limulurus: © ....20s ae alata C. (——-) varistriata ......... ales Wo alb Bala ilaine te as Sle C. Outhis hybrida ..isteeadeeee-stiwalans Fl isch Pabedan woe] Sh. | WL. GECIUSH 2: uaconcsteggeadsuawaevas Eee Meads sienna vee] F We OFbiculapis).<.qinesae es dant doaen| dor moet) a leis les veal oe Sh. | WL. TESUpINALAs 1 4 seh ees deevesase|are dois veahn dave inci ig Fe Sh. | WL. Spirifer (Delthyris) bilobus...... FEE at, sllawed ni waa) ae C, V. ( ) granulosus? ........./++ asda one A aan| C. (——-) macropleurus......... eadiees| nom, eon sns | Bol gan Hee Me ( ) pachyopterus......... analaan), acs lnsahonsl|czo)smelsacaismnmeine a PUCHUNIS) .eosdnee ese: 3] Cems *|%|*| ... |Va, Sh. WL, L ( BPEN. a. cup aae en ena eioes fann| i asa staal ate | * | sce | ie Atrypa concentrica?? ............ a> Ue gai cee spaceatlice Gage g: D PEGUINAMIATA inser nem cenehuicun|ae) =<: Sienna Saale v: ADA AGA ss aiscs scoassnacnabavsnscyec|s enna. sion, |e ara * | * C. FACUMONAS no. vane a> seems -decesesiaea|sos Fae leea| awa Sekeee tees C. NSEWIN Hes |usateeele ss * | soe | Shel ieee Rhynchonella borealis ............|-.+|++: oqe fecsloewlace| #| cos | SEL five PEDIC IAM GL saraace tee naan sess sau wesl ans ade fenglesstoos| | con | Sve summa WV GSD bias canine imac eacateen Hah} SV Gate steel ees lees] ase | | Vay Terebratula deflexa ?............00 Be ee ec ere Coe sl a oe Ale NPs a cakasieendnae tx ccematvemucs bane teas miaelldechenatiee *| ... | Shee Pentamerus galeatus............... ca Reat, oaualleesi laa *|/*|... | Sh. | WL. pseudo-galeatus ............seeleoe{ oss sicty cdlgen [aestoe| ate H. Avicula multilineata ............... Ar en ae am (ed AC eee H. THONCICOIR (So abies Pos nia te cunes buatees cas lame lab cH mere) cee 1 Lower Silurian. 2 Devonian. a [To face p. 424. Tapie VIII.—The Recurrent Fossils of the Devonian System of the State of New York; including the species which enter from the Silurian. Fossils. Microdon bellastriata ......... Pleurotomaria pervetusta ...... Bellerophon striatus ............ EXPALSUN: soneeseaeret aes te Goniatites expansus ............ Clymenia ? complanata ......... Cornulites serpularius ......... Calymene Blumenbachii ...... Phacops macrophthalmus...... Pleurodictyum problematicum Lower Silurian. “Sandstone. ees ick-River Limestone. = fo) o % ae ro re) =) =| a | % 3 SF ia op) =| g : om n Palast eC! iver Group. Middle Siturian: Upper Silurian. 1e. Limest. of Schohar tamerus Limestone. i Shaly Limestone. ndstone. > Group. a. 3 iS) roup. + * * * | Salt Group. eee % eee eee eee . ees eee eee eee eee V eee eee eee eee eos eos eee eco V V * eae ooe see see atamerus Limestone. Lower Devonian. andstone. i Group. Limestone. is Limestone. oo ee eS Se SS aan Middle Devonian. | Upper Devonian. [To face p. 424. Tanie VIII.—Dhe Recurrent Fossils of the Devonian System of the State of New York; including the species which enter from the Silurian. Lower Silurian. Middle Silurian. Upper Silurian. Lower Devonian. Middle Devonian. Fossils. Potsdam Sandstone. Calciferous Sandstone Chazy Black-River Limestone. Birdseye Limestone. Trenton Limestone Utica Slate. Hudson-River Group. Oneida Conglomerate. Medina Sandstone. Clinton Group. j Niagara Group. Coralline Limest. of Schoharie. Onondaga-Salt Group. Waterlime Group. Lower Pentamerus Limestone. Delthyris-Shaly Limestone. Upper Pentamerus Limestone. Oriskany Sandstone. Schoharie Grit. Onondaga Limestone. Corniferous Limestone. | Upper Devonian. Marcellus Shale. Hamilton Group. Catskill Group. Tully Limestone. | Chemung Group. Fucoides graphica . Cauda-gall Tentaculites Fissurella Columnaria, sp. ind. .. Catenipora escharoides . Favosites alveolaris .. Gothlandica ...., Stromatopora concentrica Athyris concentrica .. Leptzna crenistria..... depressa .. linearis Setigera . Orthis Tulliensis umbonata .... Spirifer acanthotus acuminatus... apertnratus cultrijugatus’ . heteroclytus . mucronatus Niagarensis plicatus Urii Atrypa affinis didyma .. emacerata ?. lentiformis . prisca ... reticularis concentrica?..... Rhynchonella borealis . Nucula Productus Fragaria ? scabriculus. Orbicula minuta Avicula Boydii . fragilis multilineata . orbiculata . pectiniformis Pterinza fasciculata Lucina rugosa Posidonia lirata Chemnitzia nexilis Modiola concentrica Microdon bellastriata Pleurotomaria pervetusta Bellerophon striatus .... expansus....,..... Goniatites expansus . Clymenia? complanata Cornulites serpularius Calymene Blumenbachii Phacops macrophthalmus, . | Pleurodictyum problematicum] ... tox: | Cauda-galli Group. coo | | Portage Group. * x1: x Genesee Slate. NN* Es : A| 5 2 Fossils. "5! 2) 2 Q|-2 YQ 2 si) le ES Shea! |S -a | Ojaa Of a Stromatocerium rugosum ...|*|*| || Pleurotomaria umbilicata ....... * ox Chetetes Lycoperdon ...... * | * |x || Orthoceras duplex ............ | > Joos] * Lingula obtusa .................. | 3k Wertelindle ,7/5,th of an inch in diameter, I shall adopt the following scale, and call SORBY—STRUCTURE OF CRYSTALS. 455 Cavities above ;3,th of an inch in diameter, very large. » from >)pth to 45th, moderately large. 3 « from Toooth to Tyo0oth, moderately small. » less than nti ths very small. In some respects it is best to mount crystals formed in the wet way, in as shallow glass cells as will hold them, in a concentrated cold solution of the salt itself; for then, never being dried, none of the cavities can lose their fluid, which is not the case if they are mounted in varnish or Canada balsam. Independent of that, some facts are seen to greater advantage when crystals are mounted in clear varnish in cells which may be made out of cardboard with a wadding-puuch ; and I therefore usually adopt both methods. The magnifying powers generally required are from 50 to 400 linear; and when the crystals possess strong double refraction, a polarizer or analyser should be used, so adjusted that only one image of the cavities is visible; or else they appear indistinct. I have in nearly all cases lithographed the accompanying figures (Pls. XVI.—XIX.) as seen with one adjustment of the focus, but have slightly shaded the enclosed crystals, although they are some- times quite colourless, in order to distinguish them from irregula- rities on the surface of the cavities. The figures with a dotted outline represent portions of crystals, whereas all the rest are entire crystals or detached cavities, as if the surrounding paper were the clear substance of the larger crystals in which they occur. -Few substances could be more suitable, as characteristic types, than the chlorides of sodium and potassium, sulphate and bichromate of potash, alum, and sulphate of zinc. When a solution of chloride of potassium is allowed to evaporate spontaneously, the character and form of the crystals vary most remarkably, according as the weather is cold or warm, moist or dry. In cool damp weather, when evaporation goes on slowly, sometimes all the crystals are similar to fig. 1, having a square patch towards the centre, which is white by reflected, but black by transmitted light, whilst the rest of the crystal is clear and transparent. When much more highly magnified, it is seen that the opacity of the central portion is due to vast numbers of minute cavities, the amount of which varies in bands parallel to the sides of the crystal, and also in such a manner as to give rise to the peculiar cross seen in the figure. These cavities are full of the liquid from which the crystals were deposited ; and this having a smaller power of refraction than the substance of the crystal, the contents reflect and strongly refract the light, and, like the bubbles of air m the water of a cataract, give a white appearance as seen by refiexion, or darkness and opacity when viewed by transmitted light. The manner in which these cavities are formed is well illustrated by fig. 2, where the unshaded portion represents part of the extreme edge of a crystal of common salt, and the shaded the concentrated solution from which it crystallized, entering into a deep notch formed by the irregular growth of the crystal. If, on the further growth 456 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. of the crystal, more salt were to be deposited at the upper part of the notch than at the bottom, as shown by the dotted line, a portion of the liquid would be enclosed in the crystal, and form a fluid- cavity like that seen on the right-hand side ; whereas, if the crystal grew so as to enclose the projecting portion of fluid by a plane parallel to the face of the crystal, a fluid-cavity like that on the left side would be produced. These two cavities, as well as figs. 3, 4, and 5, illustrate the usual character of those in common salt or chloride of potassium. When deep, they have a broad dark outline, like fig. 4 ; but when flat and very shallow, they are bounded by a narrow black line, as in fig. 5. Often they are much longer in one direction than in any other, so as to be tubes, like fig. 3 ; and this is especially the case in the long prismatic crystals of chlo- ride of potassium sometimes formed on the cooling of a warm solution. The manner in which the cavities are produced necessarily causes them to be full of fluid at the time of their formation. If this takes place at the ordinary temperature, and they are kept in fluid, they remain quite full, and none of the cavities contain bubbles. When, however, they are formed at a higher temperature, the fluid of course contracts on cooling, and, just as happens on the cooling of a glass- tube filled with hot water, a vacuity like a bubble makes its appear- ance, as shown in fig. 7. In order to obtain crystals slowly deposited at the heat of boiling water, I employ a flat-bottomed flask, over the mouth of which I tie a piece of blotting-paper, and keep it in a bath of boiling water, with the long neck projecting through a hole in a metal plate covering the bath. For these experiments no substance is more convenient than com- mon salt, because it is so very little more soluble in hot than in cold water. Having, then, a concentrated solution in the flask, it evapo- rates through the blotting-paper, and crystals are slowly deposited at the heat of boiling water. When a number of about =,th of an inch in diameter are formed, the hot solution is quickly poured off, and a small quantity of a concentrated ‘cold solution added, so as to prevent the deposition of salt when the remaining solution becomes cold ; and then, separating the larger and very small by means of sieves, the crystals of about j,th to 4th of an inch in diameter are mounted in glass cells in a concentrated solution of the salt. On examining them with the microscope, it is seen that the greater part of the ca- vities contain small bubbles, produced by the contraction of the fluid. Adopting the same method with chloride of potassium, in some eases most excellent thin flat crystals are formed, containing many very interesting cavities. A portion of one of these crystals is drawn in fig. 6, which serves to show the great number and peculiar form of the cavities, and how they occur in bands parallel to the edges of the crystal. Unlike when formed at the ordinary temperature, many of the cavities are of very complicated forms, as shown in figs. 8 and 10. | In order to ascertain the relative size of the fluid and bubbles in the cavities, it is best to measure with the micrometer such long re- SORBY—STRUCTURE OF CRYSTALS. A457 gular tubes as figs. 9 and 50. It may also be determined with suffi- cient accuracy from cavities like figs. 101 and 113, which are equally deep throughout, and have a flattened vacuity, so that the propor- tion between their areas is that between their volumes. If, however, neither of these kinds can be found, the best approximation that can be made is to be derived from such cavities as are nearly equiaxed, so that the relative magnitude of the cavity and vacuity equals the cube of the ratio of their diameters. In the very excellent tubular cavity (fig. 9) in chloride of potassium formed at a heat not much below that of boiling water, the vacuity is about ‘025 of the fluid; but, if the cohesion of the sides produced no effect, it should have been about ‘030. Hence I think we must conclude that the cohesion of the liquid to the sides of so small a cavity slightly diminishes the size of the vacuity, either by stretching the fluid or the substance of the crystal. That very minute cavities do produce such an effect, is proved by the fact that they often con- tain no bubbles, as though the cohesive force entirely counteracted the contraction of the fluid, and operated like the reverse of a very great pressure; and M. Berthelot has also shown (Annales de Chimie, 3° sér. t. xxx. p. 232) that this occurs to a certain extent, even in glass-tubes. When fiuid-cavities are large, the bubbles move about, if the cry- stal be turned, like those in spirit-levels; but when small, this test is not easily applied. We can readily see, with a high magnifying power, that the constant tremor of the ground causes the bubble in a level to be in constant motion; but no such movement can be seen in the larger fluid-cavities. In the very small, however, the bubbles move in a most striking manner, as if they were minute animalcules swimming about and exploring every part of the cavities. The true physical cause of this movement still remains to be determined ; for hitherto I have not been able to form any theory that was not appa- rently upset by facts subsequently discovered. Whatever be the cause, the fact of the movement is of very great value in these in- quiries, since, when a bubble moves about, the substance in the cavity must of course be a liquid. The peculiarities of fluid-cavities formed when crystals are deposited from a solution containing some other salt, can be studied to great advantage by crystallizing common salt from a solution of bichromate of potash. If the solution be saturated with the bichromate at the ordinary temperature, it is of a deep yellow colour, and the fluid- cavities in the crystals of common salt deposited from it are seen to be filled with this yellow liquid ; and the crystals are thus rendered yellow, and remain so when mounted in a colourless solution of com- mon salt. If, however, the crystals be formed at the temperature of boiling water in a solution containing more of the bichromate than can remain dissolved at the ordinary temperature, small crystals of the deep red colour of that salt are deposited inside the fluid-cavities, as shown by figs. 11 and 12. When the solution is saturated at 100° C. with both common salt and the bichromate, so that, on slow evaporation at that temperature, crystals of both salts are deposited, 458 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. the common salt encloses some small crystals of the bichromate, like fig. 14. Occasionally these sq interfere with the crystallization, that they give rise to small attached fluid-cavities, as seen on the right- hand side of fig. 15 ; or there may be more than one crystal and a larger fluid-cavity, like fig. 16. These fluid-cavities differ from those just described, in containing no small crystals of the bichromate, that which could not be retained in solution having been deposited on the larger preexisting crystals. Moreover, as shown by fig. 16, these en- closed crystals project beyond the general boundary-line of the fluid- cavities, whereas in the other case they are merely deposited on the surface of the cavities. Great numbers of that kind do also occur; and often so many crystals are deposited, that the cavity appears to be quite full of them, as shown by fig. 17. It is, however, well worthy of remark, that many of the smaller cavities remain for months full of a deep yellow liquid, which I have supposed to be represented by the shading in fig. 13, containing far more of the bichromate in solution than can be retained when in large quantities, as if these minute cavities exercised the same influence in preventing the deposi- tion of crystals, that, accordmg to Dr. Percy’s and my own observa- tions (Dec. 1857), minute tubes exercise in preventing the freezing of water until the temperature is much lower than that at which it freezes at once in larger tubes. . When, instead of bichromate of potash, chloride of potassium is employed, small cubic or rectangular crystals are deposited in the fluid-cavities of the common salt, as shown in figs. 18 and 19; and in every case that I have seen, their edges are all parallel to the rect- angular planes of the cavities. Ifa concentrated solution of hydro- chlorate of ammonia be used, the fluid-cavities in the common salt contain crystals of the salt of ammonia of a very rounded character, as shown by fig. 20, so as to appear like enclosed globules of a dense liquid. i Phiise experiments (March 1858) therefore show that, when cry- stals are formed at an elevated temperature, evidence of it is afforded by the contraction of the fluid enclosed in the cavities giving rise to a vacuity, and the reduction of its solvent power causing the deposi- tion of crystals. Since, of course, the amount of the contraction of the fluid depends upon the height of the temperature from which it has cooled, the relative size of the vacuity must indicate how much the temperature at which the crystals were formed was above that at which they are examined, in the same manner as the sinking of the mercury in a self-registering-maximum thermometer shows the dif- ference in the temperature. Figs. 21 & 22 in nitrate of potash, 23 in binoxalate of ammonia, 24 and 25 in sulphate of zinc, represent fluid-cavities of rather striking forms,—the shading in figs. 24 and 25 being like the ap- pearance produced by planes inclined to the line of vision. In many substances the fluid-cavities are commonly in the form of tubes, which are often of irregular width, and, as it were, pass into rows of smaller, shorter cavities, as shown by fig. 26, representing a portion of alum. Some of the cavities in this salt are as shown in fig. 27 ; SORBY—STRUCTURE OF CRYSTALS. 459 but the more common forms are like figs. 28, 30, and 31. When deposited at a heat of 50° C. (122° F.), the cohesion of the sides is sufficient to entirely counteract the small amount of contraction, and prevents the formation of vacuities. Besides fiuid-cavities, a few most interesting larger cavities full of air were formed, which appear as if they had been bubbles, given off from the solution, that were enclosed in the growing crystal. Small quantities of this air are also in some cases caught up in the fluid-cavities; so that a few contain bubbles of considerable size in proportion to that of the cavity. The dif- ference between the cavities full of fluid and those full of air is most striking. The refractive power of the fluid being nearly the same as that of the crystal, the cavities containing it are almost invisible by reflected light, and give only a narrow outline by trans- mitted, whilst, the refractive power of the air bemg so much less, the cavities containing it shine brilliantly by reflected light, and by transmitted light have a very broad and dark outline, as shown by fig. 29. Hitherto all my descriptions refer to crystals that were mounted in liquid and never dried. When, however, exposed for some time to dry air, it is as if some of the cavities were not so completely closed as to prevent the slow passage of liquid from them; and there- fore bubbles make their appearance, gradually increasing in size, and becoming quite large, as shown by figs. 30 and 31, which are cavities in alum, originally quite full of fluid at the ordinary tempe- rature. In the case of some crystals, especially those like alum, containing chemically combined water, perhaps the fluid may actually pass off through their solid substance; but this is apparently con- fined to cavities near the surface. In many crystals, however, and especially in the more solid parts, where tle fluid has been completely shut up, it appears to remain nearly or quite permanently—at all events for many years—even when they have been kept quite dry. These facts must be carefully borne in mind when attempting to deduce the temperature at which crystals were formed; and care must be taken not to confound cavities that have lost some fluid by drying, with those in a normal state enclosing bubbles that have been produced by the contraction of the liquid on cooling. They may often be distinguished without much difficulty, because when fluid is lost there is a great inequality in the relative size of the bubbles in different cavities, whereas in the other case it is nearly uniform. If the planes of a fluid-cavity are inclined at certain angles to the line of vision, they may totally reflect the transmitted light, and the cavity appear like a fragment of some black and opake substance enclosed in the crystal. This is often the case in sulphate of potash ; and an example from that salt is represented by fig. 33. When a solution of common salt is evaporated at 100° C. in an open-mouthed flask, a crust is formed on the sides, above the level of the solution. In this case, during the growth, the crystalline crust is alternately exposed to the solution and the air; and when a portion is mounted in fluid and examined with the microscope, it is seen to have a peculiar and very interesting structure. Some of the cavities VOL. XIV.—PART I. 2H 460 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. are precisely like those formed below the level of the solution, whilst others are as if it had been partially evaporated in the cavities before they were finally enclosed in solid crystal ; and therefore they contain much solid matter, as shown by fig. 37. Minute crystals of sulphate of lime are also enclosed in the solid crystal ; and some have been deposited inside the fluid-cavities before they were finally shut up, as shown in fig. 36. Other cavities have caught up air as well as fluid, so that they contain very large bubbles, as shown in fig. 34; whilst in others, like fig. 35, there is no fluid ;—these various kinds gradually passing into one another. In a similar manner when the solution of salt contains less bichromate of potash than can be held in solution at the ordinary temperature, there occur, in the crystalline crust, cavities like those in crystals formed below the level of the liquid when a dilute solution is employed, as well as like those when a saturated hot solution is used, on account of its becoming variously concentrated by drying on the surface of the crust. b. Number, size, form, and arrangement of cavities. There is generally a most intimate relation between the number of cavities in a crystal and the rate at which it was formed. This is well illustrated by the chlorides of sodium and potassium ; for when very slowly deposited, they are transparent, and contain but few, whereas, when deposited more quickly, they are so full of cavities as to be very white and opake. In some cases the deposition proceeds rapidly at first, and white opake nuclei are formed; and afterwards it proceeds more slowly, and the exterior of the crystals is clear and transparent, as shown by fig. 1,—the change from opake to trans- parent being either sudden or gradual, according to circumstances. This also usually happens when substances are crystallized by the cooling of a strong hot solution; for then deposition proceeds rapidly at first, but slowly towards the close of the process. Sul- phate of potash, however, contains nearly as many cavities when formed slowly as when deposited quickly. There is also a consider- able difference in the number of cavities in different salts, though formed under similar conditions. Thus, if solutions of alum and chloride of potassium be evaporated moderately quickly side by side at the ordinary temperature, the chloride of potassium contains so many cavities as to be perfectly white and opake, whereas the alum contains very few, and is perfectly transparent. The same is the case when a mixed solution of common salt and alum is evaporated. In general the size of the cavities varies inversely as their number ; for when the crystals are slowly formed, they are larger, though less numerous, as shown to great advantage by the different parts of fig. 1. Ifthe rate of growth be the same, crystals formed at a high temperature contain fewer and larger cavities than those formed at a lower. When the sides of the cavities are definite and straight, they are planes of the crystal ;.and therefore there is a connexion between the SORBY—STRUCTURE OF CRYSTALS. 461 form of the crystal and that of the cavities. For example, in the cubic crystals of the chlorides of sodium and potassium they are rectangular, as seen in figs. 4, 17, & 19; and in the octahedral crystals of alum they are often equilateral triangles, like figs, 28 & 30: but, from forms thus essentially related to the planes of the | crystals, they pass into all kinds of irregular shapes only slightly related, as shown in a remarkable manner by the cavities in chloride of potassium formed at 100° C. (figs. 8 & 10). The arrangement of the cavities is also sometimes related to the form of the crystal, as shown in fig. 1; and bands parallel to the bounding edges are very common, being in fact lines of growth, pro- bably indicating variations in the rate of deposition. In some cases they occur as bands of single cavities, twisting and curving about without any very definite connexion, as shown by fig. 32; or they are scattered promiscuously through the entire crystal. e. Expansion of fluids by heat. By the experiments described above, I have shown that, at the temperature at which they are formed, the fluid-cavities in crystals are full of the fluid, and that, if they be examined at a lower tempe- rature, they contain vacuities, owing to the contraction of the fluid on cooling. Hence I think it is only reasonable to conclude that, provided the temperature were not known, it might be ascertained approximately by determining what increase of heat would be re- quired to expand the fluid so as to fill the cavities. In some cases this can be learned by direct experiment ; but generally it cannot, and we must have recourse to calculation. From the nature of the case the temperature is that required to cause the liquid to expand so much that the increase in volume is equal to the size of the vacuity. Taking, then, the volume of liquid for unity, and representing the relative sizes of the vacuity by V, it is easy to perceive that, if the law of the expansion of the liquid were known, and the value of V had been ascertained by observation, the temperature could be cal- culated. In order to be able to do this, I have (June 1858) made an ex- tensive series of experiments to ascertain the law of the expansion of water and saline solutions up to a temperature of 200° C. (392° F.). This I did by hermetically enclosing the liquid in strong glass tubes about 2 inches long and =,th of an inch internal diameter, and heating them in a bath of parafiine, with such arrangements that the inerease in vclume could be measured, by means of a micrometer microscope, to within the ,)5oth of an inch. This, however, is not the place for anything but the general conclusions. By appropriate experiments and calculations, I find that the increase in volume may be represented very accurately by an expression of the form V=Bt+C?’, where ¢ is the temperature in degrees Centigrade, and B and C constants, the value of which depends upon the nature of the aqueous solution. Perhaps, indeed, in reality there may be terms involying higher powers of ¢ than ¢’; but if so, they are ne nearly H al A62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. compensated for by the unequal expansion of the mercury of the thermometer itself, by the expansion of the glass tube, or the com- pression of the liquid by the rapidly increasing tension of the vapour, that their value up to 200° C. is so small that they do not produce any clearly marked effect in the results. The action of water on glass at temperatures above 200° C. is so powerful that I was unable to determine the volume at a greater heat; but from 25° to 200° there is such a very close agreement between calculation and expe- riment that I think the formula would give sufficiently accurate approximations to the truth up to at least 300°. The law does not hold good near the freezing-point ; but that is of no consequence in the present inquiry. The following are the actual values for water and various saline solutions, the volume at 0° C. being taken for unity :— LI) \WENIGUSS Bie nenan cbse en aloe co OS aes Deericinn oe V = '0001344¢+--00000324572 2. ,, with 10 p.c. of chloride of potassium .. V=‘0001868¢-+--0000025242? 3. 4, 4, 25p.c. of chloride of potassium.... V=*0003006¢-+-'00000141072 a 12% p.c. of chloride of potassium-+ a ; ° é 122 p. c. of chloride of sodium.. ie 00052800 5. 5», 4, 29p.c. of chloride of sodium...... V=-0003520¢+--0000013702? Goss. », 25 p.c. of sulphate of soda........ V =:0003077¢+-0000016442? do vony yy 20 Pe C. Of mixed salts beme the |», - ; 2 mean. of 3, 4, 5, & R. ee ae }v= 00032212-+ 0000014617 On examining this table, it will be seen that the addition of salts to the water increases the value of the coefficient of ¢, but decreases that of ¢; thus causing the expansion to be more uniform, by making it greater at low, and at the same time considerably less at high, temperatures. As far as I have been able to ascertain, the most trustworthy experiments indicate that the product of these coefficients is nearly constant, and that the increase in the value of the coefficient of ¢ varies in simple proportion to the quantity of salt in the solution, the amount of water bemg taken as constant. Pro- bably these laws are not strictly correct, but still sufficiently so to enable us to determine the effect of variation in the strength of the solution as accurately as is requisite for the purpose of the present paper. d. Lffects of pressure. These conclusions of course apply to those cases where the pressure to which the liquid is exposed is only equal to the elastic force of the vapour ; but since, in nature’s laboratory, crystals have no doubt often been formed under very great pressure, it will be necessary to take into account the compression of the fluid. The amount of this has been determined with great accuracy by a number of observers (Gmelin’s Handbook of Chemistry, Cavendish Society’s Translation, vol. ii. p. 62); but I would particularly refer to the paper of M. Grassi (Annales de Chimie, t. xxxi. p. 437). He there shows that the amount of compression of pure water, for a pressure equal to one atmosphere, is *0000502, but decreases as the temperature in- creases. It is less for saline solutions, but increases as the tempera-. SORBY=4,,th of an inch. § 2. Water contained in crystals. The difference between the water mechanically enclosed in the fluid-cavities of a crystal, and that chemically combined with the sub- stance of which it is composed, is of course most complete. That chemically combined is one of the essential constituents of the mineral, cannot be seen with any kind of magnifying power, and is probably not in the state of liquid water; whereas that in the fluid- cavities is altogether unessential to the existence of the substance, and is in the form of a visible liquid, merely enclosed mechanically. _ When a mineral! contains fluid-cavities, of course it does not neces- sarily follow that the fiuid is water ; and it is often difficult to ascer- tain what it is when 27 the cavities. If, however, the mineral contains ‘no chemically combined water, it is easy to prove what it is when out of the cavities. On applying a strong heat, the expansion of the. 470 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. fluid, or the elastic force of the vapour, bursts the cavity and often causes the crystal to fly to pieces with great violence. When sub- sequently examined with the microscope, it is seen that the fluid has been expelled ; and in order to ascertain whether or not the fluid thus given off is water, I adopt the following method. I havea glass tube 8 inches long and with a 2-inch bore, closed at one end; and, having placed in it fragments of the mineral dried at 100° C., I fill the tube with air dried by passing over chloride of calcium. ‘The open end is then closed with a well-dried cork, and the other passed through two holes in the opposite sides of a small box containing a mixture of pounded ice or snow and salt, so as to project about a couple of inches. A sufficiently strong heat is then applied to the closed end, containing the fragments, to expel the fluid from the cavities. If they contained water, it is condensed as small crystals of ice on the cold part of the tube; and when the whole has cooled, it is with- drawn from the box and placed in a strong solution of common salt, at a temperature several degrees below the freezing-point of water, and the form of the enclosed crystals examined with a magnifying glass. By carefully noticing the rise of a thermometer as the solu- tion of salt becomes warmer, the temperature at which they cease to be solid and pass into a liquid is easily ascertamed; and if it be found that the crystalline form and melting-point of the liquid thus given off from the fluid-cavities are the same as those of water, I think we may safely conclude that the liquid seen in the cavities is water or some aqueous solution. § 3. Minerals contained in Secondary Rocks. a. Rock-Salt, Calcite, Se. In proceeding now to apply the above general conclusions to the investigation of the circumstances under which natural crystals were formed, it will be best to commence with rock-salt, since its peculiar structure can be imitated artificially with perfect accuracy. it often contains excellent fluid-cayities, which, besides a fluid, sometimes enclose a variable, and often a considerable, quantity of mud. On the whole, the specimens I have examined do not contain much of this substance; and in the solid parts of the crystals the cavities are full of liquid. Hence the salt must have been deposited very slowly from solution in more or less muddy water, at a heat not very considerably, if at all, higher than the ordinary temperature of the atmosphere, unless it was formed under a very great pressure. Much the same conclusions apply to the selenite in gypseous marls ; but most of the cavities have lost fluid by drying,—which need not surprise us, since it contains combined water and has a very laminar structure. 7 When pure calcite containing no fluid-cavities is heated, it does not decrepitate, and gives off no water; but when it contains fluid- cavities, the crystals fly to pieces and give off water, and I therefore conclude that the fluid in the cavities is water. I have found many excellent fluid-cavities in the calcite of modern tufaceous deposits, in SORBY—STRUCTURE OF CRYSTALS. 471 that of the veins in limestone, and in many trappean rocks ; also in fluor spar, in the sulphates of baryta and strontia, and in several other minerals found in ordinary veins, as if they had been deposited from solution in water. In most of the cases I have examined, the vacuities in the normal fluid-cavities are very small ; and, unless they were formed under great pressure, the temperature must have varied from that of the atmosphere up te about that of boiling water. Much, however, remains to be determined ; and the variations in tem- perature have too local a connexion to be considered in this paper. 6. Quarte-veins. Since the facts to be learned from the study of the fluid-cavities in quartz are extremely interesting, I must describe them in some detail. As is well known, they are occasionally of considerable size, so as to be perfectly visible to the naked eye, and contain bubbles that moye about like those in spirit-levels. The fluid contained in them was proved by Sir H. Davy (Philosophical Transactions, 1822, p- 367) to be nearly pure water; and my own experiments confirm that conclusion. I froze the fluid in a cavity about 4th of an inch in diameter in a transparent crystal, and found that it thawed exactly at the thawing-point of ice. When clear quartz containing no fluid- cavities is heated in a tube, no water is given off; but that with fluid-cavities gives off a fluid condensing, at a low temperature, into crystals whose form and thawing-point are the same as those of ice. Besides this water, there is often another substance given off, which condenses as a solid nearer to the hot end of the tube than where-the water is deposited. I have ascertained that this is chloride of potas- sium or sodium. The water also often has a strong acid-reaction, due to hydrochloric acid, either derived from the decomposition of the above-named salts by the heated quartz, or, as is certainly the case in some instances, existing in a free state in the fluid-cavities. Tn order to ascertain the nature of the salts dissolved in the fluid in the cavities, I reduce the carefully-washed crystals to powder, so as to break open the cavities, and then dissolve out the soluble salts with distilled water. When rendered quite clear by filtermg and standing for some days, on evaporating this solution to dryness, the nature of the salts can be ascertained by the microscope and appro- priate chemical tests. In this manner I have found (July, 1858) that the fiuid in the cavities often contains a very considerable quan- tity of the chlorides of potassium and sodium, the sulphates of pot- ash, soda, and lime, and sometimes free acids. This explains why I was not able to freeze the fluid in some rock-crystal from Ceylon, containing very excellent fluid-cavities of about ;{)th of an inch in diameter, at a temperature of about —20° C. (—4° F.); for though, according to my own observations, pure water in tubes less than =}5th of an inch in diameter does not freeze till the temperature is reduced to about —15°C. (3° F.), it freezes at once at that temperature in those of the diameter of these fluid-cavities. It also serves to explain the amount of expansion by heat. I had ascertained from most ex- 472 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. cellent data, that the vacuities were uniformly very nearly *141 of the enclosed liquid at 0°C.; and therefore, calculating from the results of my experiments, if the fluid had been pure water, it would have expanded so as to fill the cavities at 189°C. However, on heating a portion of the quartz in a bath of paraffine, so arranged that it could be examined with the microscope, I found that at 217° C. very mi- nute bubbles were still visible in the fluid-cavities ; but at 220° they ‘had most certainly disappeared. We may therefore conclude that the fluid expands so as to fill the cavities at a temperature of from 218° to 219°. On reducing some of the crystal to powder, I obtained so much of alkaline chlorides and sulphates that I do not think they could amount to less than 15 per cent. of the fiuid in the cavities. They could not amount to above 30 per cent. ; or else crystals would have been deposited in the cavities. If in equation (3) we substi- tute the values of B and C, previously determined for a solution containing 25 per cent. of mixed alkaline chlorides and sulphates, we obtain t= /684462V + 12144—110........ equation (8) and substituting in this the value, V="141, we find <=219°4. Cal- culating from the laws of the variation due to a difference in the amount of salt in solution, if less or more than 25 per cent., the value of ¢ would be reduced; so that, if 20 or 30 per cent., it would be 218°. If therefore, as is probable, the fluid in the cavities is a strong solution, the temperature determined by calculation almost exactly agrees with that previously ascertained by actual experiment. It is seldom that the size of the cavities is sufficiently large to enable me to verify my calculations in this manner ; for the experiment can- not be made when very high magnifying powers are requisite ; but the agreement in this case is so remarkable as to cause me to have very considerable confidence in those that cannot thus be verified. Equation (8) of course gives the temperature requisite to expand the fluid so as to fill the cavity, and does not indicate the tempera~ ture at which the crystal was formed, unless the pressure was only equal to the elastic force of the vapour. This true temperature is expressed by substituting the value of V given by equation (2), in (8), when we obtain a v+ 00000271 | | i= / oasaea? + COON 12144—110 .. equation (9) which, of course, becomes (8) when p=0. Some quartz contains cavities enclosing two immiscible fluids, like those otcurring in Brazilian topaz, described by Sir David Brewster (Transactions of the Royal Society of Edinburgh, vol. x. pp. 1 and 407). Since, however, their peculiarities have been so well explained by him, and they occur so rarely in quartz as to be quite an excep- tion to the general rule, I need not do more than refer to fig. 52 as an illustration of their general character. They appear as if they contained two bubbles, one inside the other, owing to the fluid which has a less refractive power containing a bubble, and collecting itself SORBY—STRUCTURE OF CRYSTALS, 473 into a globular form. Since the bubble moves about in the central fluid, and this also moves in the exterior fluid, both must be liquids; and I very strongly suspect that further research will prove that one is water and the other a condensed gas. In determining the relative size of the vacuities in fluid-cavities, of course, care must be taken not to make use of such as have caught up bubbles of gas along with the fluid, which is more likely to hap- pen with large cavities than with small. There is also a greater risk of the large coming across flaws in the crystal, so as to lose fluid. The very minute should, however, be avoided, as being too much affected by the cohesion of the liquid to the sides. It is therefore best to select those of moderate size, which have vacuities of very uniform relative magnitude, in parts where vapour- or gas- cavities do not occur and the erystal is very solid. Sometimes we may dis- tinctly see that the quartz has been cracked, and the cracks after- wards filled up with quartz. This, like the formation of the large veins described below, appears in some cases to have taken place at a lower temperature, and explains why bands of cavities occasionally occur with vacuities relatively less than those in the fluid-cavities of the general mass. As already mentioned, whenever it is possible, such tubular cavities should be chosen as that represented by fig. 50. In the trachyte of Ponza there occur veins of quartz, as described by Scrope (Transactions of the Geol. Soc. 2nd ser. vol. ii. p. 208). These contain many fluid-cavities with water holding in solution the chlorides of potassium and sodium, the sulphates of potash, soda, and lime, and free hydrochloric acid. In this case we may, I think, conclude that the pressure was not very great, so that v= V, and the relative size of the vacuities would indicate the temperature at which the crystals were deposited from the aqueous solution. The mean of many good observations is v=*143, which, when substituted in equation (8), gives == about 220° C. (428° F.). At this tempe- rature the elastic force of the vapour of water is, from (7), equal to 292 feet of rock. | The quartz of the veins in Cornwall has precisely the same structure as the above in every respect; the fluid-cavities contain the same salts in solution; and at a great distance from the granite, making no allowance for pressure, the relative size of the vacuities indicates the same temperature, but if the pressure was great, a still higher. On approaching the granite, the temperature and pressure appear to have been much greater ; for the relative size of the vacuities in the fluid-cavities in the quartz of the veins is nearly the same as in those in that of the granite itself. Thus, the mean of the means for the quartz of the granite at St. Michael’s Mount and Mousehole is v='148, and for the quartz of the associated quartz-veins, also containing mica, tin-ore, wolfram, and other mine- tals, v='133. In cases like this, 1 think we may consider the pres- sure equal for both, so that the difference of the temperature may be calculated by means of equation (9). If the pressure was no greater than the elastic force of the vapour, these facts indicate that the quartz.of the veins crystallized at a temperature not more than 474 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 16° C. lower than that at which the quartz of the granite itself ery- stallized; but, as I shall show below, it is far more probable that the pressure was very great, and the temperature a dull red heat visible in the dark, and, if so, substituting in (9) the value, p=43,100, deduced from equation (10), given further on, I calculate by equa- tion (9) that the difference in the temperature must have been about 13°. These results clearly show that a great variation in the actual temperature and pressure produces only a small variation in the cal- culated difference in temperature. Perhaps some may think such cal- culations an impossible refinement ; but the facts appear sufficiently distinct to warrant them. Ina similar manner I find that the quartz first deposited in a vein in granite at Camborne indicates a tempe- rature quite equal to that at which the granite crystallized ; but in the quartz deposited towards the close of the process the relative size of the vacuities is so much less that the temperature must have fallen fully 30° or 40° C., which is quite probable. The number of the fiuid-cavities in the quartz of veins is often very great, as if it had been deposited rapidly. They are frequently on an average less than ;,'55th of an inch apart, which corresponds to upwards of a thousand millions in a cubic inch; and they are the chief cause of the very usual whiteness of the mineral. As an illus- tration of their forms, I refer to figs. 49, 50, and 51. Fig. 49 is of very irregular shape, whilst fig. 50 is a tube extremely well fitted for determining the relative size of the vacuity with great accuracy. Clear and transparent crystals contain few or none, as if deposited far more slowly; and very often crystals, which at their base are white and opaque on account of the number of cavities, are clear and trans- parent at their extremities from containing very few, as though, like what so very commonly happens in making artificial crystals, depo- sition proceeded rapidly at first, but much more slowly towards the close of the process. The form and arrangement of the fluid-cavities are also in every respect analogous to those in crystals prepared arti- ficialty ; and every peculiarity in the structure of the quartz of veins, and their relation to the granite, can be most completely ex- plained by supposing that it was deposited from water holding vari- ous salts and acids in solution, at a temperature varying from about 200° C. to a dull red heat visible in the dark. In those cases where we must suppose a very high temperature and a great pressure in. order to explain the relation between the fluid-cavities in the quartz of the veins and in that of the granite itself, such other minerals as mica, felspar, and tin-ore were often deposited, especially towards the commencement of the process, as if water at a very high temperature were the effective cause of their production. Tin-ore contains many excellent fluid-cavities, though they are usually very small *. Of course these conclusions do not apply to all quartz, for, as I have shown, some must have been deposited from nearly pure water ; * These deductions are strongly confirmed by the fact, that several of the above- named minerals have been formed artificially by the action of water at tempera- tures similar to those just described.—Senarmont, Ann. de Chimie, 3° sér. t. xxxii. p. 129; Daubrée, Ann. des Mines, 5° sér. t. xii. p. 289.—Oct. 1858. SORBY—STRUCTURE OE CRYSTALS, 475 and that associated with chalcedony in veins or in cavities contains very few fluid-cavities with relatively small vacuities, indicating a slow deposition from water at a much lower temperature, § 4. Metamorphic Rocks. In some portions of the granite containing large crystals of felspar at Trevalgan, near St. Ives, Cornwall, the felspar has been more or less completely removed, and its place filled with quartz, mica, or schorl, either alone or variously mixed. These most interesting and important pseudomorphs appear to have been almost entirely over- looked ; though I have found them in so many other localities in Corn- wall that they cannot be very rare. The removal of the felspar from the centre of the surrounding, fine-grained granite, and the introduc- tion of the quartz, mica, and schorl, cannot I think be explained except by the action of water. In this quartz are many very interest- ing fluid-cavities, and in some parts nearly all contain small cubic crystals, as shown by fig. 53. In other cases, besides such cubes, there occur prismatic crystals, like in fig. 55, or more rarely rhombic, as fig. 54. Occasionally the angles of the cubic crystals are corroded and rounded, as shown by fig. 55; and some cavities, as fig. 56, are so full of crystals that their form cannot be determined. The quartz also contains gas- or vapour-cavities, and every connecting link be- tween them and the other cavities. In all respects therefore the structure of this quartz is analogous to those crystals that are formed artificially above the surface of a hot liquid, and exposed alternately to water and air. When reduced to powder, water dissolves out much chloride of sodium, and a good deal of sulphate of lime, and hence the cubic crystals in the fluid-cavities are no doubt chloride of sodium, and perhaps some of the prisms may be selenite. Even if the effects of pressure are supposed to have been not material, the relative size of the vacuities indicates a heat of 220° C.; but, since the relative size of those in the fluid-cavities in the granite is nearly the same, in accordance with the principles described below, the pressure was pro- bably very great, and the temperature nearly or quite equal to a dull red heat, visible in the dark. It therefore appears, that to the action of water at a very high temperature, holding various salts in solution, must be ascribed the removal of the felspar, and the production of the mica, quartz, and schorl. In a paper read at the British Association (Report, 1857, p- 92), I showed that the material of the quartz and mica might be derived from felspar, decomposed by the removal of part of the alka- line bases ; and we thus have a key to those cases of metamorphosis where deposits of decomposed felspar-clays have been converted into crystallized mica and quartz, so as to constitute mica-schist. In the bands of quartz in mica-schist and gneiss, which are as it were irre- gular concretions passing along the foliation, and in the carbonate of lime and iron sometimes associated with the quartz, occur vast num- bers of fluid-cavities containing water. The quartz mixed up with the mica, forming the chief constituent of the schist, also abounds with fluid-cavities; and I have even found them in some of the VOL. XIV.—PART I. 21 476 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. garnets. These facts led me to argue, in my paper on mica-schist already referred to (Report of British Association, 1856, p. 78), that the alteration of deposits of decomposed felspar into crystallized mica and quartz was not the effect of dry heat and a partial fusion, but was due to highly heated water disseminated through the rock. If so, it is no wonder that ordinary shales have never been converted into mica-schist artificially, by the mere heat of furnaces, since the condi- tions are not those met with in nature—water is absent. | The mean relative size of the vacuities in the fluid-cavities in the quartz of the slightly metamorphosed schists in Cornwall, at a con- siderable distance from the granite, is ‘125, which corresponds to a heat of at least 200° C. (392° F.); and therefore a considerable thickness of rock must have been raised to a high temperature. If the pressure was great, the temperature must have been still higher ; and on approaching the granite, the relative size of the vacuities indicates nearly as high a, temperature as that at which the granite itself was consolidated, which agrees with the gradual passage from gneiss to granite, and might be used as a strong argument by those who contend that some granites are only thoroughly metamor- phosed stratified rocks. The vacuities in the fluid-cavities in the mica-schist of the southern border of the Highlands of Scotland are relatively so small (v=-05) that, if they were formed under no great pressure, they indicate a temperature of only 105° C. (221° F.). It, however, appears to me far more probable that the heat was really as high as in the case of analogous rocks in Cornwall, but the pressure greater. If so, from equation (6) we deduce that the Highland rocks were metamorphosed under a pressure equal to about 23,700 feet of rock more than those in Cornwall, or probably when at a much greater depth from the surface; a result which is confirmed in a most remarkable manner by a comparison of the fluid-cavities in the elvans and granites. These conclusions only apply to when the quartz crystallized : it does not follow that the rock was never heated to a still higher temperature. § 5. Minerals and rocks formed by cooling from a state of agneous fusion. The most instructive glass-cavities that I have met with im natural minerals are those in the crystals of clear, transparent felspar con- tained in some of the pitchstone of Arran. Pitchstone, like obsidian and some artificial slags, consists of a glassy base, having no action on polarized light, in which are scattered small crystals that decom- pose it and show colours. The basis of the pitchstone surrounding the crystals of felspar is transparent, and nearly colourless, but contains vast numbers of minute, green, prismatic crystals, probably some variety of pyroxene, often arranged in radiate groups, which impart a deep green colour to the rock. These may be seen to great advantage in thin splinters, but the glass-cavities in the felspar can be studied to far greater advantage in thin sections of the rock. The surfaces of the crystals of felspar are in some cases irregular, SORBY-—STRUCTURE OF CRYSTALS. 477 and portions of the surrounding pitchstone project right into them. Such projecting portions of the glassy basis have often become en- closed in the solid crystal, in precisely the same manner as the fluid- cavities in crystals formed from solution in water, as shown by fig. 2. Fig. 57 is a very good example of one of the larger of these glass- cavities. The centre is full of glass, precisely like the general basis of the pitchstone, except that the groups of green crystals are not so large and well developed, whilst somewhat larger prisms than those in the centre are attached to the sides, as if deposited during the cooling of the glassy solvent. The accompanying bubble is no doubt the effect of the contraction of the glass before it became solid. Fig. 58 is an example of a smaller cavity, having all the green crystals attached to the sides. It also contains several bubbles, which is a fact very characteristic of glass-cavities, since it never occurs in fluid- cavities, except under very peculiar circumstances, seldom met with. A common kind of cavity is shown by fig. 62; but the very smallest of all contain no green crystals, like fig. 60, corresponding therefore to those very small fluid-cavities in which crystals have not been deposited from a supersaturated solution. Fig. 61 is a case where the bubble has been much distorted, and crystals project from the sides quite into it, proving that the crystals were deposited before the glass became solid. Besides these glass cavities, the felspar has caught up small, colourless, contemporaneously-formed, prismatic crystals, to which in some cases glass-cavities are attached. A very excellent example of these is shown by fig. 59; and it is a striking fact, that very nearly all the green, prismatic crystals have been deposited on the included large crystal. The felspar also contains bands of vapour-cavities, and it is near to them that cavities with several bubbles occur; but, at a distance from them, the glass- cavities almost always, if not invariably, contain a bubble from 3th to 4th the diameter of the cavity. In some cases, however, there are cavities like fig. 63, which do not contain the prismatic crystals or a bubble, being more like stone-cavities. In the pitchstone are also some dark crystals, not visible except in sections, which look extremely like augite. The glass-vavities in these do not contain the green crystals; and if the two minerals are the same substance, this fact agrees with what takes place in crystals formed from solution in water, the material being merely deposited on the sides, and not as independent crystals. They, however, con- tain bubbles, relatively of a smaller size than those in the felspar ; whilst the glass-cavities in another mineral, the exact nature of which I have not been able to determine, contain many green crystals, but no bubble, as shown by fig. 64, probably owing to these minerals contracting more than felspar in cooling from a high temperature. The analogy between these glass-cavities and fluid-cavities is there- fore in many respects very striking; and, as will be seen, their peculiar characters can be most perfectly explained, if we suppose that the glassy base, when in a state of fusion, acted like a solvent liquid and dissolved various mineral substances, which were deposited on cooling in precisely the same manner as crvstals are deposited on 212 478 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. the cooling of a saturated, aqueous solution. There is therefore, in my opinion, no more necessary connexion between the temperature at which the crystals were deposited from this glassy solvent and their own fusing-point, when heated alone, than between the tem- perature at which crystals are deposited from solution in water and their own fusing-point, even if they be fusible. In both cases, the only necessary connexion is, that the crystals could not be deposited in a solid form, except at a lower temperature than that at which they become liquid; but it might be any heat less than that high enough to cause the glossy solvent to be sufficiently fluid. These facts are of very great importance in the study of igneous rocks, and serve to explain several peculiarities in their structure. Such glass-cavities, however, differ essentially from fluid-cavities, in con- taining bubbles that never move, and do not change their place or disappear when the fragment containing them is heated, unless the heat is strong enough to melt the enclosed glass, which is more fusible than the felspar. The best examples of glass-cavities that I have met with in the erupted lavas of Vesuvius occur in the augite. One very excellent case is shown by fig. 65. They contain, at least, two kinds of crystals, which sometimes project beyond the general outline of the cavities, as shown in the figure, as if they were formed at the same time as the augite, and were caught up in it along with the fused material of the glass-cavity, which on cooling deposited other crystals, and by contracting gave rise to a small bubble. In some eases long prismatic crystals have been caught up in the augite, as shown by fig. 66, having two glass-cavities attached to them, one with a bubhle and the other without, which is not unfrequently the case in detached cavities, as if, like in some fluid-cavities, the cohesion of the sides had overcome the contraction of the melted glass. The leucite in-the lava of Vesuvius often contains many cavities, the material in which has to a great extent become crystalline, and therefore they are very commoniy stone-cavities. An example of one, partially stone and partially glass, is shown by fig. 68, which is somewhat analogous to those in the felspar of the pitchstone, repre- sented by fig. 63. Another form is shown by fig. 70, and a very curious, almost circular, flat cavity is seen in fig. 69, containing three different kinds of crystals ; whilst fig. 67 represents a crystal enclosed in the solid leucite, with a small stone-cavity attached to it. In no case have I seen decided bubbies in the cavities in leucite ; but their absence from cavities containing many crystals is easily explained, because many substances expand in crystallizing to such an extent as would compensate for the previous contraction from a high tem- erature. In the felspar of the trachyte of Ponza the cavities are all filled with stony matter, as shown by fig. 71. A very long tubular cavity is represented by fig. 72. ; The general arrangement of these various glass- and stone-cavities is precisely analogous to that of those in crystals formed artificially ; and, independent of the fact that, in all their essential characters, they are identical with the cavities in the crystals in artificial furnace SORBY—STRUCTURE OF CRYSTALS. 479 slags, their very nature proves the igneous origin of the minerals containing them. ‘This is especially the case with glass-cavities ; for nothing but igneous fusion could so liquefy the enclosed glass that perfectly spherical bubbles could be produced. Besides stone- and glass-cavities, the minerals of erupted lavas con- tain gas- or vapour-cavities, as if they had caught up small quantities of gases and vapours that were in contact with them; but I have never found any fluid-cavities, and hence the purely igneous origin of the characteristic minerals of erupted lavas appears to be com- pletely proved. The zeolites, however, occurring in the cavities of lava that has been exposed to the action of water since it was erupted, contain no glass- or stone-cavities, but a few fluid-cavities, as if de- posited very slowly from solution in water. The best examples I have met with are in the Arragonite in the lava of Vesuvius, which have the vacuities equal to about ;4,th of the fluid, corresponding to a temperature of 160° C. (320° F.). Precisely the same conclusions apply to far more ancient trappean rocks. The augite in some of the basaltic rocks of Scotland has the same characteristic structure as that in the modern lavas of Vesuvius. A very good example of a glass-cavity is shown by fig. 73, containing a bubble and many small crystals deposited on the sides of the cavity. In the case shown by fig. 74, many most distinct crystals have been formed on the sides, but it contains no bubble, whilst sometimes, as fig. 75, there is a bubble but no crystals. In the felspar of a porphyritic greenstone from Arthur’s Seat near Edinburgh, there occur many stone-cavities; but, like the felspar itself, they have undergone a great amount of alteration by the subsequent action of water. Fig. 76 is much like some of the cavities in leucite, whilst that shown by fig. 77 evidently contained a bubble like a glass- cavity, but it has been filled with the chloritic mineral that has been introduced by water into nearly all parts of the rock. In fact the microscope clearly shows that the amount of alteration effected by the action of water on these ancient voleanic rocks is very much more than is generally supposed; and rocks, which to the naked eye appear to contain only two or three minerals, are seen to be made up of ten or twelve. Some of these are the igneous minerals containing glass- or stone-cavities, and others are zeolitic minerals containing fluid-cavities, which indicate that they have been deposited from more or less heated water. The characteristic structure of the minerals of which ancient trappean rocks are composed is, therefore, so analogous to, or even identical with, that of the constituents of modern lavas, that the purely igneous origin of these ancient lavas appears to me to be completely established; but, at the same time, their present aspect is often to a very great extent due to the sub- sequent action of water. In fact they have frequently been as much metamorphosed by water as some stratified rocks have been by heat. The production of zeolites, by the action of the thermal springs at Plombiéres on the ancient masonry, strongly confirms these deduc- tions. (Daubrée, Annales des Mines, 5° série, t. xil. p. 289, and xill. p. 227.) 480 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. § 6. Minerals and Rocks formed by the combined operation of water and igneous fusion. a. Minerals in the blocks ejected from Vesuvius. As is well known, in the blocks ejected from Vesuvius during eruption, a large series of minerals occurs, which do not exist in the erupted lava. Many of these are found in the limestone blocks in the Conglomerate of Somma, and, as pointed out by Delesse (Bulletin de la Société Géologique de France, 1852, t. ix. p. 136), in their number and character they differ so much from erupted lava, that it is little probable that the rock was ever in a state of simple igneous fusion. This conclusion is completely borne out by the microscopical structure of the minerals, for they contain many fluid-cavities, as well as glass- and stone-cavities, indicating that they were formed by the combined action of water and igneous fusion. In the calcite associated with light green mica, I have found many very excellent fluid-cavities, as shown by fig. 78. When heated they give off water, and on reducing the spar to powder, water extracts the chlorides of potassium, sodium, and magnesium, and the sulphates of potash, soda, and lime. UHence I think there can be no doubt that the cubic crystals seen in the cavities are chloride of potasstum or sodium, and the fluid a concentrated aqueous solution of those salts. I have not been able to ascertain the relative size of the vacuities with great accuracy, but it is nearly 3th of the volume of the fluid. Similar cavities occur in the nepheline of ejected blocks, and they all contain one or more cubic crystals of chloride of potas- sium or sodium, as shown by figs. 79, 80, and 83, no doubt deposited from the fluid on cooling, like those seen in the cavities formed artificially (figs. 18 and 19). Occasionally there are crystals of some other substance, as in fig.79. I have very carefully determined the relative size of the vacuities, and find that it is about *28 of the fluid ; and it isso uniform as to forbid us from supposing that the vacuities are owing to a loss of fluid. In calculating the temperature in this and the other cases given below, I shall assume that the pressure was not much greater than sufficient to counteract the elastic force of the vapour, so that we may consider v=V, and make use of equation (8). Judging from the change in the amount of expansion produced by an increase in the amount of salt in the experiments already described, the temperature indicated by relatively large vacuities would be nearly the same when there was more salt than can be retained in solution at the ordinary temperature, as when there was only 25 per cent.; the small difference being singularly enough almost exactly compensated for by the increase in the bulk of the salt on crystallizing. This is a fortunate circumstance in this in- quiry ; since, when, as in the case of the fluid-cavities in many modern volcanic minerals, the vacuities and included crystals are relatively large, it is unnecessary to take anything into account but the relative size of the vacuities, and substitute their values in equation (8). In this manner I deduce that this nepheline and By oN ys : Ree i SORBY—STRUCTURE OF CRYSTALS. 481 calcite must have been formed at a temperature of about 340°C. (644° F.). Of course, if the pressure was greater than supposed, the temperature must have been still higher. Since then (Gmelin’s Handbook of Chemistry, Cavendish Society’s Translation, vol. i. p- 167) solid bodies begin to be dull red in the dark at 335°C., and bright red at 400°, this temperature would be that of a very dull red heat only just visible in the dark, at which, from equation (7), the elastic force of the vapour would be equal to a pressure of 1954 feet of rock. On heating the fragment containing the cavity shown by fig. 80 to a very dull red heat visible in the dark, it became as fig. 81. The small crystals had disappeared, and the vacuity and crystal had changed their places; thus proving that the cavity contained a liquid, and that the crystals were soluble in it. On heating to a very decided red heat, the cavity became as fig. 82; the fluid had disappeared, and the nepheline had partially fused and collapsed over the altered crystal. When another fragment containing the cavity, fig. 83, was heated to a dull red heat, the cavity lost its fluid, and the crystal melted into a globule, as shown in fig. 84. All these results agree perfectly with the supposition, that the fluid is an aqueous solution, and the crystals chloride of potassium or sodium ; and it will be seen that the expansion of the liquid is not sufficient to burst the cavities until the heat is that of redness, which agrees perfectly well with calculation, if we consider that the enclosed crystal was not all dissolved on account of being exposed to a high temperature for only a short time. All, or nearly all, the fluid- cavities contain the crystals, which are on an average equal to about 1rd of the bulk of the liquid, or about four times as much as is de- posited from a solution of chloride of potassium saturated at the heat of boiling water, and many times more than from a solution of chloride of sodium. This entirely confirms the conclusion derived from the size of the vacuity, since, to dissolve so large an additional quantity, a very high temperature would certainly be requisite. Some cavities, as shown by fig. 85, are as though many minute crystals had been deposited over their whole surface, except where prevented by the attached cube. Most excellent gas-cavities also occur in the same nepheline, as shown by figs. 86 and 87, being like bubbles of gas enclosed during the growth of the crystal, in the same manner as in some of the artificial crystals already described. Others, like fig. 88, are as if some highly compressed, heated vapour had been enclosed, and on cooling had condensed into small crystals. Such cavities can be distinguished from stone-cavities by the fact of being partially trans- parent in the centre. The same fragment of nepheline also contains excellent glass-cavities, figs. 89 and 90, in all respects analogous to those in crystals formed when melted stony matter is present. As will be seen, the outline is very obscure, and quite different from that of the fluid-cavities, and is rendered apparent chiefly by the small crystals. The difference is also strongly marked by the pre- sence of several bubbles, as shown by fig. 90. This glass-cavity was 482 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. in the same fragment as the fluid-cavity, fig. 80, and when heated to a verv dull red heat, it remained nearly as drawn. When, however, heated a little higher, the minute crystals disappeared, and the bub- bles changed their places ; whilst at the same temperature the fluid- cavity still retained its fluid. At the temperature at which the fluid was expelled, it became as fig. 91, where all the crystals had disap- peared, and the bubbles not only had changed their places, but two had coalesced. It is therefore clearly proved by experiment (April 1858) that, at a heat not sufficient to expand the fluid in the cavities so much as to burst them, the substance in the glass-cavities is melted, so as to dissolve the small crystals it had previously deposited on cooling more slowly, and permit a change in the position of the bubbles, all which results agree most perfectly with the supposition that the crystals were formed at a red heat visible in the dark, when melted stony matter, gases, vapours, and liquid water saturated with soluble alkaline salts, were all present and alternately in contact with the growing crystals, so that the conditions of fusion, sublimation, and solution were all united. In the idocrase forming along with calcite the general mass of a block ejected from Vesuvius, many fluid-cavities occur, which often contain so many crystals that it is difficult to determine their form. A very good exampleis givenin fig. 92, with crystals like those in the fluid- cavities in nepheline. Fig. 93 shows clearly that the relative size of the vacuities is very great. On an average, they are equal to one- third of the fluid, and therefore indicate a temperature of 380° C. (716° F.), or a decided red heat; at which temperature the elastic force of the vapour of water is, from equation (7), equal to the pressure of 3222 feet of rock. Similar cavities occur in hornblende, indicating a heat of 360° C. There are also very good fluid-cavities in the crystals of felspar found in the ejected masses of ice-spar. These contain many crystals of two or three kinds (as shown by fig. 94). On reducing the felspar to powder, I found the usual chlorides and sulphates, but besides these a very considerable quantity of the carbonates of potash and soda, and, therefore, probably the presence of these carbonates is the reason why the crystals in the cavities differ so much from those previously described, though in other specimens they are quite similar, all being cubes. As shown by fig. 95, the vacuities are very large, and of about the same relative size as those in idocrase, indicating a temperature of 380°C. Other cavities, like fig. 96, have caught up vapour or gas along with the fluid, in the same manner as sometimes occurs in artificial crystals ; whilst others are quite full of the gas or vapour, which in some cases has been condensed into crystals on cooling, so as to cover the sur- face, as shown by fig. 97, seen out of focus in the centre. The same crystal also contains most decided and excellent glass-cavities, like fig. 98, and others, as fig. 99, that have become to a great extent crystalline, and contain no bubbles ; both of which are very analogous to cavities in the felspar of the pitchstone of Arran. We are thus led to conclude that the peculiar minerals character- istic of the blocks ejected from Vesuvius were formed at a dull red SORBY—STRUCTURE OF CRYSTALS. 483 heat, under a pressure equal to several thousand feet of rock, when water containing a large quantity of alkaline salts in solution was present, along with melted rock and various gases and vapours. Whether or no the presence of this water was instrumental, or even essentially requisite, in producing some of the minerals, still remains to be proved; but I think no one could compare the drusy cavities in the ejected blocks with the crystalline cavities in the slags of fur- naces, without perceiving that the occurrence of various minerals, placed one over the other in regular order, is a most striking differ- ence, which could be accounted for most completely by the action of water. It would also probably serve to explain why, according to Daubeny (Treatise on Volcanos, 2nd edition, p. 236), the minerals most characteristic of the ejected blocks are never found in the erupted lavas, the crystalline minerals of which were apparently formed when no /zquid water was present. I therefore think we must conclude provisionally, that at a great depth from the surface, at the foci of volcanic activity, liquid water is present along with the melted rock, and that it produces results that would not otherwise occur. It may perhaps be thought that the spheroidal condition assumed by water in contact with highly heated substances, would explain why it might be present at a less depth, and under less pressures, than those I have described ; but it appears to me that water could not remain in the spheroidal state, unless the vapour could escape, and that the temperature it remains at is essentially connected with the boiling-point at the pressure to which it is exposed, and there- fore the permanent presence of water at such a high temperature necessitates a great pressure, even if it was in the spheroidal state. But I think no one who has made experiments on the subject, would think it possible for water in that state to enter into tubes less than zoooth of an inch in diameter. This, however, has constantly occurred in the minerals of the ejected blocks, and hence it appears to me almost demonstrated that it was not in the spheroidal state, separated by a layer of vapour, but in actual contact with the crystals at a high temperature, and under great pressure. The presence of genuine gas- and vapour-cavities side by side with the fluid-cavities, and the existence of so large an amount of salts in solution in the fluid, prove that the water was caught up in a liquid state, and not as vapour so highly compressed as to condense into an equal bulk of water (see Cagniard de La Tour’s paper, Annales de Chemie, 1822, t. xxi. p. 127); for in that case, since in the nepheline there is no gradual passage from. fluid-cavities to vapour- cavities, we should have to conclude that the two gaseous bodies were not mutually diffusible, and that a very large amount of various alkaline salts was present as vapour along with the vapour of water ; both of which suppositions are I think quite inadmissible. Perhaps some may suppose that possibly the water penetrated to the cavities long after the minerals were formed. This, however, would necessitate percolation through the solid substance of the crystals, a fact differing as much from percolation through a rock, or amongst the minute crystals of which such substances as agate 484 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. are composed, or even through the pores existing in imperfectly solidified metals, as the passage of water through solid glass would differ from its passage amongst closely-packed fragments of glass. Not only does this appear to me most improbable, but actually opposed by facts. In the first place, the proportion between the amount of fluid and the size of the cavities in the nepheline is so uniform that I cannot believe it to be the result of accident, as we should have to suppose if they were not all filled full at the same temperature. If, to overcome this difficulty, it be supposed that the fluid penetrated into the cavities when in a highly heated state, it would require it to have been at the same temperature as that at which I have supposed it entered in the same legitimate way that it enters into the fluid-cavities in artificial crystals. But, even then, the facts are against the supposition ; for, besides fluid-cavities, there occur gas-cavities like figs. 86 and 87 ; and though there is no abso- lute line of division between their form and that of the fluid-cavities, their general characteristic shape is very different, because, as in artificial crystals, in one case the crystal is moulded to the bubble of gas, whereas in the other the irregular growth of the crystal deter- mines the form of the cavity. Moreover, besides these gas-cavities, there are the bubbles in the glass-cavities, which never contain a fluid. If then we suppose that the fluid percolated through the solid crystal into the fluid-cavities, we are led to conclude that it selected these cavities like artificial fluid-cavities, but avoided those resembling artificial gas-cavities, and the vacuities in the glass-cavities, a conclusion which is so extremely unreasonable that we must reject the proposition that leads to it. b. Granitic Rocks. In some of the trachyte of Ponza of solid character, as if it had been formed under considerable pressure, there occur a few small crystals of quartz, forming one of the genuine constituents of the igneous rock, in every respect like those in many elvans and some granites that contain but little quartz. They can scarcely be distin- guished in the rock in its natural state, but are readily seen in a thin section. When I examined this (April 1858), I found that the quartz contains very excellent fluid-cavities, as shown by figs. 100, 101, and 102. There is no doubt that they contain a liquid, for the bubbles move about in it. They are usually very flat, like fig. 101, and, when inclined in particular positions, the transmitted light is totally reflected from the bubble, which therefore appears like a black opaque substance, as shown by fig. 102. By careful measure- ments, I find that the relative size of the vacuities is very nearly *30. Assuming then, that, like in the fluid-cavities in the minerals of ejected blocks, and in the quartz of the veins in the self-same trachyte, as well as in those in the quartz of elvans and granite, the enclosed fluid is a strong aqueous solution of alkaline chlorides and sulphates, I deduce, from equation (8), that the temperature at which the crystals of quartz in the trachyte were formed was at SORBY—STRUCTURE OF CRYSTALS. 485 least 356° C., which closely corresponds with the mean deduced from the fluid-cavities in the blocks ejected from Vesuvius. At this temperature the elactic force of the vapour of water is equal to about 2400 feet of rock, and therefore the quartz must have crystallized under that pressure, at least. Considering the nature of the rock, the pressure cannot, I think, have been very much more than that, though it must have been somewhat more, and then of course the calculated temperature would be higher; but it would require a pressure equal to upwards of 19,000 feet of rock to alter it to 400°C. If it was equal to about 4000 feet, the calculated temperature would be 360° C. (680° F.). This is a very dull red heat visible in the dark, and the elactic force of the vapour of water would be equal to 2500 feet of rock. It does not necessarily follow that the rock was finally consolidated under such a pressure, or at such a depth, since the strength of quartz is such, that, if the crystals had been formed at a considerable depth, they might be carried to a much less without the elastic force of the fluid bursting the cavities. ‘To completely fuse such a rock, a white heat is necessary; but I find that, when in a glassy state, thin fragments become soft enough to bend at a very moderate red heat, so that the temperature at which it became quite solid probably could not differ very materially from the dull red heat deduced from the fluid-cav:ties, the two independent facts strongly confirming each other. Along with these fluid-cavities occur most excellent stone-cavities, as shown by fig. 103, in every respect analogous to those in the crystals in slags, and especially like some in leucite; and it may easily be seen that they are small portions of the surrounding fel- spathic material of the trachyte, that have been enclosed in the growing crystals of quartz. That they were caught up when their substance was in a fused, or at all events in a soft state, is proved by the fact, that their form is related to, and they are moulded upon, the crystalline planes of the quartz; whereas, if they had been solid fragments, the quartz would have been moulded to their own form. It therefore appears to me to be completely proved, that these crystals of quartz were generated under similar physical conditions to those concerned in the development of the minerals of the ejected blocks, by the combined influence of a dull red heat, liquid water, and par- tially melted rock. The structure of the quartz of many elvans and some granites is in every respect analogous to that in the trachyte just described. The only sensible difference is that the fluid-cavities are seldom so flat, and gas- or vapour-cavities more numerous. The proof of the igneous origin of elvans is complete, for the stone-cavities are very well developed. Examples of these are shown by figs. 104, 105, 106, and 107, from the elvans near Penrhyn and Gwennap. As will be seen, fig. 104 is extremely like those in the trachyte, differing only in being of rather coarser grain, and in containing a long prism of schorl. Very often long hair-like crystals of that mineral occur in the quartz itself, sometimes attached to stone-cavities, as shown by fig. 106; like the crystals with attached stone-cavities in leucite, 486 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. fig. 67. Fig. 105 represents a cavity of more irregular shape, and fig. 107 is from an elvan of much coarser grain, and has a gas- or vapour-cavity attached to it. These gas- or vapour-cavities often occur in distinct bands, like those in augite and other volcanic minerals ; but sometimes they are mixed up with fluid-cavities, which in that case have bubbles of variable relative size, caused by the irregular combination of fluid and vapour in the same cavity ; whilst in other parts fluid-cavities occur alone, with vacuities of very uniform relative size. As in the case of artificial crystals, the form of the fluid-cavities is often related to the crystalline planes of the quartz, as shown by fig. 108. Fig. 109 is a fluid-cavity contaming prismatic crystals, which in some cases must certainly have been caught up during the growth of the quartz, and not deposited from the solution on cooling, for they often pass through the cavities, as shown by fig. 110, and appear to be schorl. The passage from elvans to granite is quite gradual, and this is also the case with the peculiarities in the microscopical structure of their constituent minerals. The quartz of granite often abounds with most excellent fluid-cavities, and as an illustration of this fact, I have in fig. 111 represented a portion of the quartz of the granite of St. Austel, which occurs as distinct crystals, precisely like that in the trachyte described above, and not as a residue of crystallization. In many granites the fluid-cavities are so numerous in the quartz, that on an average they are not above ;,5,th of an inch apart. This agrees with the proportion of a thousand millions in a cubic inch; and in some cases there must be more than ten times as many. They also really constitute a most important part of the whole bulk of the quartz, for sometimes they make up at least 5 per cent. of the volume; and I have found that the loss of water on heating the quartz of the granite of Cornwall to redness is on an average about 0-4 per cent. of its weight, which is equivalent to about | p.c. of its bulk. These fluid-cavities are not confined to veins of granite, or to that part near the junction with the stratified rocks, but are quite as numerous in the most solid rock, far away from the junctions; as though the fluid was not an accidental ingredient, due to the perco- lation of water to a fused mass naturally containing none, but as if it was a genuine constituent of the rock when melted. Their number varies very much in different granites, but hitherto I have found them in all specimens I have examined ; and, though there are ex- ceptions to the rule, yet on the whole they are more numerous in granites than in elvans, and in coarse-graimed, than in fine-grained granites *. The felspar of the Cornish granites is usually so opaque, on account of partial decomposition, that it is difficult to see the fluid-cavities. * This is especially the case near Aberdeen ; for in the quartz of the coarse- grained veins, having crystals of mica, felspar, and schorl several inches long, the fluid-cavities are so numerous, large, and distinct, that even with only a mode- rately high magnifying power they may be seen to greater advantage than in any other granite | have hitherto examined ; whereas in the rather fine-grained stone used in building, they are few, small, and obscure.—Oct. 1858. SORBY—STRUCTURE OF CRYSTALS. 487 Fig. 112 is one in this mineral, but they are undoubtedly very rare. Few also occur in this mica, but they are certainly sometimes met with, as shown by fig. 113, which is very flat and shallow. The presence of so many in the quartz, and of so few in the felspar and mica, is analogous to what occurs when a mixed solution of common salt and alum is evaporated, as already described ; and, when solu- tions of alum and chloride of potassium are evaporated side by side, the crystals of chloride of potassium are even more loaded with fluid- cavities than the quartz in granite, whilst some of the crystals of alum contain none. By many experiments, I have proved most conclusively that the fluid in the cavities in the quartz of granites and elvans is water, holding in solution the chlorides of potassium and sodium, the sul- phates of potash, soda, and lime, sometimes one, and sometimes the other salt predominating. Since the solution has often a most decided acid reaction before, or even after, having been evaporated to dryness, there must be an excess of the acids present. This oc- currence of free hydrochloric and sulphuric acid is, I think, a very interesting fact, when we bear in mind how very characteristic they are of modern volcanic activity. Sometimes the amount of salts dis- solved in the heated water was greater tnan could be retained in so- lution at the ordinary temperature, and cubic crystals of the chlorides have been deposited, as shown by fig. 114. Near the granite, this is also sometimes the case with the fluid-cavities in the quartz of metamorphic schists and quartz-veins, which cavities contain the same saline solution as those in the quartz of the granite itself, as if in all these cases the quartz had been deposited from the same liquid, which, at a greater distance from the granite, became more dilute, on account of being mixed with pure water. Besides the cubic crystals, the fluid-cavities in the quartz of granite occasionally also contain prismatic crystals, as seen in fig. 115, and therefore agree very closely with those in the blocks ejected from Vesuvius. There is often a considerable variation in the amount of crystals contained in the fluid-cavities in the same portion of quartz, as if the strength of the solution had varied during the consolidation of the rock; and there is also sometimes a passage from fluid- to vapour-cavities, as if there had been an alternation of liquid and vapour or gases; both of which circumstances would be likely to occur. The stone-cavities are not well developed, except in granites whose structure approximates somewhat to that of elvans. The most dis- tinct I have yet found are in the quartz of the granite of St. Austel, containing the fluid-cavities, fig. 111. They are entirely similar to those in the quartz of the trachyte of Ponza or of elvans, as will be seen on comparing fig. 117 with figs. 103 and 104. As I have already remarked, when some substances pass into the crystalline state they occupy more space than when melted, and therefore, if entirely enclosed in a solid substance, they might expand so much as to crack it, like we all know often happens when water freezes. This appears to have occurred in the cavity fig. 119, there bemg three cracks radiating from it, as drawn, This increase in the bulk of the 488 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. included stone, explains why there are no vacuities in the stone- cavities of granites and elvans. In the quartz of very coarse-grained granites the stone-cavities are generally obscure and of irregular shape, as shown by fig. 118. Those in the felspar are often so much obscured by the partial decomposition of that mineral, that it is difficult to distinguish them from small decomposed patches ; but in some very clear from the granite of Lamorna they are sufficiently distinct, and, as shown by fig. 120, are very analogous to those in the felspar of the trachyte of Ponza, figs. 71 and 72. Besides fluid- and stone-cavities, the quartz of granite often con- tains vapour-cavities, like those in minerals from modern volcanos. Some are almost perfect spheres, and exactly like enclosed bubbles of gas; but others are of more irregular shape, and gradually inter- fere with and pass into fluid-cavities, in the same manner as occurs in some of the minerals of ejected blocks, and in crystals formed ar- tificially by alternate exposure to liquid and the air. Some of these empty cavities may be fluid-cavities that have lost their fluid, but I have found them in specimens obtained on the sea-coast below low- water mark, which were afterwards kept under water and never dried, and therefore some must certainly be genuine gas- or vapour- cavities. On the whole, then, the microscopical structure of the constituent minerals of granite is in every respect analogous to that of those formed at great depths and ejected from modern volcanos, or that of the quartz in the trachyte of Ponza, as though granite had been formed under similar physical conditions, combining at once both igneous fusion, aqueous solution, and gaseous sublimation. The proof of the operation of water is quite as strong as of that of heat ; and, in fact, I must admit, that in the case of coarse-grained, highly quartzose granites there is so very little evidence of igneous fusion, and such overwhelming proof of the action of water, that it is im- possible to draw a line between them and those veins where, in all probability, mica, felspar, and quartz have been deposited from solu- tion in water, without there being any definite genuine igneous fusion like that in the case of furnace slags or erupted lavas. There is, therefore, in the microscopical structure a most complete and gradual passage from granite to simple quartz-veins ; and my own observa- tions in the field cause me to entirely agree with M. Elie de Beau- mont (Note sur les émanations volcaniques et. métalliféres, Bulletin de la Société Géologique de France, 2 série, t. iv. p. 1249) in con- cluding that there is also the same gradual passage on a large scale. My remarks respecting the possibility of the water having passed into the fluid-cavities in nepheline after they were formed, will, to a considerable extent, apply to the fluid-cavities in the quartz of elvans and granites. If they had contained nearly pure water, and were quite full, and easily lost it on drying, such a supposition would have been sufficiently probable. It is, however, not mere water, but va- rious saline solutions, with free acids, precisely like the fluid in the cavities of some modern volcanic minerals. Moreover, that a very great pressure will not cause water to pass through solid crystal, ex- SORBY—-STRUCTURE OF CRYSTALS. 489 cept by cracking it, is proved by the fact, that when the quartz from Ceylon, in which the fluid expands so as to fill the cavities at about 218° C., was heated to at least 350°, some of the fluid-cavities still retained their fluid, though, judging from the force calculated to be necessary to counteract the expansion of the fluid, they must have resisted a pressure equal to about 40,000 feet of rock. Also in my experiments in treating fragments of nepheline to a red heat, a thick- ness of only 4th of an inch must in some cases have resisted a pres- sure of several thousand feet. Since water has not penetrated into the vapour-cavities, or into the vacuities in the glass-cavities, in ancient trappean rocks, it should appear that a considerable pressure for a very long time will not cause it to pass through the solid substance of crystals. In my opinion this could only happen by the formation of actual cracks, which, as sometimes happens with cracked glass, were healed up by the adhesion of the sides, after the fluid had en- tered. This, however, would differ as much from the escape of the fluid when the crystal is strongly heated, as the breaking of an arch by a symmetrical pressure from above would differ from a fracture produced by a pressure from the inside; and, therefore, if fluid- cavities can resist so great a pressure from within, it appears to me that none at all probable could burst them from without. That the fluid remains permanently in many of the cavities in quartz, is, I think, proved by the fact that, when specimens are obtained below low-water mark on the sea-coast, and afterwards kept in water, the cavities are in no respect different from those in very thin fragments which have been kept dry for years. On the whole, in the absence of any proof of the contrary, I think these reasons are sufficient to warrant the conclusion that the aqueous solutions enclosed in the fluid-cavities in the quartz of granitic rocks, were caught up during the formation of the crystals, and have remained ever since, herme- tically sealed up in their solid substance, without any increase or diminution of the fluid ; and that therefore we may determine from their present condition the circumstances under which the rock was originally formed. In my opinion, the water associated with thoroughly melted igne- ous rocks at great depths does not dissolve the rock, but the rock dissolves the water, either chemically as a hydrate, or physically as agas. In the case of those obsidians and pitchstones which, when heated to redness, give off water having a strong acid reaction, it may probably be in the form of a hydrate, retaining its water when heated under pressure. It is also sufficiently probable that, as suggested by M. Angelot (Bulletin de la Société Géologique de France, 1 sér. t. xiii. p. 178), fused rock, under great pressure, may dissolve a con- siderable amount of the vapour of water, in the same manner as liquids dissolve gases. In either case, if the fused rock passed by gradual cooling into anhydrous crystalline compounds, the water would necessarily be set free ; and, if the pressure was so great that it could not escape as vapour, an intimate mixture of partially melted rock and liquid water would be the result. It is difficult to form any very definite opinion as to the actual amount of this water, and 490 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. to decide whether or no it exercised an important influence over the crystalline processes that took place during the consolidation of such rocks as grauite. The comparatively large quantity of alkaline chlo- rides and sulphates, dissolved in those portions caught up in the growing crystals, indicates that the amount cannot have been wn- limited ; but, bearing in mind the facts I alluded to when describing the fluid-cavities in the blocks ejected from modern volcanos, and knowing, as we do, that the action of highly heated water is so very energetic, 1 cannot think that its influence was unimportant. On the contrary, seeing that the fluid-cavities in the quartz of quartz- veins contain the selfsame salts and acids as those in the granite, as though it had been deposited from portions of the liquid which had passed from the granite up fissures, I think the amount, though limited, must nevertheless have been considerable, and that its presence will serve to account for the connexion between granite and quartz- veins, and the very intimate relation of both to the metamorphic rocks, and explain many peculiarities in the arrangement of the minerais in the cavities in granite or in the solid rock, even if it was not the effec- tive cause of their elimination and crystallization. These analytical de- ductions have been confirmed in a most striking manner by the ad- mirable experiments of M. Daubrée (Observations sur le métamor- phisme, &c., Annales des Mines, 5° sér. t. xii. p. 289), who, in having produced felspar and quartz artificially, by the action of water at a similar temperature to that I have deduced from the fluid-cavities, has removed some of the principal objections that might have been urged against my conclusions. I therefore must confess myself to be a very strong adherent to the views of Scrope (Treatise on Vol- canos ; and on the nature of the liquidity of lava, Quarterly Journal of the Geological Society, vol. xii. p. 338), Elie de Beaumont (Note sur les émanations volcaniques, ut supra), and Scheerer (Discussion sur la nature plutonique du granite, &c., Bulletin de la Société Géolo- gique de France, 2 sér. vol. iv. p. 468, and vol. vi. p. 644), though, as will be perceived, I by no means agree with them in every par- ticular. ce. Temperature and pressure under which granitic rocks have been formed. In studying the fluid-cavities in elvans and granite, it is particu- larly necessary to bear in mind the influence of pressure. As already shown, the temperature requisite to expand the fluid so as to fill the cavities is that at which the crystal was formed only when the pres- sure was not greater than the elastic force of the vapour, and when in equation (9) p=0; but if the pressure was very great, that tem- perature would necessarily be far short of the actual heat. There- fore, as already described, the true heat can only be determined when the approximate value of the pressure is known; and the pressure cannot be deduced unless we can in some way or other approximate to the temperature. The trachyte of Ponza was probably formed under so small a pressure that it scarcely need be taken into account ; but, in the case of granites, such a supposition would lead to the con- SORBY—STRUCTURE OF CRYSTALS. 491 clusion that sometimes they did not solidify from a state of fusion until the temperature was as low as that of boilirg water. In the present state of the inquiry (July 1858), it therefore appears to me that the best course is to suppose that the quartz of the various igne- ous rocks crystallized at about the same temperature, and that the greatest value of v yet observed, viz. in the trachyte of Ponza, was when p was not so great as to prevent the value °3 being a sufficiently accurate approximation to V to be substituted in equation (6), so as to enable us to calculate the value of p from the observed value of v by the equation p=369,000 2—” iro Considering the very strong analogy between the structure of this trachyte and that of elvans and granites, this supposition appears to me quite admissible as an approximation until a more correct is known. Of course the results deduced from the equation are the amounts of pressure in feet of rock, and not the actual depth. In some cases the pressure was probably much greater than that of the superin- cumbent rocks, for otherwise they could not have been fractured and elevated ; whereas in other cases it may have been much less, if the internal pressures had been in any way relieved. Fortunately, a con- siderable variation in the strength of the saline solutions in the fluid- cavities would be to a great extent compensated for, because, though a more dilute solution would expand more by heat, it would be more compressed by pressure. Moreover, according to the principles de- scribed by Mr. James Thompson (Transactions of the Royal Society of Edinburgh, vol. xvi. p. 575), which have been strikingly verified by the experiments of Professor Wm. Thompson on the thawing of ice (Philosophical Magazine, 3rd ser. vol. xxxvil. p. 123), by those of Bunsen on spermaceti and paraffine (Poggendorff’s Annalen der Physik und Chemie, 1850, vol. Ixxxi. p. 562), and by those of Hop- kins and Fairbairn on spermaceti, parafline, sulphur, and stearine (Report of the British Association for 1854, p. 57),—if a substance expands in solidifying, it would become solid at a lower temperature when under a greater pressure; whereas if it contracts, it would solidify at a higher temperature. Therefore if, as I have already shown, the stone-cavities in the quartz of granite indicate that the general fused mass from which the quartz crystallized expanded in the act of solidification, it would probably become solid at a lower temperature when under greater pressure. We may, however, be nearly certain, that at very great pressures the compression of water would be relatively less than at moderate ; for, if not, a finite pressure would compress it into nothing; and therefore, since the force re- quired to produce this relatively less compression of the liquid, which was not so much expanded by the lower temperature, might be nearly the same as would produce the greater compression of the more heated and expanded liquid assumed in the above equation, it is ob- vious that these two sources of error have a tendency to counteract one another, and therefore perhaps the equation would give a tole- VOL. XIV.,—PART I. 2K eg 2 «<2 @ equation (10), 492 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. rably accurate approximation to the truth when the pressure was very great, as well as when only small. Even if the real amount of the compression of the highly heated liquid differed from that supposed to be the most probable, the difference would affect all the results in similar proportion, and therefore, though not actually correct, they would be sufficiently accurate as compared with each other. The chief point about which there may be some doubt is whether, when the rock contains much quartz, it became crystalline at a higher temperature than when it contains less. I have, indeed, found cases where there was evidence of the first-formed quartz having crystal- lized at a higher temperature than the last, but the facts were scarcely . sufficiently decided to be fully relied on, and in the present state of the inquiry this cannot be accurately taken into account ; nor, indeed, if mean results are employed, do any other facts seem to require that it should. That even highly quartzose elvans and granites did not become finally solid at a temperature much higher than a dull-red heat, is, I think, clearly proved by the great number of hair-like crystals of schorl enclosed in the quartz; for schorl readily melts at a bright-red heat, and therefore must have crystallized at a lower _ temperature than that. ‘The properties of the pyrognomic minerals described by Scheerer (Discussion sur la nature plutonique du granite, &c., uf supra) indicate a temperature not higher than a brown-red heat. It therefore appears to me in the highest degree probable that granites and elvans became finally solid at about the dull-red heat calculated from the fluid-cavities in the quartz of the trachyte of Ponza. Still, however, taking everything into consideration, the following deductions must only be looked upon as the best approxi- mations that can be made at present, for so many data are only im- perfectly known. : From the nature of the case, equation (10) gives the excess of pressure over and above that under which the quartz of the trachyte of Ponza crystallized, whatever, within moderate limits, the real temperature and pressure might be. If then we consider these to have been 360° C., and 4000 feet of rock, that amount would have to be added to the calculated value of p, in order to obtain the total pressure. The greatest value of v that I have yet found for any elvan is for one at Gwennap, in which it is very nearly ‘25. This, from equa- tion (8), indicates a minimum temperature of about 320° C. (608° F.), or very little lower than a dull-red heat visible in the dark. Sub- stituting this value of v in equation (10) we obtain p=14,100 feet, to which, as explained above, must be added 4000 teet to arrive at the total pressure, which was therefore about 18,100 feet. The least value of v for any elvan in Cornwall is -125, for that at Swan- pool, near Falmouth, which corresponds to a pressure of 53,900 feet. The mean of my observations in the elvans of Cornwall gives a pres- sure of 40,300 feet; but, for the analogous quartzose porphyry-dykes in the Highlands of Scotland, 69,000 feet. I have never yet found any granite in which v is greater than *2, which is the relative size of the vacuities in that of St. Austel. This SORBY—STRUCTURE OF CRYSTALS, 493 indicates a minimum temperature of 256° C. (493° F.), and a pres- sure equal to about 32,400 feet of rock, or considerably less than some of the elvans. In the Cornish granite I have never found v less than :09, in that from the Ding Dong mine near Penzance, which corresponds to a pressure of 63,600 feet; and the mean of all my observations gives 50,000 feet, or 9700 feet more than the mean for the elvans. This, I think, is a very satisfactory result, since the association of those rocks clearly proves that granite must have been consolidated at a considerably greater depth than elvans. _ The. conclasions derived from my examination of the various granites in the neighbourhood of Aberdeen are very striking. In the main mass, at a considerable distance from the stratified rocks, v=about :04 ; and the great difference between vacuities of that size and those in the fluid-cavities in the quartz of the trachyte of Ponza will be seen on comparing fig. 116 with fig. 100, both magnified to the same extent. if the pressure were not taken into account, this would indicate a temperature lower than that of boiling water; but if the temperature was the same as that at which the quartz of the trachyte of Ponza crystallized, the pressure must have been equal to about 78,000 feet of rock. If the temperature was higher, the pres- ‘sure must have been still greater. In the exterior part close to the stratified rocks v=-071, which indicates a pressure of 69,000 feet. This is the same as for the porphyries, but 9900 feet less than for the centre of the granite, which appears to me a very reasonable result, since it is extremely probable that the pressure on the outside would be considerably less than in theinterior. In some more recent veins of very coarse-grained granite intersecting the other, v=‘166, which corresponds to a pressure of only 42,000 feet, as though the condi- tions under which it was consolidated differed materially from the other case, either on account of the elevation of the rocks, or some other physical change. The general mean of all my measurements in the main masses of granite in the south border of the Highlands from Aberdeen to Ben Cruachan indicates a pressure of about 76,000 feet, or 7000 feet more than the quartzose porphyry-dykes. The number of cavities is also much less than in those granites formed under a less pressure, as if the crystallization had taken place more slowly, on account of a more gradual cooling, which would probably be the case, if the thickness of the superincumbent rocks was greater. Comparing these conclusions and that derived from a comparison of the metamorphic rocks, we have as under :— The granites of the Highlands indicate a pressure of 26,000 feet of rock more than those of Cornwall. The elvans of the Highlands indicate a pressure of 28,700 feet of rock more than those of Cornwall. The metamorphic rocks indicate a pressure of 23,700 feet of rock more than those of Cornwall. This remarkable agreement cannot be the result of mere accident, but I think clearly pomts out that the consolidation of the granites and elvans, and the metamorphosis of the stratified rocks, took place _In the Highlands at a very much greater depth than in Cornwall,— 494 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, a conclusion which appears to me to agree extremely well with the general association of facts on a large scale. Of course all the pressures deduced as above involve any error there may be in the amount of compression supposed to be the most probable for highly heated water, and would be materially altered by variations in the temperature; but, considering all the circum- stances of the case, it appears to me as likely that they are too little as too great, and, therefore, at present we cannot do better than adopt them provisionally. | In order that the various results may be compared more conve- niently, I subjoin the following Table. The first column gives the temperature in degrees Centigrade requisite to expand the fluid so as to fill the cavities, if the pressure was not greater than the elastic force of the vapour, which, of course, is the lowest temperature at which the rock can have been consolidated, since the excess of pres- sure could not be less than nothing. In the other column is given the pressure in feet of rock requisite to compress the fluid so much that it would just fill the cavities at 360°, being, therefore, the actual pressure, if in each case the rock was consolidated at that temperature. Tempera- ture. Pressure. Drachyte ot Ona. coneasee = beets shen sers Sal csgeesseame neuer 356 4,000 Balan aut: Gvy OM Ap waieisis.ay i caslesio us Maaeeeessaciasa ros eeistamiamey cenady 320 18,100 Granite at St. cAmstel vse, semen. asec abiosiisloneentenmaute as ae 32,400 Mean-of the Corimish €lvanis, 420 acssorecascaveeaenccasdons® 250 40,300 More recent veins of granite at Aberdeen .........s00.6. 245 42,000 Mean of Cornish granites ....... a SRO Cee. Tae EN aeat 216 50,000 Elvan at Swanpool, near Falmouth...............ceseecees 203 53,900 Granite from the Ding Dong Mine, near Penzance .... 162 63,600 Mean of the Highland porphyry-dykes..............see00 135 69,000 Exterior of the main mass of the granite at Aberdeen 135 69,000 Mean of the-Highland granites stc.ntscacsctedssencntenees 99 76,000 Centre of the main mass of the granite at Aberdeen... 89 78,080 It wili thus easily be seen that, if pressure is not taken into account, there is a gradual decrease in temperature on passing from trachyte to granite ; whilst if, asis far more probable, the temperature was nearly the same, the pressure increases in passing from trachyte through elvans to granite; and I think all geologists will agree with me in thinking that this is a very satisfactory result. It therefore appears that the fluid-cavities indicate that all the elvans and granites I have hitherto examined were consolidated under pressures varying from about 18,000 to 78,000 feet of rock. These are certainly very great pressures; dut, bearing in mind that they probably represent the forces concerned in the elevation of mountains, I think they are sufficiently reagonable. ‘They also cor- respond very well with the pressure under which, in many cases, the lava at the Zoci of modern volcanic activity must become solid, as is well illustrated by the Peak of Teneriffe. It is upwards of 12,000 feet high, and the bottom of the ocean from which the volcanic dis- trict of the Canary Islands rises is 12,000 feet deep, and at no great distance westward it is 16,800 feet (Lieut. Maury’s Physical Geo- SORBY—STRUCTURE OF CRYSTALS. 495 graphy of the Sea, Ist edition, plate xi.). If, as is sufficiently pro- bable, the lava at a great depth extends some distance westward of the exhibition of volcanic activity at the surface, there must be a considerable thickness of rock between it and the bottom of the ocean, or else it could not, as it does, resist the pressure of a column of lava at least 20,000 feet high, when an eruption takes place from the Peak. If a few thousand feet is sufficient for that purpose, when the internal forces are relieved by an eruption of lava near the summit of the Peak, there would be a pressure of an actual column of at least 30,000 feet of melted rock on the lava at the base. Pro- bably, however, part of the lava is at a greater depth than a few thousand feet below the general bed of the ocean, and the pressure may be more when not relieved by an eruption, and therefore it ap- pears to me reasonable to suppose it might in some cases be solidified under double that pressure. At all events the best conclusions we can deduce from this modern volcano agree so well with the amounts calculated from the fluid-cavities in granitic rocks, that I cannot but conclude that the pressure under which granites and elvans were consolidated was of the same order of magnitude as the pressure under which the lava of modern volcanos must be solidified at the foci of their activity, as though these rocks were the unerupted lavas of ancient volcanos, variously protruded amongst the superincumbent Strata. As is well known, the temperature of rocks increases with the depth ; and it becomes an interesting question to determine whether the rate of increase might give the temperature deduced from the fluid-cavities in the quartz of the trachyte of Ponza, at a depth which would correspond with the amount of pressure deduced from a com- parison with those in the quartz of granite. According to M. Cor- dier (Edinburgh New Philosophical Journal, 1828, vol. iv. p. 275), the rate of increase is not uniform in all countries, being in some as rapid as 1° F, for each 24 feet, and in others not more than 1° for each 104 feet, as if owing to an regular distribution of the subter- ranean heat. If the increase was the same for great depths, there would be a temperature of 680° F. at a depth varying from 15,100 to 65,500 feet. According to Mr. R. W. Fox (British Association Report for 1857, p. 96), the rate of increase in various mines in Cornwall is by no means uniform, but varies from 1° for each 32 feet to 1° for 71 feet, being on an average 1° for 49 feet, which would give a temperature of 680° at a depth of 30,900 feet. However, he states expressly that the increase is more rapid in shallow than in deep mines; and, according to information -kindly furnished to me by Mr. Robert Hunt, the rate is 1° for every 50 feet in penetrating through the first 100 fathoms; for the next 100 fathoms 1° for 70 feet ; whilst, when the depth exceeds 200 fathoms, it is only 1° for each 85 feet of depth. If this be the true rate of increase far below the surface, there would be a temperature of 680° F. at a depth of about 53,500 feet. These results will be best compared with the pressures under which granites were most probably formed, by means of the following Table ;— 496 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Depth in Feet. | Pressure in feet of Rock. Cordier’s results ....... 15,100 to 65,500 | Various granites .... 32,400 to 78,000 F@x'S' Med 52) ., dissovenetscuses 30,900 Cornish granites .... 32,400 ,, 63,600 Flint’ s results. 6%, cebinodis 53,500 Mean of ditto, .seccsscces se 50,000 It will thus be seen that, if the rate of increase to a very great ‘depth is the same as near the surface, the calculated temperature would occur at a less depth than corresponds with the calculated pressure, although the general order of magnitude of the two quan- tities is very similar ; whilst, if the rate of increase to a very great depth is the same as below 200 fathoms, it would occur in Cornwall at a depth which corresponds remarkably well with the calculated mean pressure for the granites in that district. Very variable ele- ments enter into the calculations; there are many possible sources of error; the number of feet of rock expressing the pressure might differ very considerably from the actual depth, and the distribution of heat in the earth’s crust, when the granite was consolidated, might not be the same as now. Still, however, we must admit that the rate of increase in the heat of the rocks indicates that the tem- perature at which the quartz of granite probably crystallized would in all probability occur at a depth agreeing very well with the pres- sure to which it appears to have been exposed. Since, then, as I have already shown, the metamorphic rocks near the granite cry- stallized at about the same temperature as the granite itself, 1 think, even if we do not give our entire assent, we must acknowledge that _ the above fact is a strong argument in favour of the supposition that the temperature concerned in the normal metamorphosis of gneissoid rocks was due to their having been at a sufficiently great depth beneath superincumbent strata. ' It will, therefore, be seen that the application of the principles I have described leads to many very striking and remarkable results, which agree so extremely well amongst themselves and with other general circumstances, that I cannot for one moment believe them to be the effect of accident. On the contrary, they clearly point to definite laws ; and though, in the infancy of such a wide subject, in- volving many very difficult physical questions, considerable errors cannot be avoided, yet the character of the results indicates that the general principles are correct. With respect, then, to minerals and rocks formed at a high tem- perature, my chief conclusions are as follows. At one end of the chain are erupted lavas, indicating as perfect and complete fusion as the slags of furnaces, and at the other end are simple quartz veins, having a structure precisely analogous to that of crystals deposited from water. Between these there is every connecting link, and the central link is granite. When the water intimately associated with the melted rock at great depths was given off as vapour whilst the rock remained fused, the structure is analogous to that of furnace slags. If, however, the pressure was so great that the water could not escape as vapour, it passed as a highly heated liquid holding different materials in solution up the fissures in the superincumbent rocks, and deposited various crystalline substances to form mineral ‘ s . ’ £ - ‘i 3 a ‘ . “Big Fs : : 4 i : My ‘ « 4 e > aw : : ” - _ * 7 L oe rt 4 Oy: Quart. Journ.Geol. Soc Vol XIV. PLXAVL bo 6 i = rae as Ail 0 qreg i MY: 45 q “! r a : ; 0/4 Ly vr rare}: Qils'tq, O Oo: Pause eae teem at eens a] odo TE Ag. yas iy: if] H.Cc.SCR AVY BEL ET. LETH. SL RUGTURE: oF LORS EAs « ‘SORBY—STRUCTURE OF CRYSTALS. 497 veins. It also penetrated into the stratified rocks, heated, some- times for a great thickness, to a high temperature, and assisted in changing their physical and chemical characters, whilst that re- maining amongst the partially-melted igneous rock served to modify the crystalline processes which took place during its roguoldatian. These results are all derived from the study of the microscopical structure of the crystals; but my own observations in the field lead me to conclude that they agree equally well with the general struc- ture of the mountains themsely es, and serve to account for facts that could not have been satisfactorily explaimed without the aid of the microscope. And here I cannot but make a few remarks in conelu- sion on the value of that imstrument, and of the most accurate physics in the study of physical geology. Although with a first- rate microscope, having an achromatic condenser, the structure of such crystals and sections of rocks and minerals as I have prepared for myself with very great care can be seen by good day-light as distinctly as if visible to the naked eye, still some geologists, only accustomed to examine large masses in the field, may perhaps be disposed to question the value of the facts I have described, and to think the objects so minute as to be quite beneath their notice, and that all attempts at accurate calculations from such small data are quite inadmissible. What other science, however, has prospered by adopting such a creed? What physiologist would think of ignoring all the invaluable discoveries that have been made in his science with the microscope, merely because the objects are minute? What would become of astronomy if everything was stripped from it that could not be deduced by rough calculation from observations made without telescopes? ‘With such striking examples before us, shall we physical geologists maintain that only rough and imperfect methods of research are applicable to our own science? Against such an opinion I certainly must protest ; and I argue that there is no necessary connexion between the size of an object and the value of a fact, and that, though the objects I have described are minute, the conclusions to be derived from the facts are great. DESCRIPTION OF PLATES XYVI. to XIX. The number of times that the objects are magnified in linear dimensions is expressed by the sign X. The figures with a dotted outline are portions of crystals, and the rest are entire separate cavities and crystals. PLATE XVI. CAVITIES IN CRYSTALS FORMED ARTIFICIALLY. § L. From solution in Water. Fig. 1. A single crystal of chloride of potassium deposited on slow evaporation in winter. X60. Fig. 2. A portion of the edge of a crystal of chloride of sodium, x 200, showing how the fluid-cavities are formed. Fig. 3. A fluid-cavity in chloride of potassium formed at the ordinary tempera- ture. X 800. Figs, 4, 5. Fluid-cavities in chloride of sodium formed at the ordinary tempe- rature. 4, X800; 5, 1000. 498 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. = 6. A portion of a crystal of chloride of potassium formed at 100° C. x 150. g. 7. A-fluid-cavity in chloride of sodium formed at 100° C. 400. Ties, 8, 9, 10. Fluid-cavities in chloride of potassium formed at 100° C. 8, x300; 9, x400; 10, x 200. Figs. 11, 12, 13. Fluid-cavities in chloride of sodium formed at 100° C.,ina strong solution of bichromate of potash. 11, 13, x1000; 12, «600. Figs. 14, 15, 16. Crystals of bichromate of potash and attached fluid-cavities, in chloride of sodium formed at 100° C., in a concentrated solution of the bichromate. 14,15, X100; 16, x70. Fig. 17. A fluid-cayity in chloride of sodium formed at 100° C., in a concen- trated solution of bichromate of potash. x 800. Figs. 18, 19. Fluid-cavities im chloride of sodium formed at 100° C., in a strong solution of chloride of potassium. 18, x800; 19, x 1200. Fig. 20. A fluid-cavity in chloride of sodium formed at 100° C.,in a strong solution of hydrochloride of ammonia. x 800. Figs. 21, 22. Fluid-cavities in nitrate of potash formed at the ordinary tempe- rature. 21, X400; 22, x 200. Fig. 23. A fluid-cavity in binoxalate of ammonia formed at the ordinary tem- perature. 150. Figs. 24, 25. Fluid-cavities in sulphate of zinc formed at the ordinary tempe- rature. X130. Pratt XVII. Fig. 26. A portion of a crystal of alum formed at 60° C. 100. Figs. 27, 28. Fluid-cavities in alum formed at 50° C. 27, x100; 28, x400. Fig. 29. A gas-cavity in a portion of a crystal of alum formed at 50° C. x50. Figs. 30, 31. Fluid-cavities in alum that have lost water by drying. 30, x 800; 31, x 400. Fig. 32. A portion of a crystal of bichromate of potash, with bands of fluid- cavities. X 200. Fig. 33. A fluid-cavity in bisulphate of potash, which totally refiects the trans- mitted light. x 200. Figs. 34, 36, 37. Fluid-cavities in chloride of sodium formed above the level of the liquid at 100° C. 34, x800; 36, 37, x1000. Fig, 35. A gas-cavity in chloride of sodium formed above the level of the liquid at 100° C. x600. § 2. Formed by Sublimation. Fig. 88. A gas-cavity in hydrochlorate of ammonia. 600. Fig. 39. A gas-cavity in corrosive sublimate. x 400. § 3. Formed from a state of Igneous Fusion. Fig. 40. A portion of a crystal of basic silicate of protoxide of iron, from a cop- per slag. x 200. Figs. 41, 42, 48. Glass-cavities in a portion of a crystal of basic silicate of prot- oxide of iron, from a copper slag. 41, x1600; 42, x 400; 43, «600. Figs. 44, 45. Part alass-, part stone-cavities in a portion of a erystal of basic silicate of protoxide of iron, from a copper slag. 44, 1200; 45, X1600. Fig. 46, A stone-cavity in a portion of a crystal of basic silicate of protoxide of iron, from a copper slag. x 1600. Fig. 47. A stone-cavity in pyroxene, from a blast-furnace slag. 800. Fig. 48. A glass-cavity in Humboldtilite, from a blast-furnace slag. 400. FLvuiIp-Csv ITrES IN NATURAL MINERALS. Figs. 49, 50, 51. In quartz of a vein at Mousehole, near Penzance. 800. Fig. 52. A fluid- -cavity containing two fluids, in the quartz of a porphyry at Cove, near Aberdeen, X 2000, Quart.Journ .Geol.Soc.Vol. XIV.PIXVII. a g a5 i i ae e Oy : Pa Na load adie _ > , H.G.SORBY DEL.ET.LITH Se Galera Joo) GAweS TALS . ee ee. = ye Quart.Journ Geol.Soc. Vol. XIV. Pl. XVII. HG. SORBY DEL ET ATH: ST RUCTURA) or CRMs Rie Journ.Geol.Soc . Vol_XIV. PL X Dae H.C.SORBY DEL.ET.LITH. STRUCTURE. or ovis iste SORBY-—STRUCTURE OF CRYSTALS, 499 Figs. 53, 54, 55, 56. Fluid-cavities containing various crystals, in quartz re- placing felspar, at Trevalgan, near St. Ives, Cornwall. 53, x1600; 54, 55, 56, x800. Pratt XVIII. GLASS- AND STONE-CAVITIES IN THE MINERALS OF ERUPTED LaAvas, &e. Figs. 57, 58, 59, 60, 61, 62. Glass-cavities in the felspar of a porphyritic pitch- stone in Arran. 57, X300; 58, X330; 59, x360; 60, x1600; 61, X600; 62, 400. Fig. 63. A cavity of a different character in the felspar of a porphyritic pitch- stone in Arran. X600. Fig. 64. A glass-cavity in a prismatic crystal in a porphyritic pitchstone in Arran. 300. Figs. 65, 66. Glass-cavities attached to crystals in the augite of tho lava of Vesuvius. 65, x500; 66, 400. Fig. 67. A stone-cavity attached to a crystal in the leucite-of the lava of Vesuvius. 300. Figs. 68, 69, 70. Stone- and glass-cavities in the leucite of the lava of Vesus vius. 68, x600; 69, 70, x800. Figs. 71, 72. Stone-cavities in the felspar of the trachyte of Ponza. 800. Figs. 73, 74. Glass-cavities in the augite of a trappean rock at Balloch, Dum- barton. 78, X450; 74, x 600. Fig. 75. A glass-cavity in the augite of a trappean rock near Glasgow. 600. Figs. 76, 77. Altered glass- or stone-cavities in the felspar of a porphyritic greenstone at Arthur’s Seat, near Edinburgh. 76, x400; 77, x 200. Fiuip-, Gas-, VAPOUR-, STONE- AND GLASS-CAVITIES IN MINERALS FORMED BY THE COMBINED ACTION OF WATER AND IGnzEovUsS FUSION. Fig. 78. A fluid-cavity in the calcite of a block ejected from Vesuvius. 300. Figs. 79, 89, 83, 85. Fluid-cavities in the nepheline of a block ejected from Vesuvius. 1000. Figs. 81, 82, 84. Fluid-cavities in the nepheline of a block ejected from Vesu- vius, after haying been heated to a more or less bright red heat. Figs. 86,87. Gas-cavities in the nepheline of a block ejected from Vesuvius, in a natural state. 86, x1000; 87, 400. Fig. 88. A vapour-cavity in the nepheline of a block ejected from Vesuvius, x 8900. ; PLATE XIX. Figs. 89, $0. Glass-cavities in the nepheline of a block ejected from Vesuvius. 89, x400; 90, X1200. Fig. 91. The cavity, fig. 90, after having been heated to bright redness. Figs. 92, 93. Fluid-cayvities in the idocrase of a block ejected from Vesuvius. x 1200. Figs. 94, 95. Fluid-cavities in the felspar of a block ejected from Vesuvius. 94, x800; 95, X1600. Fig. 96. A fluid-cavity in the felspar of a block ejected from Vesuvius, with much enclosed vapour. 500. Fig. 97. A vapour-cavity in the felspar of a block ejected from Vesuvius, out of _ focus in the centre. 500. Fig. 98. A glass-cavity in the felspar of a block ejected from Vesuvius, out of focus in the centre. x 400. Fig. 99. A stone-cavity in the felspar of a block ejected from Vesuvius, out of focus in the centre. 500. Figs. 100, 101. Fluid-cavities in the quartz of a trachyte from Ponza. 100, x2000; 101, x800. Fig. 102, A fiuid-cavity in the quartz of a trachyte from Ponza, x1600, so placed that the bubble totally reflects the transmitted light. Fig. 103. A stone-cavity in the quartz of a trachyte from Ponza. x 400. 500 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Figs. 104, 105. Stone-cavities in the quartz of an elvan near Penrhyn, Cornwall. 104,. %250; 103, x 800. Fig. 106. A stone- -cavity attached toa crystal of schor! i in the quartz of an elvan near Penrhyn, Cornwall. x 400. Fig. 107. A stone-cavity attached to a vapour- or gas-cavity in the quartz of an elvan near Gwennap, Cornwall. x 800, Fig. 108. A fluid-cavity in the quartz of an elvan near Gwennap. X 2000. Figs. 109, 110, Fluid-cavities in the quartz of an elyan near Gwennap, enclosing or attached to crystals of schorl. 1200. Fig. 111. A portion of the quartz of the granite at St. Austel, Cornwall, x 200, with many fluid-cavities, and one vapour- or gas-cavity. Fig. 112, A fluid-cavity in the felspar of the granite at Penrhyn, Cornwall. x 1600. Fig, 113. A fluid-cavity in the mica of a granite-vein at Polmear Cove, Corn- wall. <1600. Figs. 114, 115. Fluid-cavities in the quartz of the granite from the Ding Dong Mine, near Penzance. 114, x 2000; 115, x800. Fig. 116. A fluid-cayity in the quartz of the main mass of granite at Aberdeen. x 2000. Fig. 117. A stone-cayity in the quartz of the granite at St. Austel. x 1000. Fig. 118. A stone-cavity in the quartz of a rather coarse-grained granite near Cape Cornwall. x800. Fig, 119. A stone-cavity in the quartz of the granite at St. Austel, with ra- diating cracks. 600. Fig. 120. A stone-cavity in the felspar of the granite at Lamorna, near Pen- zance. 800 THE QUARTERLY JOURNAL OF THE GHOLOGICAL SOCIETY OF LONDON, PROCEEDINGS OF THE GEOLOGICAL SOCIETY. FEeBRuARY 3, 1858. Viscount Dufferin, Dufferm Lodge, Highgate, and Clandeboye, Co. Down, the Rev. Fred. Smithe, M.A., Churchdown, Gloucester- shire, and the Rev. W.A. Jones, M.A., Taunton, were elected Fellows. The following communication was read :— On the Succession of Rocks in the NortHERN HiGuHLanps, from the oldest Gneiss, through stRaATA of CAMBRIAN and LoweEr SILURIAN AGE, fo the Otv RED SANDSTONE inclusive. By Sir R. I. Murcuison, F.RB.S., V.P.G.S., &c. [Abstract.] {The publication of this Memoir is postponed. | THIs memoir comprised a general sketch of the succession of the stratified rock-masses occupying the northernmost counties of Scot- land (Sutherland, Caithness, and Ross), as determined by former observations of Prof. Sedgwick and the author, and of Macculloch, Jameson, Cunningham, Miller, and Nicol, and by the recent disco- veries of Mr. C. Peach. In the commencement, Sir Roderick, having referred to the long-held opinion that the great mountainous masses of red conglomerate and sandstone of the west coast were detached portions of the Old Red Sandstone, alluded to Mr. C. Peach’s dis- covery (in 1854) of organic remains in the limestone of Durness, which led the author to revisit the Highlands (accompanied by Prof. Nicol), when having found still more fossils, he expressed his 502 PROCEEDINGS OF THE GEOLOGICAL society. ([Feb. 3, conviction (at the British Association, Glasgow Meeting, 1854) that the quartzites of Sutherland and their subordinate limestones were of Lower Silurian age; and was strengthened in the opinion (which he had already published) that large portions of the cry- stalline rocks of the Highlands would prove to be the equivalents of the Lower Silurian deposits in the South of Scotland. In 1856 Colonel James and Prof. Nicol separately observed the unconform- - able overlap of the great conglomerates by the quartzite series ; and the latter geologist ereatly | extended all previous observations, and communicated to the Society a memoir, showing that the old gneiss and its superposed conglomerate, as seen along a very exten- sive region of the western coast, formed the buttresses upon which all the crystalline quartz-rock and limestone of the western parts of Ross-shire and Sutherland reposed. At the same time Prof. Nicol hypothetically suggested, that, until the evidence of fossils was more complete, the quartzite and limestone might be considered as the equivalent of the Carboniferous series of the South of Scotland. Another hypothesis, which had been propounded by the late Mr. Hugh Miller, regarded the quartz-rocks and hard limestones of Sutherland merely as the metamorphosed representatives of the Old Red and Caithness series of the astern Coast. Both of these hypotheses, however, seemed to the author to be incompatible with the physical order of the rock-masses in question ; for, according to the observations made long ago by Prof. Sedgwick and himself, the above-mentioned crystalline rocks, in the lower part of which the Durness fossils have recently been found, are the inferior members of the great undulating mass of micaceous and schistose rocks, which, rolling over to Caithness on the east, there constitute the basis out of which the bottom strata of the Old Red Sandstone are chiefly formed. Of late, Mr. Peach has, by his untirmg perseverance, obtained a still larger collection of fossils from Durness, and in better preserva- tion than those found in 1854, and Mr. Salter finds that this collec- tion of well-defined forms comprises genera belonging only to the Lower Silurian of North America. Hence all doubt is now dispelled ; and the author, following up the suggestions which he offered at the Glasgow Meeting of the British Association, describes in the present paper these rocks and their fossils ; defining the great unfossiliferous conglomerate-masses of Sutherland as of Cambrian age, the quartz- ites and limestones as Lower Silurian, and the ov erlying micaceous and gneissose schists and flagstones as also of Silurian age. In the body of the memoir, Sir Roderick, after a brief notice of the ‘“‘fundamental gneiss,” described the ‘‘ Cambrian red sandstone and conglomerate,” alluding to the faithful descriptions of it by Hugh Miller and Nicol. He also detailed certain subsequent observations of Colonel James and Mr. Peach on the unconformity of these rocks to the overlying quartzites, and on tke great dislocations exhibited in these masses ; and he also noticed the discovery of a porphyry between the gneiss and the conglomerate by the latter observer. 1858.] MURCHISON—NORTHERN HIGHLANDS. 503 The “ Lower Silurian rocks, in the form of quartz-rock, crystal- line limestone, chloritic and micaceous schists, and younger gneiss,” were then described. The fossils from the quartz-rock consist of small annelide-tubes, now named Serpulites Maccullochii, and traces of fucoids. These fossils were long ago noticed, but of late they have been traced in beds for great distances by Mr. Peach. The strong band of limestone between two quartz-rocks is estimated by Colonel James to lie about 800 feet above the base of the series, and is of great extent. The fossils * detected in it have been determined by Mr. Salter to be Maclurea Peachii, spec. nov. (and its curious twisted operculum), Ophileta compacta, well known in Canada, Oncoceras, spec., and Orthoceras, a smooth species with a compressed siphuncle. They all closely resemble fossils of the Lower Silurian rocks of North America, which range from the Calciferous rock up to the Trenton Limestone, both inclusive,—a group especially to be found in the limestones of the Ottawa River in Canada. Passing across Ross-shire in a more southern parallel, from Loch Duich in Kintail, on the west, to the frontier of the Old Red Sandstone on the east, the general succession of rocks was de- scribed to be much the same as that in North-west Sutherland, though there are considerable changes of lithological character when the same rocks are followed southwards or south-south-west upon their strike ; and the author stated his belief, that not only may the regularly bedded limestones which are intercalated in the chloritic and quartzose rocks of Dumbartonshire be classed with some of the oldest of those stratified masses which, like the limestones of Suther- land, are unquestionably of Lower Silurian age, but that the vast and evidently overlying masses of mica-schist and quartzose-gneissic flag- rocks of the Breadalbane district may be some day found to be simply the prolongations of the micaceous flagstones of the North-western Highlands above alluded to, as overlying the quartz-rock and fossili- ferous limestone: further, that in the still higher limestones and. schists seen on the banks of Loch Tay, we may speculate on the existence of the equivalents of younger and higher strata than any which are observed in the Northern Counties. After some observations on the truly stratified condition of these micaceous and gneissose schists (younger gneiss) of the Highlands, Sir Roderick proceeded to the consideration of the “Old Red Sand- stone of the North-east of Scotland,’”’—defining the tripartite division of this great series, and demonstrating that the beds with Cephalaspis Lyellii and Pterygotus Anglicus of Forfarshire really lie at the base of the series, and are certainly of greater antiquity than the bitumi- nous fossil-bearing schists of Caithness. This division is in accord- ance with the relations of the deposits of the Devonian period, as seen in Devonshire and Germany, though the lowest member of the Old Red of Scotland has no representative in the Devonian rocks of Russia. The Caithness flagstones were described as being in the middle of the series; whilst the underlying conglomerates and sand- * Twenty-three in all, 11 of which are identical with American forms.— Oct. 1858. , 504 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 24, stones were shown to be the true equivalents of the Cephalaspis-beds of Forfarshire, and of the lower cornstone-strata of Herefordshire, which there graduate downwards, through the tilestones, into the uppermost Silurian rocks of Ludlow. | The Old Red rocks of the North Highlands were described in some detail by the author, who showed that the group, as seen in Caithness and the Orkney Islands, is composed of—Ist, lower red conglomerate and sandstones; 2nd, grey and dark-coloured flag- stones and schists, both bituminous and calcareous (this portion being in Elginshire and Murrayshire represented by Cornstones) ; and 3rd, upper red sandstones. The North Scottish Old Red con- tains one great inferior portion which has no representative in the Devonian rocks of some foreign countries, though it is completely represented in all its parts in other tracts both of Britain and the Continent. Having next described the conditions under which many of the species of fish (at least twenty-one) found fossil in Caithness, Cro- marty, and Morayshire, occur in Russia commingled with the middle Devonian mollusks of Devon, the Boulonnais, and the Rhine, and having pointed out that the lowest member of the Devonian series, with its Cephalaspides, is wanting in Russia, Sir Roderick insisted on the importance of the Devonian series in the scale of forma- tions, and on the fact that the Old Red conglomerates, ichthyolitic schists, and cornstones, with the overlying sandstones, of Scotland and Herefordshire fully represent in time the Devonian rocks of the South of England and the Continent, so full of corals, crinoids, and marine mollusks. Some brief observations on the Newer Red Sandstone of the West Coast of Ross-shire, and the Lias and Oolitic deposits of the North of Scotland and the Western Isles, concluded this paper. Frepruary 10, 1858. ANNUAL GENERAL MEETING. [For Reports and Address see the beginning of this volume.] FEBRUARY 24, 1858. T. Ashford Sanford, Esq., Nynehead Court, Somerset; C. E. Austen, Esq., C.E., Grove House, Croydon; and Thomas R. Polwhele, Esq., Geol. Surv. Great Britain, were elected Fellows, The following communications were read :— 1. On the Grapvua Evevarion of the Coast of Siciiy from the mouth of the Stmreto to the ONOBOLA. By Gartano Giorei1o GEMMELLARO. Communicated by Sir C. Lyett, F.R.S.,F.G.S. _A RECENT alluvial soil which forms the plain of Catania is composed “of rolled blocks (cto¢toli) of sandstone, limestone, and basalt, with 1858.] . GEMMELLARO—SICILY. 505 clay and sand. Volcanic currents from Etna more or less recent, all augitic,—basalt, for the most part spheroidal and prismatic, a pleisto- ene formation which has succeeded to that of the Terre Forte of Catania, ancient prismatic and compact currents from Etna, recent alluvium from San Tecla to Mascali, formed of volcanic felspathic and augitic rocks—these elements constitute the topography of the coast of Sicily from the mouth of the Simeto to the Onobola. From the Simeto to the Sciarra del Principe it is difficult to find characteristic features in the recent alluvium, such as may mark the lapse of time. The Sciarra del Principe, a volcanic current of 1669 ; the shore at Catania, in which are seen pebbles of sandstone, recent lavas, and fragmentary matter; the Sciarra dell’ Armisi; that of the Crocifisso of Lognina; the current of 1361,—these form the coast to the neighbourhood of Lognina, and have been much changed from their primitive aspect, these materials beimg daily used in the con- struction of the mole at Catania. In the Scala di Lognina, from 4 decimetres to 1 metre above the level of the sea, among great blocks of lava which form the shore, one may observe a marine breccia, formed of small blocks of sand- stone, augitic lava, and fragmentary matter, cemented together by a calcareo-siliceous cement. From Lognina to Aci Castello, the volcanic currents which form the shore present nothing of interest. Here begins the basaltic current which came to the surface of the earth before the pleisto- cene formation ; and as far as the Capo de’ Molini, the study of the coast is interesting In every respect. ~ From the Pietra delle Sarpe, passing by the cotel/o to the cannito of S. Giuseppe, the front of the volcanic current of 1169 has a very compact structure, and forms a perpendicular cliff, showing in several points, and for several metres in height, a zone of corrosion, depending on the chemico-mechanical action of the sea-water. The lava, from the upper part of which the blocks come that are seen along the shore, shows itself with a very scoriaceous and irregular surface .at the height of from 8 decimetres to 1 metre above the level of the sea, which makes one suppose that the igneous current must once have touched the waters of the sea. Besides this, which is observed in all lavas which are in contact with the waters, it appears that we may also add the presence of many Serpule, which indicate that the current formerly touched the sea-water, and that it still preserves its primitive configuration. From the west of the Cannito of 8. Giuseppe to the basaltic rock on which the ancient castle is built, one may see the same volcanic current, which covers the spheroidal basalt, metamorphosed for 3 decimetres from its surface of contact. The south side of the rock, formed entirely of spheroidal basalt and piperino, being ina state of decomposition, falls continually, and presents nothing that is in- teresting for examination. To the north of the rock the same lava of 1169 is excavated and corroded at different heights; and at 2 metres above the level of the sea, we find adhering.a coarse shelly sand, in which may be dis- 506 PROCEEDINGS OF THE GEOLOGICAL Society. [Feb. 24, tinguished, almost in a normal position, Cyprea lurida, Lamk., Turbo rugosus, L., Patella cerulea, Lamk.(?), Patella scutellaris, Lamk., and Balanus balanoides, Rang. Along the shore from the Pietra degli Uccelli northwards there are a great quantity of blocks of prismatic lava, some of the size of 4 to 7 decimetres, perfectly rolled, and others subangular, masses of 1 and 3 cubic metres, to which adheres a shelly caleareo-marine deposit of the recent epoch. These blocks, thus rolled and subangular, are generally corroded on the surface by the chemical action of the chloride of sodium of the Sea-water ; and this condition extends for many metres above the sea-level to the northern side of the provincial road, in the farm of Signor Zappola and of Barone Sisto. Here these blocks rest on the pleistocene formation, which succeeds to that of the Terre Forte of Catania, and which is seen at Cefali, Leucatia, S. Paolo, and Catira ; they are generally 2 or 3 metres in thickness, usually corroded like @ wasp’s nest on the surface. At the height of about 14 metres above the level of the sea is an oval block, well rolled, 8 decimetres long and 4 wide, encrusted by Serpule. At a few paces from it is seen another block of prismatic lava of the enormous size of 7 cubic metres, about 13 metres above the level of the sea, also corroded on the surface by sea-salt, to the northern face of which Serpule@ are adhering; and in a crack was found a shell, which I believe to be Cardita calyculata, Brug., which is living on our shores. On the surface of the soil have been found many shells in a sub-fossil state, among which the most prevail- ing are Trochus Jragraoides, Lamk., Trochus articulatus, Lamk., Donazx trunculus, L., and Patella scutellaris, Lamk., which, although they have been generally referred to the pleistocene fauna, must be rather considered, as Sir C. Lyell pointed out to me on the spot, as shells of the more modern epoch or raised coast. To the south of Aci Trezza, a group of basalts raise their crests above the sea, and are commonly called the Faraglioni, or Cyclopean rocks, the largest of which is called the Island, or Taraglione grande, and on their surface they have clay more or less altered by the intru- sion of basalt. Beginning an examination of them from west to east, we first see the so-called Faraglionelli di Passaggio, which are, in my opinion, the most important in the researches in which I am occupied. On their sides we find attached large pieces of a calcareo-siliceous shelly marine deposit of the actual epoch, of which the highest is 5 metres 6 deci- metres above the level of the sea. It is everywhere bored horizon- tally by the Modiola lithophaga, Lamk., which is sometimes found entire, and sometimes in various states of alteration, Besides this, I have also found adhering the Lima squarrosa, Arca Noe, Cardita calyculata, Spondylus gederopus, Murex truncatus, Den- talium entale, Ostrea plicatula, Vermetus gigas, Vermetus triqueter, and many Serpule identical with those which liye on the correspond- _ing coast. The Faraglione of the Birds (degli Uccelli) presents also on its 1858. ] GEMMELLARO—SICILY. 507 sides fragments of the same calcareo-siliceous deposit, but less exten- sive. On the east side there is one patch entirely isolated, which, after great labour, I reached, up the perpendicular ascent of the decomposed rock. I measured the height, which is 11 metres 1 decimetre above the water. This fragment (lemdo), which marks one of the greatest heights in our coast above the sea in the present epoch, is isolated on the side of the basalt ; perhaps because the rock, having fallen into fragments, may have carried with it the lower part, which was its base. The basalt presents no lithophagous shells in its structure ; but corrosion is seen at some points, which depends, in my opinion, on the action of external agents, and chiefly those of the salts of sea-water, which continually tend to bring it down. The Pialsagia and the Faraglione del Mezio have also on their weathered sides patches and fragments of the same nature; and to the west of this last such patches are at considerable heights, and in the zone of the Modiola lithophaga, Lamk.; here we see adhering a very large Spondylus gederopus. The Faraglione grande at a certain height, im consequence of the continual giving way of its prisms, presents nothing of interest to the observer; whilst in the lower part we find patches of the usual calcareous deposit 4 to 6 metres above the sea. In the island we find interesting phenomena. On its sides are many fragments of the calcareo-siliceous shelly deposit more or less high above the level of the sea; here the argillolite and there the basalt show a zone of irregular corrosion some metres from the water. The island has large clefts, almost all directed from north to south. In the most western of these, on the sides, are great quantities of patches of calcareo-siliceous deposits, similar to those which are seen on the fianks of the other basaltic rocks, extending from the level of the sea to the height of 7 metres 8 decimetres, the maximum. These patches are horizontally bored by the Modiola lithophaga, Lamk., which is found in all periods of its organic development ; and we also find great part of the littoral shells now living on the coast. The argillolite, which forms the sides of this cleft above the before-men- tioned patches, is also bored for about 5 more metres by the Modiola lithophaga, Lamk. ; so that we have at this point one side bored by lithophagous shells, as high as almost 13 metres above the sea. In the great eastern cleft we find a marine breccia, formed of blocks of augitic lava, basalt, and argillolite, at the height of from 4 to 6 metres. In it there are great quantities of shells, which are in a fine state of preservation; among these many are adhering to the breccia in a normal position. UR Of these, the following species are identical with those now living on our shores :—Arca Noe, L., Cardita calyculata, Lamk., Patella cerulea, Lamk., Fissurella gibba, Phil., Monodonta corallina, L., Buccinum variabile, Phil., Rissoa calathisca, Trochus cingulatus, Brocchi, J’. Adansonii, Payr., Mitra lutescens, Lamk., Colombella rustica, L., Turbo neritoides, L., Cyprea lurida, L., Vermetus gigas, Biv., and others. The lateral walls of these clefts are bored by Modiola hthophaga VOL. XIV.—PART I. aL 508 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, regularly and horizontally, which holes are seen at the height of about 9 metres above the sea-level. Along the shore from Aci Trezza to Capo de’ Molini we may con- tinually observe, at the height of from 3 to 5 metres, large blocks of prismatic lava and basalt, rolled and blunted, the calcareo-siliceous shelly deposit, and marine breccia, formed of pebbles (ciottoli) of augitic lava, of basalt, and sandstone, and of gasteropodous and lamel- libranchiate shells. From this place to Aci Reale, the recent volcanic currents do not present any phenomena of interest. On the shore of the cliff of the Scalazza of Aci Reale, we find large blocks of compact augitie lava more or less rolled and rounded, which have generally the surface corroded by the action of chloride of sodium and other salts of the sea-water. We likewise find in this place, among the blocks, the calcareo-siliceous deposit, which extends upon them from 2 to 4 metres in height ; and the immense current, which forms the wonder- ful Grotto delle Colombe, shows a zone of erosion several metres in height. The shore of 8S. Tecla is almost entirely formed of recent alluvium, the materials of which are pebbles of felspathic and augitic lava of various sizes. ‘Then come volcanic (augitic) currents from Etna, more or less recent ; and lastly, from Prajola to the Onobola a great allu- vial deposit extends along the shore. Now from these observations we may discern— ist. That from the shores of the Simeto to the Onobola we find from place to place undeniable characters of the ancient levels of the sea in the recent epoch. 2nd. That the great blocks with blunted angles, rolled, and cor- roded on the surface, the calcareo-siliceous shelly deposit, and the marine breccia, which are seen at different heights above the level of the sea, are the effect of the continued and daily action of the waves of the sea. 3rd. That the existence and disposition of the holes of the Modiola lithophaga, Lamk., in the calcareo-siliceous shelly deposit, and the normal position of the shells, both gasteropod and lamellibranchiate, make one suppose a slow and gradual elevation of the coast. 4th. Lastly, that the Lcthophage and the calcareo-siliceous deposit being found on several islands and on the Faraglione of the Birds up to the height of almost 13 metres, and on the shore of the Pietra degli Uccelli there being large blocks of lava, blunted, rolled, and invested with Serpule to the height of 14 metres, we may establish the mean height to be 13 metres and 5 decimetres,—the greatest height of the now undeniable gradual elevation of the coast of Sicily from the Simeto to the Onobola during the present period. 1858. ] JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 509 2. On Fossin SHELLS and StriaTeD Boutpers at H1eH LEVELS an ScoTLAND. By Tuomas F. Jamieson, Esq. In Letters addressed to Sir R. I. Murcuison, V.P.G.S., &e. [As the notices read before the Meeting from these letters are fully detailed by Mr. Jamieson in a Paper received shortly afterwards, the latter is here printed in full.] On the PLetstoceNE Deposits of ABERDEENSHIRE. By T. F. JAMIESON, Esq. Communicated by James Smiry, Esq., F.G.S. In the lower districts of Aberdeenshire, all along the coast, we find the rocks almost entirely hidden by a clothing of superficial matter, varying in quality from fine clay to stony earth, loose shingly gravel, and sand. in some places this covering is of great depth, exceed- ing even 100 feet in thickness, and is most developed in wide basin- shaped tracts, where the rock sits low. Much of it seems to have been gradually accumulated under the waters of a former sea, and, when now exposed to the light of day, presents a series of stratified layers of silt, sand, and clay, occasionally disposed in lamine as thin as paper. A careful search now and then discloses traces of marine shells scantily dispersed, either in the shape of broken fragments er, more rarely, in a perfect condition—bivalves entire and shut, with the delicate skin or epidermis in complete preservation, apparently in the spot where the animals had lived and died. In other places, however, we find large boulders, and blocks sometimes of gigantic size, together with deposits the character of which cannot be accounted for by the causes at present operating on our coast. Commencing at the southern boundary of the shire, I shall proceed north, sketching the features of the coast as I go along. At the mouth of the River Dee the denuded remains of these beds are found on both sides of the stream; and at the Torry brickwork on the southern side, the succession of strata is as follows :— 1. Shingle, or coarse water-worn gravel, irregularly Rete tltne ee lepine ens tk SE SLE MS Geet. 2. Finely-laminated clay, varying in colour from yellowish-brown to red and bluish-grey. Con- tains some thin seams of fine sand........ 22 feet. 3. Gravel; depth unascertained. No organic remains appear to have been got in this excavation, the base of which is probably rather below the present sea-level. At the bottom of the uppermost gravel-bed, and resting between it and the subjacent clay, I saw an angular boulder of quartzose gneiss, be- tween two and three feet in length. None were seen by me in the clay itself; but the manager of the work told me that they are occasionally found in all the beds. I suspect they must be of small size, for I saw no large blocks lying about the place. At another brickwork, on the opposite side of the river, the series of beds, commencing also at the surface, is— Po ie 510 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, Feet. 1, Water-worn gravel and sand, StRRtiGeds ts 22h caces see ne 2. Alternating seams of fine sand and brownish clay, the layers very numerous and somewhat undulating 20 The clay gets redder to- wards the lower part, and passes down into 3. A mass of fine brick-red clay 17 4. Fine light-greyish clay, with thin seams of sand .... 10 5. Sand and gravel irregularly disposed. . 10 6. Strata of fine pale- -oreyish clay, laminated and con- taining seams of small sand . be 20 7. Fine sand ; “depth u unascer- tained. In the mass of red clay the skeleton of a bird was obtained about twelve years ago. It is now in the museum of the Marischal College, Aberdeen, where it is ticketed as the bones of a duck. I have not seen any shells or other organic remains from this excava- tion; but the workmen told me that, a few years ago, they had found in the lowermost clay-strata the remains or impression of what they thought were fossils, but nothing that would bear removal. No boulders or large stones were seen by me in any part of this excavation ; the clay-strata are, in- deed, remarkably devoid of stones and pebbles of every kind. The bottom of the cutting is a little below the present high-water mark. The greater part of the city of Aberdeen appears to stand on this gravel-covered clay; and some borings for Artesian wells, at- tempted in different parts of the town, reveal its connection with the sub jacent rock. ‘ay UeIN “p “JSIYOS-VOTU PUB SsIOUN) *a ‘puvs pue Ayo peytyenys °¢ “Ae[O-op[nog pue Jarvryg ‘v a EY Ns TNS WES WN MFR QQ S SSS — ~— =~ SATS ~~ iiwra > Pp ~ sa af =2r7_ I= ~ p= «2 q---& Black Dog. -Milden. Menie. Ythan. Collieston. Cruden Bay. Buchan Ness. Invernettie. Ugie. Annochie, “So tU CE moge ySusy ‘auysuaapsagy fo psv0g ay7 Huojw uordzg9— | “Sig 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. od I have obtained the following account of the most interesting of these bores. One sunk at the Woolman Hill pierced through— Feet. ie eret le nM Cyr cee es ae oo eee 6 Zeasey, erbinish Clay os eee ee Se ANG AME SWINGS eae a to te 20 ZO LIES OES VCE GE ie er 6 5. Rough sand and shingle ............ 3 6. Old Red Sandstone conglomerate .... 115 7. Alternating strata of compact red sand- BROCE cst nite eS a ole, @ ann aie , OA Sy WAN GRAS She Se eee! Another, executed by Messrs. Richards and Co., disclosed the following beds :— Feet ip eVioss aad black*earth {22.2.0 ..¢9..-.. 18 22 Gravel ang siiall stones’ .2'.;........ 094 Bo LV BULDNS Te Oe aati ee A al ae iieese samdeand Clay! 2... sy... 6 a lwek, mosily eramines 2 2). 2.2. 2... (132 To the north of Aberdeen the coast is low, with a sandy beach all the way to the River Ythan. Between the mouths of the Dee and Don the surface is generally occupied by coarse water-rolled gravel and shingle, which frequently assumes the form of large irregular mounds and _ hillocks, such as the Broad Hill, the Powder-magazine Hiil, and others. This gravel, so far as my observation goes, is found to rest upon fine strata of clay and sand, occasionally exposed in cuttings at the outskirts of the town. For instance, at the Seaton Brickwork, near the River Don, the following section is got :— Feet. etn ep nar fey toe 9 ei iaky, Sais, akadt bate ae 3 Fine clay of a yellowish-brown or bluish-brown hue ; contains some thin seams of sand...... 16 Sand and gravel; depth unascertained. The bottom of this section is also about the sea-level. No shells appear to have been found here. These brickworks are generally established at a spot where the gravel-covering is thin, in order to avoid the expense of reaching the clay. ’ Keeping still close to the sea, we find another excavation for clay about 22 miles to the north of the River Don, at a place known by the name of the Black Dog. Here the cutting discloses— Feet. Coarse gravel and shingle, water-rolled ........ Fine strata of clay and sand, disposed in undu- lating layers ; contain broken shells ....,... 11 Sand; depth unknown. HL2 PROCEEDINGS OF THE GEOLOGICAL SocIETY. [Feb. 24, The clay varies in colour from brick-red to a dull-greenish tint, and predominates over the sand, which is of fine quality and brownish colour. The shells that occur in some of the seams, although ap- parently all in a broken or comminuted state, yet often retain their glossy surface. Those which I found were in very small fragments ; amongst them, however, I could recognize the Cyprina Islandica, Tellina solidula, Saxicava rugosa, Cardium echinatum, and a species of Astarte; and doubtless others occur. No boulders were seen in these beds of sand and clay. The meeting of the upper bed of gravel with the clay forms a distinct horizontal line, the two masses not mingling where they jo. The section here is also not much above the sea-level, although somewhat higher than the last. - Large irregular mounds and straggling narrow ridges of coarse gravel abound in this locality, known by the name of the Hills of Fife. I have not met with any shells in this gravel, the base of which seems to rest on the stratified beds. A little further on, and we come to the Burn of Millden, along the banks of which we again find the stratified clay and sand crop- ping out. A section, the base of which is probably not more than three feet above high-water mark, shows some 16 feet of alternating layers of pure red clay and fine greyish sand, quite devoid of all stones. These strata are arranged horizontally, and terminate some- what abruptly towards the sea. Their surface indicates considerable denudation ; and on the top of one of the banks, lodged amongst the bent-covered sand which drifts off the adjoining beach, 1 found two or three boulders of gneiss, granite, and syenitic greenstone,— the largest not exceeding 33 feet in diameter. Some boulders of granite and trap occur also in the bed of the stream. These may have been left by the agency which denuded the clay. A short distance further up the stream, and at a height of pro- bably not more than nine or ten feet above the sea, there is a very small patch of what appears to be the Old Red Sandstone conglomerate, but quite smothered beneath a heavy mass of the stratified sand and clay. Mounds and ridges of coarse ferruginous shingle and gravel, all water-rolled, come nearly close up to the top. of these banks, as if superimposed abruptly on the stratified beds,—while, a little further north, some small cuttings occasionally show the gravel overlying fine red clay. The great mass of shingle, however, retreats inland a. short dis- tance here, returning towards the heweh at Menie, from whence it may be traced, with hardly any interraption, to the mouth of the Ythan. In the neighbourhood of Hopeshill the fields abound with large boulders, mostly of syenitic greenstone and other varieties of trap, similar in quality to rock in situ a few miles to the west. Near the Menie Coast-guard Station I found these large boulders of trap, granite, and gneiss resting on the top and surface of the gravel- ridges (fig. 2), some of them measuring six feet in length, and more or less rounded in form: I traced. them also amongst the low 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 513 hillocks of blown sand overgrown with bents, which margin the beach, occurring sometimes singly, sometimes in clusters, and of various sizes up to 1] or 12 feetin length. Their surfaces are either rounded or rugged, scarcely ever angular, while in mineral character they are generally of greenstone and syenite. Fig. 2.—Diagram showing the position of the Boulders at the top and on the surface of the Gravel-mounds at Menie Coast-guard Station. = SSS SS J SL ae eee In a field on the farm of Drums a gigantic boulder of granite occurs, known as “the Grey Stane.”’ I found it to measure 54 feet in circumference, with a height of about 7 feet ‘above the ground. It has no sharp angles, and most of its exterior is rounded. Another immense block, also apparently a transported mass, is seen lodged in the surface of a field near Menie. I found it to be 78 feet in circumference, and projecting 6 feet out of the ground. It is a coarse-grained greenstone. Drums seems to take its name from these tumuli and hillocks of gravel,—Druim in the Celtic language meaning a ridge or little hill, and being of frequent application in the names of places. I found these ridges to consist of highly-rolled fragments of rock of all sizes, from coarse gravel up to boulders 2 feet in diameter. Those of gneiss are perhaps most numerous, often of a hard, tough, crystalline nature, yet much worn and rounded, showing the great attrition which they have undergone. Granite, both grey and red, is also plentiful, and lumps of serpentine occasionally occur, with other varieties of trap; but, besides these, there are a good many _ rounded fragments of red sandstone in several places, both at Drums and near Menie. On the top of one of these gravel-ridges, a little to the north of Drums, I found a boulder of coarse crystalline rock, of a greenish tint, measuring 8 feet in length by 5 im breadth. No sharp angles occur on its surface. A layer of red clay, about 9 inches thick, overlies the gravel at this spot; and I found traces of a similar clay covering the gravel at Drums. This boulder rested immediately upon the gravel; but the clay encircled its base. An- other large boulder of greenstone lay beside it; and many other blocks were observed in the adjoining fields. Here, then, are clear instances of large transported boulders sitting on the top of these abrupt ridges of water-worn shingle. It seemed 514 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, rather remarkable to me that I had never met with any of these larger blocks imbedded in the gravel itself; nothing larger than 2 or 21 feet in diameter has occurred to me. I have, however, been informed by workmen that they do occasionally find boulders even of very large size in the interior of these gravel-mounds. Reaching the estuary of the Ythan, we find the coast much encumbered by great heaps of drifted sand; and tradition relates that a small parish, called Forvie, was here suddenly overwhelmed by the sandy drift. Coarse gravel and stony earth generally cover the surface, on piercing through which, however, the stratified beds are often exposed at the lower levels. For instance, on the north side of the estuary, at Westfield of Auchmacoy, the following section has been laid open :— Feet. ° 1. Gravel and coarse water-worn shingle ...... oo paanae 2. Strata of fine clay, varying from red to pale grey, with occasional seams of fine sand............ 3. A layer of-eravel 2. 0..2 92 2 ss 4, Pure red clay .. ee 5. Gravel; depth unascertained. The bottom of this section is rather below high-water mark. Fragments of shells occur occasionally in the sandy seams, chiefly in No. 3.* Up beside the dwelling-house, at a level of probably 50 feet higher, m sinking a well, the layers passed through were— Feet. 1. Shingle and coarse gravel SNRs Pe at 3 2. Coarse red clay, containing small fragments of stone 9 3. Fine brownish sand, quite devoid of all stones or TA is osu x' jo,» epeve nile = phe lnyn ts) wipes or 26 The bottom of this sand was not reached ; and no water was got. Finely-laminated clay, I find, occurs up the valley of the Ythan for some miles, but is seldom exposed to view. In sinking a well in the village of Ellon, 44 miles inland, the beds exposed were— Feet Coarse water-worin raved. i.) 5.054.550. 0°s cn usps as Ye 11 Fine laminated clay, varying in colour from brick-red to.pale-sreenish grey). 6. 2% wei. 24 cee < Ce 33 This clay was not passed through, so that its depth was not ascer- tained ; and the bottom of the bore here would also be about as low as the sea-level. Along the south bank of the Ythan, below Ellon, the same fine stratified clay occurs, covered by masses of water-worn gravel, and sometimes by a stratum of stony earth, full of boulders of all sizes, * Since the above was written, I have obtained the fragments of what seems to be the skull of a Common Seal (Phoca Vitulina, Linn.), from the layer of red clay No. 4.—October, 1858. T.F. J. 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 515 up to a weight of about a ton and a half, and of a mineral character similar to rocks which occur further up the valley. - Fig. 3.—Section at Collieston Coast-guard Station. a. Clay. —*B.. Sandy strata. c. Gneiss. About a couple of miles to the north of the River Ythan the sandy beach gives way to a rocky coast of gneiss and mica-schist, which continues without interruption to the Bay of Cruden, a dis- tance of more than five miles. These cliffs very commonly present a face from 60 to 100 feet high towards the sea: where the rock itself attains this elevation it is generally destitute of superficial covering, or has sometimes a thin layer of coarse clay; where, - however, the rock sits low, the additional height is made up of grassy banks, which appear to be composed of red clay and sand, stratified, frequently in an undulating manner. Owing to the grassy surface, the interior of these banks is seldom disclosed by any good section. At the Collieston Coast-guard Station (fig. 3), however, a slip has laid the mass open from top to bottom, showing— Feet. 1. Red clay, devoid of stones, but without any strati- HeAMON-IMES: ADPATEMG a. 9.0. < ieee te oe Soelde LZ 2. Strata of the finest sand, varying in colour from pale brownish-grey to reddish................ 56 3. Gneiss-rock, covered by a foot or so of its own CLC IS et Gyro kh sie pads nei AL arora re The sandy strata lie horizontally with some gentle undulations: they are quite devoid of all stones, pebbles, or coarse gravel. In some small seams of coarser sand, near the bottom of the mass, I found traces of broken shells, but so comminuted as to render any knowledge of the species unattainable. The junction of the clay and sand forms a line nearly horizontal ; and the sea-waves wash the foot of the rock. At a cliff, a mile or so to the north of Collieston, some slips show that the gneiss is covered by 30 or 40 feet thick of strata, composed almost entirely of fine sand varying in hue from red to grey. Some 516 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, seams of pebbly gravel occur in several places, interstratified with the fine sand in undulating layers. These gravelly seams contain fragments of broken shells, amongst which I could distinguish the hinge of the Cyprina Islandica, also bits of smaller Pectens and pieces of a bivalve shell, ornamented with fine radiating strize be- tween the growth-lines. Along with these shells there occur also many small bits of grey and yellow limestone, which appear to have been derived from secondary formations. All along the coast of Slains, the mass of sandy strata seems to rest directly upon the gneiss-rock, without the intervention of any other deposit. Sometimes the top of the bank consists partly of fine red clay, occasionally interstratified with the sand. No large boulders are seen in these strata; but large boulders occur in the fields immediately back from the brink of the cliffs, as if resting on the surface of the deposit. These blocks are of greenstone, gneiss, and granite. Further north, towards the Bay of Cruden, the rocks get higher, and the Pleistocene deposits retire from the cliffs, which are gene- rally bare. The gneiss is thrown into long undulations, and gets more contorted and altered in texture as it approaches the granite, which first shows itself at the southern side of the Bay of Cruden. At the bay itself the rocks disappear, and a low expanse of drifted sand is backed by steep grassy banks, which appear to be composed almost entirely of Pleistocene beds. These banks attain a height of about 120 feet above high-water mark, presenting a steep front to the sea. Their base is perhaps 10 or 12 feet above the sea-level. No good section reveals the structure of these slopes; but near the top of one of them, about 5 feet of coarse red clay is seen rest- ing on fine soft sand, of a reddish-brown tint, indistinctly strati- fied, and quite free from stones. The clay shows no stratification- lines, and contains pebbles of greenstone, granite, quartz, &c., more or less rounded. I picked out one fragment about 5 inches long, smoothed on one side, and covered with many strize in different directions. Towards the northern side of the bay these banks appear to have suffered denudation, and are much lower and more undu- lating. A section, 18 feet deep, shows fine, soft, reddish sand, con- taining several thin seams of red clay. Following up the Burn of Cruden, deep masses of fine sand and clay appear to occupy the ground on both sides; and at Ardiffery we find the stream flowing along the foot of steep banks about 130 feet high, and the ground slopes up behind perhaps 20 feet higher, making a total height of 150 feet. These banks appear to be composed, to their very base, of sand and clay. The stream here cannot be many feet above high- water mark—perhaps 15 feet. No deep extensive section occurs ; but slips in various places reveal the structure of the mass almost from the top to the bottom. The lower part of the bank, to the height of about 20 feet above the stream, is concealed by the low slope of the ground, beyond which several small sections disclose reguiar horizontal strata of very fine sand, mostly of a pale-grey tint, but occasionally reddish. Amongst this sand there occur a few thin 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 517 layers of fine brick-red clay. The appearance of these sandy strata, deep down in this bank, very closely resembles the lower part of the cliff at Collieston ; and in like manner I found them to contam mi- nute fragments of shells. A shell, said to have been obtained in these banks, is in my possession, which I received from Mr. Dawson of Cruden. It appears to be the Mangelia turricola of Forbes and Hanley, and is somewhat water-worn, although almost entire. The only stone of any kind which I found in these sandy layers was a small pebble of flint. The strata here are horizontal, not undulated, but often finely rippled. Higher up, the sandy strata seem to be of a more reddish hue, containing seams of red clay ; and some coarser stuff, with boulders, appears to occur occasionally, as if it had slipped down in some places. The upper part of the bank is not exposed by any good section, but seems still sandy; while higher up still, where the ground slopes back, there is some coarse gravel or stony stuff ex- posed at the side of the adjacent fields. These Pleistocene deposits, although still of great depth in this locality, have no doubt been worn down and washed away to some extent during the course of events which intervened betwixt the period of their deposition and the last movement of elevation. This denuding agency, in cutting down the stratified beds, must have thrown their materials, together with other debris, into positions which are now difficult to be explained. It will be safest, therefore, to rest any theories upon good, clear, extensive sections, where this disturbing element can work no mistake. To the north of Cruden Bay the coast is composed of red granite all the way to Peterhead, forming cliffs from 70 to 150 feet high, and upwards. ~The top of these rocks is more or less bare, and destitute of any considerable covering of loose matter. In some places a depth of 3 to 4 feet of clay and stony rukbish occurs; and it is worthy of note that the stony debris is not made up of granite, but of the detritus of slaty gneiss, with varieties of porphyry and quartz : sometimes a few bits of red sandstone may be found. Some slight difference may be occasionally remarked in this superficial mass, the upper part being less stony, and of a red colour, more of the nature of red clay, while the lower portion next the granite is little else than a mass of small stony debris, the fragments mostly angular or little worn, although there are also many rounded peb- bles. One large boulder of red granite, perhaps 6 feet in diameter, I noticed amongst this stony stuff, resting on the top of a narrow precipitous ridge jutting out into the sea, immediately south of the Bullers of Buchan. To the north of the Buchan Ness the rocks sink down to a low height, and in some places disappear, and the Pleistocene deposits again show themselves. No good section is seen, however, except at Invernettie, where a brick- and tile-work has long been established. The excavations are made in the face of a bank, which rises up from the sea-beach to a height of nearly 50 feet. I found its structure to be as follows :— ST A ee 518 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, 1.) Blackish loamy earth .4).'.) 22-0, 4. See 1 2. Reddish-brown clay, apparently devoid of stratifi- cation or lamination, and containing stones of various kinds, and of all sizes up to 43 feet in ' diameter; often striated and Ea oo on the sur- face. ; . 30 to 40 3. Clay of a brick-red colour and finer. nature, and apparently free from boulders .......:. 7° 2itome 4. Very fine, laminated, dark-brownish clay, quite free from stones .... . 3s ee ee 5. Fine brownish- _orey ‘sand, “devoid of all stones or pebbles of any kind: the bottom of it has not been reached; but it has been penetrated to a depth’ of 22.09 OS Oe, rrr The foreman of the work told me that this finely-stratified clay and sand had occurred regularly at the base of the bank all along, covered deeply by the coarser clay with boulders. The fine sand at the base of the bank must extend beneath the sea-level. The stones which I found in the deep mass of boulder-clay were of granite—both red and grey, crystalline schist of different varieties, greenstone and other kinds of trap, sandstone, and flints. The largest block was of a fine- grained, tough, greenish rock, 4} feet long by 23 feet broad and 1} thick. It was rough and angular on all sides hae one, which was smooth and worn, as if it had been rubbed strongly over some hard surface. There were several sets of scratches, grooves, and furrows, mostly short, and tending in one general direction, viz. parallel to the longest diameter of the block. The granite-blocks were generally more rounded, and occasionally grooved, but much less distinctly ; those of greenstone are also oc- casionally smoothed and scratched. The largest piece of sandstone was greyish, moderately fine-grained, measuring in feet 3 x 2x 1, an- gular and rough on the surface. Many of the boulders are striated on all their sides. The stones in this upper bed of clay do not bear a very large proportion to the whole mass; so that the clay is used for making bricks and tiles after the stones are extracted. In this boulder-clay I found also traces of broken shells, occurring in films of coarse reddish sand in various parts of the deposit. I also picked a broken fragment of shell out of the finely-laminated clay No. 4. Several years ago, the skeleton of a bird was found in this bank, at a depth, it is said, of 25 feet from the surface, and about 15 or 20 feet above the level of the sea. I have not hitherto discovered what became of this skeleton. When in search of it, in the Ar- buthnot Museum, Peterhead, I found an organic remain with the following label :—“ Fossil vertebra found in excavating clay at the Brickwork, Peterhead, August 1825, 38 feet below the surface, placed on what has been the sea-beach.’’ The words in italics were somewhat indistinct, the ink being much faded. This fossil 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 219 I found to be 6} inches in diameter and 44 inches thick, and of a general roundish aspect. What animal it had belonged to, I cannot say—probably some large fish. There are no spinous processes or bony projections from it. From the depth at which it was found, it would seem to have been about the top of the mass of fine sand. No rock is exposed at the bottom of this section ; but it protrudes in the beach at a short distance on both sides. Here, then, at Invernettie is a very good instance of a clay, con- taining numerous boulders, overlying stratified clay. I found the same thing at a place called Downiehills, nearly three miles to the west of Peterhead, and at a higher elevation. At this spot there is also a brickwork, and the brickmaker informed me that he had sunk a well 40 feet deep, and bored 12 feet further, without reaching the bottom of the clay, and that the section was— Feet. Unstratified stony clay, of a reddish-brown colour, containing some large boulders and stones of many varieties, which are occasionally striated.......... 20 Stratified clay, containing layers of different colours, mimorstonesear | ee oe Poe 32 This uppermost boulder-clay is also fine enough for making bricks and tiles, after extracting the stones. He told me that he had got one block of granite in it about 3 tons in weight, some of the frag- ments of which he showed me, built into some adjoining masonry. It was of the red Peterhead granite, and showed the traces of the boring-iron upon it. No others had occurred nearly so large as this ; but boulders are often found from 2 to 3 feet in diameter, and indeed I saw some of this size in the clay myself. Ina heap of smaller stones which had come out of the same mass of clay, I observed fragments of granite of different varieties, also gneiss, trap, porphyry, and a few of red sandstone and flint, and one bit of lime- stone 4 inches long and striated on the surface, apparently belong- - Ing to secondary strata: it was fine-grained, but of impure quality. Two or three scratched and striated stones were observed by me; but they were far from numerous. This boulder-clay, according to my informant, also contains shells, generally broken, but sometimes whole. They are, for the most part, so decayed that they cannot be preserved ; but some of them appear to have been thick and strong. I have not ascertained the elevation of this spot, but should think it to be somewhere between 150 and 200 feet above the sea-level, or perhaps scarcely so much. At the north side of the town of Peterhead some low granite- rocks, the base of which is washed by the sea, are seen to be co- vered by a mass of coarse gritty earth or mud, of a dirty-grey hue, full of small stones, some of which I found to be striated or scratched on the surface. They are of trap, quartz, and granite. This mass of stuff is about 8 feet deep, and rests immediately upon the solid granite-rock, without the intervention of any other layer whatever. Some indistinct undulations seem to occur in this deposit ; but other- wise it is unstratified. No high banks occur here. 520 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, A little beyond this, the Ugie flows into the sea, draining a low basin of ground. I have found fine laminated clay composing the ground along its banks in many places, for several miles up its course, but frequently concealed by a deep covering of coarse gravel. At Ednie this fine stratified clay rests upon a mass of coarse stony stuff, which, however, is not clearly exposed. In sinking a well there was found, I am told— Feet Fine steatiiidd ‘clay tiie. cit ove. 2 eee 13 Coarse stony clay, dark-coloured, and apparently de- void. of ‘stratification »...9.000.'.4 20 2. I found some traces of broken shells in the stratified clay here also. TI am not aware that any large boulders occur in the lower mass. In the part of it which I saw, the stones were not of large size. This section, although little more than two miles distant from the sea in a straight line, is yet much more following the course of the Ugie. It is at no great height above the sea. The coast to the north of the Ugie for many miles presents a broad sandy beach, backed by undulating banks of various height, but seldom, if ever, exceeding 100 feet. The drifting sand which blows off the coast hides everything, so that the interior of these masses is rarely to be seen. In some places, however, their struc- ture is indicated, and seems to be a fine tenacious clay of a bluish tint. About five miles to the north of Peterhead is the Annochie Brick- work, close upon the sea-beach. Here the excavations are made into the heart of these sand-covered banks, and disclose a fine, blackish- blue, sandy clay, quite unmixed with stones or pebbles of any kind. This clay has been penetrated to a depth of 25 feet, and found to pass into fine sand of a similar hue; but it is not known what lies beneath. Deeply imbedded, then, in this fine bluish clay-mud, I found per- fect shells occurring, in some places rather abundantly. The species were— Nucula tenuis. Leda pygmea. Lucina ferruginosa. The last-mentioned is a very minute shell, and seems to be much less numerous than the two others. All the three are very delicate thin- shelled bivalves ; but their preservation is so perfect that the greenish- yellow epidermis, or skin-like pellicle that covers them, is quite uninjured. They are, however, so friable, that the slightest touch converts them into powder; and on exposure to the air for some time, the epidermis loses its lustre, and sometimes shrivels up. Sometimes both the valves are in conjunction and shut; but more frequently, I think, they occur as single valves. It is also worthy of notice, that no broken or comminuted shell-fragments were ob- served occurring in this clay *. * At a subsequent visit to Annochie, in company with Mr. Winter, the ma- nager of the work, who most kindly gave me all the assistance in his power, I succeeded in finding nearly a dozen other fossils.) Amongst these were several 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 521 Here, then, we seem to have the remains of the animals imbedded in their native mud. The assemblage and the deposit itself both indicate deep water; and these same species have been found con- gregating at a depth of from 30 to 100 fathoms on the western coast of Scotland, where they have all been dredged alive by Mr. MacAn- drew. They are species, however, which are characteristic of a more northern region at the present day: in fact, until within these few years, the Leda pygmea was not known to occur so far south as Britain, being principally developed in the Arctic seas; and even aN it is known in only one locality, namely the neighbourhood of kye. This clay-bed appears to have suffered much denudation, and has an irregular undulating surface. No considerable section is exposed ; and, as far as I could see, it appeared to be of a very uniform tex- ture, without any distinct stratification-lines. The position of the shells is little above the present high-water mark ; and the clay-bed appears to pass in below the beach. We have here a great change indicated, from this old muddy sea- bottom to the present sand-encumbered coast, which abounds at this place in broken shells. In the course of a short search along the beach, I picked up specimens of the following species, mostly in broken fragments :— Purpura lapillus. Tapes pullastra. Littorina littoralis. Donax anatinus, Patella vulgata. Pecten pusio. pellucida. opercularis. Cyprina Islandica. Nassa incrassata. Cypreea Europea. Buccinum undatum. Trochus cinerarius. Mytilus edulis. zizyphinus. Solen ensis. ? Astarte sulcata. Venus striatula. Mactra solida. In some of the banks in the neighbourhood I found fine blue clay, of a similar appearance to that in the brickwork, but containing numerous minute regular crystals of sulphate of lime. I have now sketched the greater part of the eastern coast of Aberdeenshire, and have shown that a deposit of stratified sand and clay, often of great thickness, appears to occur with considerable specimens of Foraminifera. Of Mollusca there were two or three species of Cylichna (one of which seems to be C. cylindrica, the others resembling C. 06- tusa or C. mammillata),—a single valve of Kellia, apparently K. suborbicularis,— decayed specimens of Panopea Norvegica and Mya truncata, variety pullus of Wood’s ‘ Mollusca of the Crag.’ These shells, however, were so decayed and friable as to render their determination difficult and doubtful. They did not occur in broken fragments, but were perfect in form, although the shelly sub- stance was gone. I was told also that the skeleton of a fish had been found > some years ago, but had not been preserved. Messrs. W. K. Parker and Rupert Jones have kindly examined microscopically some of the Annochie deposit, and they inform me that in about two thimblefuls of the dark-slate-coloured, fine, sandy clay, with roundish quartz-grains and some brownish mica, they have found several fine specimens of the Polystomella crispa, var. striatopunctata, two large specimens of Cornuspira foliacea, and a few little fragments (plates) of Eehinus. —October, 1858. T.F. J. 522 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, regularity wherever the rock sits low, and that these fine strata are covered in some places by extensive masses of coarse gravel and shingle, and in others by a clay or earth full of boulders of many kinds, often of large size, and sometimes striated and grooved in a singular manner. It has also been shown that great boulders occur on the surface of the gravel-ridges, and, according to the accounts of workmen, occasionally imbedded in their interior, although I have not observed this latter fact myself *. These stratified masses have been found resting on Old Red Sand- stone conglomerate at Millden, and on gneiss and mica-slate along the sea-margin of Slains; and no clear instance along the coast has occurred to me of any mass of coarse stuff, containing large boulders, lying beneath them; nor have any large blocks been seen by me imbedded in the fine strata themselves. These are evidently the remains of an old sea-bottom of the later Tertiary period,—the laminated clay and sand having accumulated in the deeper troughs of the ancient coast, where they were beyond reach of the surface- agitation produced by the winds. In the parishes of Slains and Cruden there are many knolls and ridges of water-worn shingle and gravel, which I have found im various places to contain broken marine shells. Perhaps the most remarkable of these are the gravel-ridges beside the Loch of Slains, locally known by the name of the Kippet Hills. They vary in form and size, but generally rise to the height of about 30-or 40 feet above their base. The sides are commonly steep, and their summit or ridge often so narrow that two carts could scarcely pass each other on them, while their breadth is such that a person standing on one side can easily pitch a pebble quite over them. In these features they would seem to resemble the Eskars of Ireland, the Kaims of the south of Scot- land, and the Osar of Sweden, concerning the origin of all which there has been some discussion. Our Kippet Hills can be traced, with hardly any interruption, for a distance of beyond two miles, in a tortuous, curving, or zigzag lme without any definite direction. They are connected also with other gravel-deposits in the district; and their extent and relations are obscured to some degree by a deposit of red clay which covers them in many places. Fig. 4.—Diagram showing the Red Clay covering, and filling up the hollows of the Gravel-ridges at the Kippet Hills. a, Clay. b. Gravel. * Tam inclined to think that the gravel on the top of which these erratic blocks lie is of older date than the gravel covering the stratified beds at Aberdeen aie elsewhere. It may belong to the same period as the gravel of the Kippet ills. 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 52e As to the composition of these ridges, I have found them to con- sist of sand, gravel, and water-worn pebbles. In some places the mass is very coarse, showing no regular arrangement, but abounding in rolled stones of all sizes up to a diameter of 21 feet; few, how- ever, exceed 1 foot in length. In other places the materials are much finer, passing from coarse pebbly gravel into undulating sandy layers. Broken shells occur in both sorts. The pebbles are of many different kinds; the most abundant seems to be micaceous schist, similar in character to what occurs along the adjoining coast, while gneiss, quartzose schist, granite, and greenstone are also plen- tiful. A bit of felspar and a flint or two may be occasionally found ; and upon one occasion I picked up two small pieces of serpentine. But, besides all these, there are in many places a great abundance of red and grey sandstone, together with a multitude of limestone frag- ments, which vary in character and hue. They are always more or less water-worn ; some are of a yellowish tint, and of a soft, tough nature, effervescing strongly with acids, while others are finely lami- nated, varying in colour from greyish-white to dull grey and yellow: these are generally of a fine earthy texture, and effervesce more feebly on being treated with nitric acid. The limestone fragments occasionally, though rarely, contain fossils. I have found a bit or two containing traces of small shells, and have seen one fragment of laminated grey limestone with the impression of a small fish: both the head and tail were wanting, owing to the wearing of the fragment ; but when complete, it might have been about 6 inches long. Ac- cording to the reverend author of the statistical account of the parish, these limestones were formerly sought out by the farmers, and burned for lime, being found “generally from 1 to 16 lbs. in weight.” I may mention that I have found similar bits of limestone in various parts of Cruden and Slains, and also more rarely in Logie- Buchan and Foveran; they are, however, more plentiful in these Kippet Hills than anywhere else. I have never found them either scratched or striated in these gravel-ridges, but have occasionally found them so in other places, where they occurred in clay or stony earth. No rock of the same nature is known to me in this part of Aberdeenshire ; but, from the abundance of the fragments, con- fined as they are to a limited tract near the coast, I am inclined to think that the source from whence they came must be within the district, and that patches of similar strata probably occur deeply buried beneath the Pleistocene deposits. which drape the whole country hereabouts. é‘ ; - With regard to the broken shells which are mixed up with this gravel, they are generally in very small pieces, and much worn, I can distinguish at least eight different kinds, and probably more. The hinge of the Cyprina Islandica is of frequent occurrence, its massy thickness having stood the wear and tear better than most others. I have found also some almost complete valves of a Tel/ina, which seems to differ from the T. solidu/a only in being thicker and stouter. It is a strong opaque shell, very tumid in the valves. Is this the Tel- lina Grenlandica® Another is a shell of larger size, also a bivalve, VOL. XIV.—PART I. 2M 524 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, and strong and thick, but very compressed in form. A fourth (of which, however, I have got nothing but small fragments) is a bivalve with strong concentric growth-lines, having the interstices ornamented with peculiar radiating striz. It is also crenated along the ventral margin similar to the Venus Casina. Some of the bits have evidently belonged to a good-sized shell, and are thickened along the edge, while others are the remans of individuals of smaller size, or perhaps of a different species. I have found it in many different places. Fragments of Astarte and Pecten are also not uncommon. I have stated (p. 516) that, in a cliff on the coast of Slains, and immediately opposite these gravel-ridges, I found in the sandy strata seams of gravel containing similar fragments of shells along with pieces of the same kind of limestone. - It would therefore appear that these mounds are formed out of the same materials, and may, perhaps, be a development of those gravelly layers which are inter- stratified with the fine sand. They may be old submarine banks of gravel, which have subsequently been moulded into the form of ridges by denudation. Their base is at about the same elevation as the top of the coast- cliffs, or perhaps a little lower, and they can be traced almost close to the cliffs, while it is also found that a stratum of red clay over- lies both them and the stratified sand at Collieston ; and further, in some places the gravel of these ridges appears to pass into fine sandy layers, similar to the masses along the coast. The district in which these shelly gravels occur lies between the estuary of the Ythan and the Burn of Cruden, comprising an area of about 15 square-miles. This tract of ground culminates, with gentle slopes, in an eminence called Highlaw, whose height I found to be 299 feet above the mean level of the sea. The summit con- sists of a mound of gravel, while banks and knolls of coarse water- worn shingle form the most of the adjoining ground. In some places these masses of gravel show many undulating layers and seams of sand, while in others the disposition of the materials is more irre- gular. No broken shells nor fragments of sandstone or limestone occurred to me here. The materials were of gneiss, granite, quartz- ose rock, felspar, porphyry, and other kinds of trap, sometimes not much rounded. It appears then that, while fine sand and mud were accumulating in the deeper recesses of the ancient sea, here, on the shoals and higher portions, under some 40 fathoms less water, the soundings would have shown coarse gravel, sand, and shingle. I remarked, however, that a deposit of red clay in many places overlies this gravel, filling up the irregularities and hollows of its surface. It is never of great thickness, and is generally absent on the higher mounds, or forms but a very thin layer over them. a A similar clay was found in many places overlying the gravel of the Kippet Hills (p. 522) ; and a thick mass of it covers the stratified sand in the cliff at Collieston.. Do not all these instances point to a de- pression of the sea-bottom, converting its shoals into sunken banks, and its deeper hollows into yet profounder depths ? I did not observe any large boulders beside Highlaw itself, but 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 525 some distance to the north, between it and the Episcopal chapel of Cruden, I found several occurring on the surface of the land, espe- cially beside some small croft-houses. The largest were from 5 to 6 feet in diameter, but many were from 2 to 3 feet; and they con- sisted of red granite, gneiss, and trap. One of these blocks I ob- served to be much smoothed or ground down, and covered with strize and scratches on part of its surface ; and this occurred in a fragment of hard crystalline quality. On drawing the attention of one of the crofters to this circumstance, he said that he had noticed the fact, and that these markings were confined to the lower surface or bed of the stone. It had been a large block, some 6 feet in diameter, and had been blown to pieces by gunpowder when I saw it. Much of the ground here (which is at an elevation of probably 200 feet or upwards) seems to consist at the surface of coarse stony earth, varying in colour from reddish to a dirty bluish-grey, and contains mary small stones of gneiss, granite, trap, micaceous schist, compact felspar, and quartzose rock. I picked up also two or three small bits of limestone of different colours, and similar in quality to those which occur in the gravel of the Kippet Hills. One of these limestone-bits was covered with striz and scratches on both sides. I noticed also some nodules of flint, and a rounded pebble of red sandstone. Several striated fragments were observed by me in this coarse earth, the stones of which are seldom sharply angular. In the Rev. Mr. Pratt’s entertaining volume upon the district of Buchan, I find it stated that the outer walls of the parish-kirk of Cruden, erected in 1777, are said to have been all built “from the greystone of Ardendraught, a huge boulder of granite on the Old- toun Farm, upon which, from time immemorial, Hallow fires had had been lighted.” I have pointed out that the stratified sand and clay can be traced for some distance up the rivers which fall into the sea along the eastern coast. The same is the case along the Moray Firth. The Kinedart Water, a tributary of the Deveron, flows through a Pleistocene deposit of considerable thickness ; and deep down in the high banks along which it runs, I found specimens of the following shells imbedded in a fine, dark, sandy mud :— Tellina proxima. Leda pernula. Nucula tenuis. ? Tellina solidula. ? Dentalium. The most plentiful was 7. proxima, always complete, with the two valves in connexion and shut, the dark-brownish epidermis remain- ing. What is, however, remarkable, the valves were always more or less cracked, especially the upper one, which was often quite squashed into the lower. It looks as if the shell had been crushed with the animal in it, as it is generally filled with a dark powder, and a blackish stain frequently extends to the sand around it. The specimens were often of large size, measuring 14 to 12 inch across. Pressure from above, and suddenly applied, seems necessary to account for the condition of these shells: the crushed fragments were never shifted sideways out of their position. 2M 2 526 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 24, A thick mass of gravel and sand, forming the upper part of the bank, appears to have been thrown down upon this fine sandy mud ; but there is no good section, at the place, to show their connexion. I found this sand and gravel in some places containing a great abun- dance of broken shells. There were many entire single valves of Tellina, solidula, and fragments of Astarte arctica. Pieces of the Cyprina Islandica were also numerous. The Tellina proxima is characterized by MacAndrew as the Tel- lina of Arctic seas, and is not now found alive on the British coasts. He gives its principal development at a depth of from 4 to 10 fathoms, but ranging down to 40. The Leda pernula is also now extinct in our seas, but is found from Drontheim to the North Cape, having a great vertical range of from 35 to 160 fathoms. The Tellina soli- dula is still found from Britain to Finmark, in more shallow water. Here then, again, are the remains of the animals apparently where they had lived and died. The prevalence of Tellina proxima marks shallower water than the assemblage at Annochie does, as might have been expected ; for this Kinedart deposit must be at an elevation perhaps 150 feet higher, situated in a sheltered ravine. Of the other shells I found but one specimen each; and these were single valves although uninjured, with the epidermis in fine preservation. The evidence still points to a chilly climate, and a sea undisturbed enough for mollusca to flourish at least for a certain lapse of time. In the valley of the Deveron itself, as far up as Huntly, I found finely laminated silt and loam exposed on its banks, at the height of 360 feet above the sea-level, and perhaps 50 or 60 feet above the river. No organic remains, however, occurred to me. Passing over to the valley of Spey I there discovered finely laminated silt, capped by sand and gravel, lining the base of the hills to a great height. On the east side of the stream, from Cairnty to Ben Aigan, it may be traced with little interruption, running up the Burn of Mulbain at a corresponding elevation; and I found it also on the west side. Having borrowed a spirit-level from one of the gentlemen engaged with the railway now in process of construction across the Spey, I proceeded to measure the height of these terrace-like banks on Eastertown of Cairnty, and found them to reach an elevation of 247 feet above the river, and 375 feet above the sea, at high-water- mark, ordinary spring-tides of the Moray Firth. Fixing the instrument on the summit, I took a sight across the Spey to the flat-topped fragment of a similar terrace on the west side, and found it to be at the same level. Turning my view up the river to a similar bank opposite Rothes, I ascertained that it was several yards higher, after allowing for curvature. I then swept the view towards the Moray Firth, and found, what was very apparent even to — the naked eye, that I quite overlooked everything between me and — its waters. It thus became evident that here was no freshwater deposit accu- mulated in the depths of some dammed-up lake, but an indubitable portion of the ancient sea-bottom, when salt-water lochs stretched their arms far inland. No remnant of any barrier appeared, that 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 527 could account for a lake at such a height ; no glacier descending from Ben Aigan or any hill on the east side could have barred the valley down here ; for there is no height on the opposite side that the icy avalanche could have rested on. Thinking that the spirit-level I had used might be out of adjust- - ment, and consequently not trustworthy for a long sight, I procured the loan of another good instrument made by Troughton and Simms, which had been adjusted but a few days previously, and with it also I found the Rothes bank to be considerably higher than Cairnty, and also that terrace-like deposits, equal in height to that of Rothes, oc- curred for some distance up the glen on the opposite side of the Spey. Whether, therefore, the elevating power had increased towards the interior, or whether it is that the strata in the lower part of the val- ley have suffered more denudation, may be questioned ; yet the fact remains, that these banks rise in height as we ascend the valley. Those at Rothes are higher than those at Cairnty ; and similar ter- races which I observed above Aberlour, and also opposite Ballin- dalloch, seemed to me higher still ; but want of time compelled me to leave their measurement unascertained. The best section of these masses is at Rothes, where the bank that looks down upon the village, from an altitude of about 190 feet above the stream, presents the following section at its highest part :— Feet. 1. Loose gravel, sand, and shingle, stratified ...... 30 2. Fine stratified sand and sandy mud, of a pale grey tint, containing no stones of any kind......... 45 3. Gravel and fine sand interstratified............. 15 4. Unstratified pebbly clay, some bands indistinctly seen here and there, colour dirty grey, somewhat Reddish, uo laree boulders... . 22. -60-6--s5.+ 1d 5. Fine stratified sand and sandy mud, often rippled and waved, some seams containing a considerable proportion of clay, colour pale-grey, occasionally reddish. It contains no gravel, stones, nor peb- [LSS eT yal SIT ed ee 3D 6. Base of the bank descending to the edge of the river, concealed by loose debris.............- 50 In some parts of the bank the unstratified stony earth attains a considerably greater thickness ; but at the time of my visit there was a very clear section at the point described. The arrangement of the beds was nearly horizontal. The stones and pebbles were of gneiss, granite, quartz, and similar crystalline rocks. No large boulders were seen; and I was disappointed to find no fossil remains in these beds, although a longer search might have been more successful. Standing on the top of these high banks, and looking down upon the fertile lowlands of Moray, dotted with farms and thriving vil- lages, I could not but picture to myself a time when the ocean rolled over its plains, and threw its breakers ashore even at my feet; here, ° 528 PROCEEDINGS OF THE GEOLOGICAL sociEetTy. [Feb. 24, far up on these hillsides, must once have been the old high-water- mark, I shall now mention some other circumstances that tend to throw light upon the depth of the sea during a part at least of the Pleisto- cene epoch. The evidence of the Mollusca, so far as it goes, indicates that, at the period of their existence, the depth of the sea was not beyond a few hundred feet, even over the lowest part of the present land; and it is important to bear in mind that their remains have not been found anywhere in this part of the country at an elevation exceeding 250 feet. What I am now going to allude to, however, is the occurrence of beds of gravel and water-worn pebbles on the summits of some of the hills in this eastern part of Aberdeenshire. I have shown that the top of the ridge about Highlaw, at an elevation close upon 300 feet, is occupied by gravel; there is also a ridge in the neighbourhood of Ellon, called Cross-stone, the top of which consists of great masses of water-worn pebbles and gravel at an elevation of 226 feet. The Hill of Auchleuchries, in the parish of Cruden, has also a crest of gravel, reaching a height of 356 feet. Again, there is a ridge of hills which, commencing at the Buchan Ness, runs inland fer seven or eight miles, rising gradually till it eul- minates, near its western extremity, in the Hill of Smallburn, at an elevation of 464 feet above the mean level of the sea. This ridge is remarkable for an abundance of flints, which are found along its summit from one end to the other. They are always water-worn, and sometimes contain chalk-fossils. Associated with them is a similar abundance of quartzose pebbles, which are also finely rounded and water-rolled. Both the flints and quartz-pebbles extend a little further west, to the hills of Skelmuir and Dudwick ; but towards the western extre- mity of the latter the flints gradually die away, and finally cease. These chalk-flints appear to have been first brought under notice by Dr. Knight of Marischal College, Aberdeen, who read a paper upon them to the meeting of the British Association, at Edinburgh, in 1834, and exhibited a series of specimens ; and they have since then been commented upon by various observers*. Their abundance is in many places surprising ; but they are often hidden by a covering of peat-moss. In some places the flints predominate, in others the quartz ; but they are both highly water-worn, the hard quartzy pebbles being often as smooth as an egg, with a clean washed aspect, like the pebbles on the beach. I found that both kinds occur in a thin stratum of reddish or yellowish-brown earth or earthy clay ; and in some places the pebbles form almost the entire mass, as is very observable in several pits at the side of a road which crosses the ridge between Tarhenry and Smallburn (fig.5). This earthy clay appears to repose immediately upon the subjacent rock. I have seen it covering the granite at the Blackhill, and gneiss at Smallburn, and * See a Memoir by Messrs. Salter and Ferguson on this subject, Quart. Journ. Geol. Soc. vol. xiii. pp. 83, &c.--Epir. 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 529 rock of doubtful character in other spots. It is also not without in- terest to observe that a stratum of coarse reddish clay, containing pebbles of granite, quartz, and flint, covers the greensand-deposit at Moreseat *. Fig. 5.—Outline-section along the hilly ridge from the Buchan Ness to Dudwick. Length about 12 miles. 1 oF seta! 5 6 7 8 { eee he H } ** Level of 450 feet above the sea-level. + —+ Level of the sea. 1. Dudwick, 563 ft. 5. Tarhenry, 451 ft. 2. Skelmuir, 482 ft. 6. Moreseat. 3. Kinknockie. 7. Cruden Hill. 4. Smallburn, 464 ft. 8. Stirling Hill, 282 ft. In addition to the water-worn pebbles, a few larger stones occur, with a rougher exterior and shapeless form. Some of them occa- sionally reach from two to three feet in length; and I believe they are sometimes found still bigger. They are granite of different varieties, and compounds of quartz and felspar varying in quality. Now, upon the top of the adjacent Hill of Dudwick, which reaches a height of 562 feet, I found the quartz-rock covered by its own debris, but the fragments all quite angular and unworn; and on a lower projection of the hill at an elevation of 480 or 500 feet the same thing occurred. But, searching along the eastern flank of the ridge, I found, to the north of acroft called Backhill of Dudwick, the water-worn pebbles of quartz and flint occurring with considerable regularity to a height of about 450 to 470 feet, beyond which they appeared to cease. It seemed, however, as if some agency had dis- turbed them since they were rounded, and had washed them up at certain points to a higher level; and a small flint or two may be picked up even on the very summit of the hill. Whatever may be thought of this, I would at least draw attention to the great extent of water-worn pebbles that clothe the long ridge before mentioned, with great regularity, up to a height which I have measured and ascertained to be 464 feet above the mean level of the sea. They seem to attain their greatest development along a zone from 350 to 450 feet high. They are strikingly displayed over the Hill of Kinknockie, and also at Hillhead of Auquharney, where there is a croft or cottage, whose foundation I ascertained to be 398 feet above the sea-level. The flints are also particularly abundant on the top of Cruden-hill, which is the point where the three parishes of Cruden, Longside and Peterhead meet ; they cover the ground there _with a uniform close stratum; but over a great part of the ridge the peat lies so thick as to hide everything. I shall now describe a great accumulation of highly water-worn shingle covering the top of a ridge in the parish of Fyvie, about twenty miles inland. * See the Memoir above referred to.— Epir. 530 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Feb. 24, The tract is known by the name of the Windyhills, and is situated close beside the hamlet of Woodhead, in the neighbourhood of the River Ythan. ‘The whole crest of the ridge is thickly covered with great sheets of quartz-pebbles, mixed with a fine whitish sand derived from the grinding down of the fragments. ‘These pebbles are of all sizes below that of an egg, for the most part a good deal smaller. It is true that bigger pieces occur; but there are no large boulders. Several holes or excavations show the mass to be very homogeneous and remarkably devoid of any foreign fragments. A few coarse water-worn flints occur, generally of large size—often nearly six inches in diameter, and frequently with a white chalk-like exterior. I did not find any trace of shells or other fossils in those I picked up. They are for the most part of a very coarse quartzy character, and are whitish, blackish-blue, or yellowish in colour, and are generally unlike the flints of the ridge previously described. The peculiar significance of this gravel (which covers a tract about two miles long and a mile broad) lies in the fact that it is not a drift- gravel, but an accumulation of local origin, derived from the quartz- beds of the clay-slate strata on which it rests. The pebbles are not pure quartz, but contain a considerable proportion of felspar, whose decay gives to the mass a particularly white aspect. Thinking it of some importance to determine the precise height of this ridge, I levelled it from a point of known elevation in the imme- diate neighbourhood, and found the summit to be 412 feet above the mean level of the sea. No clay was found overlapping this deposit ; nothing covers it but some peat-moss. I should say that it had formed a shoal or bank covered by very shallow water, the lashing of which had ground down the quartz into the shingle that we now see. Had the water been of any depth, there would have occasionally occurred seams of clay or fine sand interstratified with the pebbles; but such is not the case. No transitory flood can account for these extensive shingle-banks ; a lengthened period of time is demanded for grinding down the hard quartzy fragments into their present smoothly-rounded form. The thick accumulations of finely-laminated silt which line the lower part of the Spey valley and margin the surrounding coast, the evidence of the molluscs found imbedded in their native mud, together with the silent testimony of these gravelly shoals; all converge to prove that the sea-waters had long stood over this part of Scotland some 450 feet higher than the present coast-line. On the emergence of the land from the waters of this Pleistocene sea, I find evidence that the country had attained a greater elevation than it does at present. This is shown by superficial beds of peat passing down below the present sea-margin. In the links, or low sandy flats, adjoining the beach at Aberdeen, I have seen peat beneath the surface of the sea-sand; and at the mouth of a small rivulet, which divides the parishes of Belhelvie and Foveran, I have observed a formation of peat passing directly under the sea-beach. 1858. | JAMIESON—PLEISTOCENE, ABERDEENSHIRE. 531 Again, in the statistical account of Belhelvie, by the minister of the parish, the late Rev. Dr. Forsyth, the following interesting passage occurs :—“‘ There is a great quantity of peat-moss in the parish. Some of it near the coast is considerably under the level of the sea, and is covered to the depth of 10 or 12 feet by sea-sand. It is pro- bable that this moss extends a considerable length out to sea, and that there is a submarine forest in this bay at no great distance. For on Christmas 1799, when there was perhaps the most dreadful tem- pest that any person remembered to have seen on this part of the coast, several cubical blocks of peat-moss were cast by the sea upon the sandy beach, some of them containing upwards of 1700 cubic feet. Pieces of wood, like branches of oak-trees, apparently con- verted to a consistence like moss, passed through these blocks in every direction. Both moss and wood were perforated by a number of auger-worms of a large size; and most of them were alive in their holes. The moss was of a much harder consistence than any found in this part of the country. Such large blocks could not have been carried to the sea by any of the neighbouring rivers ; for they were not swelled at that time, but were all firmly bound up with ice. In general, when anything like a tempest occurs at sea, a considerable quantity of peat-moss of the same kind is cast upon this sandy beach; but no person remembers to have seen it in so large masses as at Christmas 1799.” The late Prof. MacGillivray, in his account of the Mollusca of this part of Scotland (p. 306.), also states, “ Dr. Fleming informs me that he has seen Pholas candida, as well as Pholas erispata, in masses of peat cast on the beach near Donmouth.”’ I have further been told that, in the Bay of Peterhead, peat is occasionally brought up by the anchors of vessels ; and in the Statis- tical Account of Fraserburgh I find it stated that “many of the benty hillocks which skirt the bay stand upon moss or clay ; and in 1760, a tree with roots and branches and a stem 20 feet long was found entire under the sand within high-water mark.” In the Moray Firth a submarine forest is known to exist between Burghead and Nairn. The occurrence of extensive fields of peat, abounding in remains of trees such as the Birch, Fir, Oak, and Hazel, and situated on exposed tracts close to the sea, where trees can hardly be got to grow at the present day, also renders it probable that the coast was further off when these woods flourished. Horns of large extinct species of oxen have been found in the sur- face-beds of peat, but are very rare. A specimen got in Belhelvie is now in Marischal College Museum; another found at a place called Tuchin, in the parish of Cruden, is in Slains Castle*. I have also in my possession the root-fragment of a stag’s horn found in a bed of peat overlying the clay at Annochie in St. Fergus. For this specimen, as also some other interesting fossils, I am indebted to Dr. Gordon, R.N., St. Fergus. Into the subject of the transport of boulders, and other phenomena _ * Both of these specimens I have seen, and find them to be remains of the Bos primigenius.—October, 1858. T. F. J. 532 PROCEEDINGS OF THE GEOLOGICAL SOciIETy. [Feb. 24, of the drift, I do not now enter, merely remarking that blocks from a distance and striated fragments are found at elevations far above what I have mentioned regarding the stratified deposits and water- worn gravels. In this paper I have chiefly sought to point out two distinct periods, ‘or resting-points, in the Pleistocene history of this part of Scotland :—one when, under a climate much colder than what we now enjoy, the land sat some 450 feet lower than at present; and a subsequent period when it stood higher than it does now, and when deer and great wild oxen roamed amongst its woods. Note.—Mr. S. P. Woodward, F.G.S., author of the well-known ‘Manual of the Mollusca,’ has favoured me with his opinion on some of the shells from the Pleistocene beds described in the foregoing paper, and remarks as follows :— ** Most of the shells from the Annochie clay at St. Fergus are examples of Nucula tenuis and Leda pygmea. All the largest shells from the same spot are Sazicava arctica. The Lucina ferru- ginosa appears to be rightly named. One shell is a Cryptodon, apparently, but quite new tous. The Cylichna is like C. obtusa. ** Of the broken shells from the Kippet Hills, beside the Loch of Slains, are— * Cyprina Islandica, Astarte borealis, Fusus carinatus, Tellina solidula, and Cardium Norvegicum. “There are two specimens of the Tellina of unusual thickness ; but they are like no other species. “Those from Cruden inciude— *« Pecten opercularis, Cardium Norvegicum, and Trichotropis bo- realis.”’—October, 1858. 3. Mr. KENNEpy Macwnas, of Inverness, communicated, in a letter to the Secretaries, the fact of flint arrow-heads and whelk-shells having been found at the depth of about 3 ft. 6 in. beneath the sur- face of a moss, covered with wood, in the parish of Abernethy (Inverness and Elgin). 4. Mr. Ricnarp Mason, of Tenby, in.a communication to the Secretaries, offered a résumé of the evidences, traditionary, historical, and physical, of—1st, the probable depression at some pre-historic period of an extensive tract of country, covering the site of the Bristol Channel and Cardigan Bay ; and 2ndly, of the more recent elevation of the land in the neighbourhood of Tenby, South Wales; the elevated district being apparently confined to that lymg on the Carboniferous Limestone. Evidences of a comparatively recent depression of the Cardiff area were also alluded to. a 1858. ] SELWYN—VICTORIA. 533 Marcu 10, 1858. Alfred Williams, Esq., C.E., Newport, was elected a Fellow; A. Escher von der Linth, Zurich, and E. Deslongchamps, Caen, were elected Foreign Members. The following communications were read :— 1. On the Geovoey of the GoLp-FIELDs of Victoria. By ALFRED R. C. Setwyn, Esq., Geologist to the Colony of Victoria. (In a Letter* to Professor A. C. Ramsay, F.R.S. and F.G.S.) I HAVE now a very large collection of genera and species of Silurian fossils, many of them known forms, and many new. M‘Coy is . going to examine, describe, and figure the new ones. I shall, I hope, soon be able to define the boundaries of the Upper and Lower Silurian rocks in this colony. Melbourne stands on “‘ May Hill Sandstone ;”’ and to the eastward I find a very gradually-ascending series, including probably Wenlock, Ludlow, Devonian, and true Carboniferous rocks, with Oolitic coal-bearing beds resting uncon- formably on the Paleozoic strata. To the westward there is a descending series, from Melbourne towards Ballarat, which I much suspect to be Cambrian. Lingula, like those of Tremadoc, are abundant in the rock asso- ciated with the Bendigo gold-quartz mines. In beds which I take to be equivalents of the Llandeilo flags, Trilobites are very abundant —many of them recognizable European species. I enclose a list of genera (p. 537). This list is now, however, much increased, and is being added to daily. Gold-bearing quartz-veins extend throughout the Silurian rocks ; and their richness appears to me to be dependent more on their proximity to some granitic or other plutonic mass than on the age of the rocks in which they occur. As far as I am aware, these gold- quartz veins do not extend into the Oolitic (?) coal-bearing rocks, which are evidently of newer date than any of the granitic masses I have yet examined. At Steiglitz (fig. 1), we have granite (a) intruded among Silurian sandstone, conglomerate, slate, &c. (6), which are cleaved and inter- sected by veins of auriferous quartz (c), and contain Graptolites, Lingule, &c., and perhaps represent both Upper and Lower Silurian strata. The granites here never contain gold or quartz-veins. Similar auriferous quartz-veins traverse the Lower Silurian cleaved sandstones and slates at Bendigo and Ballarat, as shown in figs. 2and 3. These strata also contain Grapftolites, Lingule, and other fossils. One somewhat remarkable point, in connexion with nearly ali the great granitic masses that I have examined, is that, though they mvariably alter the slate-rocks near their junction, and send veins into them, they do not in the slightest degree affect the general strike or dip of the latter, but appear to have themselves partaken * Dated 10th September 1857. 534 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 10, of the movements which have placed the Silurian rocks in their present highly-inclined and contorted positions, and given them their very uniform meridional direction. ‘There is very little true slaty cleavage until we get low in the Llandeilo beds. The gold-bearing drifts that rest on these strata are of, at least, three distinct ages. The oldest drifts (No. 1, figs. 1, 2, 3) are, I believe, for the most part, freshwater Miocene deposits. The only fossils hitherto found in them are, however, vegetable—consisting of large quantities of wood, trunks of trees, seed-vessels, &c., at various depths to 780 feet. The deposits themselves consist of fine clays—black, yellow, white, red, and mottled, siliceous sands and quartz-gravel, with large water- worn pebbles. These are often overlaid by sheets of lava, in the manner shown in the Bendigo and Ballarat sections (figs. 2 and 3, 2). The rock consists of basaltic lava, &c., sometimes porous, sometimes solid and concretionary (‘‘ bluestone’’), with interposed red, white, and yellow sometimes sandy clay (intersected in the lava in fig. 3). Whether this is a volcanic or ordinary sedimentary deposit, is at present uncertain. Near the coast there are distinct and undoubted Miocene beds, full of marine shells, occupying (apparently) the same geological posi- tion relative to the tertiary sheets of basaltic lava that the gold- bearing drifts do, which I consider to be freshwater Miocene deposits. By far the greater portion of these immense sheets of lava were spread out towards and during the close of the Miocene period ; and their irruption has evidently had nothing whatever to do with the formation of the gold. The trap-plains to the westward are very extensive; and there is every probability of gold-deposits existing underneath the trap over the greater portion of them. The limit, therefore, to the period during which these Tertiary gold-deposits of Victoria may be profitably worked may be regarded as indefinitely remote. I wrote to Jukes four years ago about the passage of these Miocene gold-drifts under the lava-plains*. The gold-beds above referred to as being probably of Miocene age extend to elevations of about 2000 feet above the present sea- level ; and their greatest thickness, includmg contemporaneous trap- pean beds, is about 300 feet; at least, there are no places where they have yet been proved to exceed that thickness. Resting on the lava-sheets is a Pliocene drift (No. 3, figs. 1, 2, 3), containing gold and bones of extinct and living marsupial qua- drupeds. It consists of clays, sands, and angular and waterworn gravel, formed during the denudation of the Miocene drifts and trap, and the granites and Silurian strata. It often rests on the Miocene beds without the intervention of basalt ; and thus two gold-bearing “bottoms” occur. I have only seen one instance of this Pliocene drift, or rather marine beds of the same age, being overlaid by vol- canic matter, ——viz. at ‘‘ Tower Hill,’’ near Warnambool, where raised * Mr. H. Rosales also adverts to the gold-drifts that are older than the basalt, in his paper in the Quart. Journ. Geol. Soc. vol. xi. p.397.—Epir. SELWYN—VICTORIA. 1858. ] sO INS NE 1 i 2 v) Fig. 1.—Section of the F ays eee pepe i}'\ S S SIN A Fig. 2.—Section of the Gold-deposits at Bendigo. (Water-shed to the North, into the Murray River.) Elevation 800-1000 feet above the Sea-level. Epsom Flat. « White Hill. White Hill. The Flat. Creek. w. Rich ‘surfacing ’’ at this spot. Fig. 3.—Section of the Gold-deposits at Ballarat. (Water-shed to the South, into. Bass’s Straits.) Elevation 1400-1900 feet above the Sea-level. Path’s Shaft Yarrowee. Ballaarat Township. (240 feet). z The Flat. z. At this point three “‘bottoms,’’ or deposits of gold, would be found in sinking, at the base of the Nos. 1, 3, and 4, respectively. a. Granite. b. Upper and Lower Silurian Rocks. (Sandstone, slate, &c. much cleaved, intersected by veins of auriferous quartz, and containing Graptolites, Lingule, &c. c. Quartz-veins. 4, Third or recent gold-drift. ; 3. Second or post-trappean gold-drift, with bones of extinct and existing Mammalia (Pliocene ?). 2. Basalt, lava, &c. 1. Oldest gold-drift. , 536 PROCEEDINGS OF THE GEOLOGICAL society. [Mar. 10, estuary beds, with shells of living species, are overlaid by thick deposits of volcanic ashes*. Resting indifferently on any of the older deposits is a third or recent gold-drift (No. 4, figs.1, 2, 3), the result of recent and existing atmospheric and fluviatile action. It is formed by the waste of all the older deposits. The mode of occurrence of the gold is as follows :—It is found at the base of 1, 3, and 4, when resting on each other, or on the Silurian gold-bearing rocks (6); never when resting on the trap (2) or the granite (a) if far removed from the Silurian or Miocene rocks (6 and 1). The gold-bearing gravels are the result of the immediate waste of older masses, and have not been transported far. This, however, does not altogether apply to the eastern gold-fields, where gold is found in the granite. As a general rule, the heaviest gold-deposits and the largest nug- gets are found only at the base of the Miocene, Pliocene, and recent drifts (1, 3, and 4) when they rest directly on the Silurian strata. In the Ballarat section (fig. 3), at the lme marked z, three “‘ bottoms” or deposits of gold would be found in sinking through the bases of 4. 3,.and, 1. I have never yet been able to discover evidence of anything re- sembling glacial action; but I have not been in those parts of the colony where, if in existence, it would be most likely to be seen, viz. on the flanks of the Australian Alps. I have discovered a cave in the basalt of Mount Macedon, a few miles north of Melbourne, containing bones of many living species, including the “‘ Devil” of Tasmania, not now living on the mainland; and also the Dingo, or native dog. In the bones sent by my assistant Aplin and myself to Professor M‘Coy, he recognized “‘ two fragments of the superior maxillary bone, with the long transverse molar, the smaller molar, and the second molar, together with two rami of the inferior maxillary bone, beyond all doubt, of the Dingo at present a. Basalt (Miocene ?). 6. Schists and sandstones (Lower Silurian). c. Mouth of Cave. living in this country.”” In the cave were also found fragments of the skulls of what appear to be a ‘‘ new genus of carnivorous ani- * See Mr. R. B. Smyth’s paper on the Extinct Volcanos of Victoria, above, p. 231.—EpirT. 1858. | SELWYN—VICTORIA. 537 mal,” mingled with numerous others, in the same state of preserva- tion, belonging to species of Halmaturus, Dasyurus, Hypsiprymnus, Macropus, and other living forms. The cave itself is in the Miocene trap (fig. 4) ; and the sides and top of the passages are smoothed and polished by the friction of the backs and sides of the animals passing in and out. The elevation of the ravine is, I think, about 1000 feet above the sea-level, and 30 miles inland. The matter in the cave consists entirely of a very dry, powdery, brown earth. There is not a particle of moisture in any part of the cave, and no calcareous incrustations. The bones are not in the least degree mineralized. When we found it, all the passages were so completely filled up that no animal larger than a rat could have entered them. It must, I imagine, have been filled up during the Pliocene, or what I call the “ post-trappean gold-drift period.”” (See sections.) In various places round the coast I have found what I believe to be Eocene tertiary beds. They consist chiefly of blue clays, with septarian bands and nodules and fine sandy loam, full of selenite, and very rich in fossils,—the whole being exceedingly like London Clay, both in mineral character and organic contents. They are certainly the lowest tertiary beds I have yet seen in this country. List of some of the Paleozoic Fossils collected by the Geological Survey of Victoria during the years 1855-56-57 :— Locality. GENERA, &c. Quarries near Princes Bridge, 1 Atrypa, Leptena,Pentamerus, The- UG OUTATES A eatee gn npooscbecouccer ca, Chonetes (5). COMMPEWOOR! woe cexceescccnedesiavese ene Orthis, Crinoidea (2). University Quarries... c....0se0ss-s06 so Crinoid stems. M‘Ivor Gold-field (75 miles north : of Melbourne)...............000.65 \ a ranay hemsamerns,: Oxthis: ( Orthis, Pentamerus, Atrypa, Lin- | gula, Calymene, Murchisonia, Moone Ponds Creek, Flemington, Chemnitzia, Sanguinolites, Ste- 3 miles north of Melbourne.— { nopora, Cucullella, Orthoceras, M7 G CEE es eae eee ces ae ae Loxonema, Theca, Uraster, Fa- vosites, Gasteropoda,Cycloceras, {and Starfish (20). Orthoceras, Atrypa, Chonetes, Lin- Merri Creek, 15 miles north of gula, Orbicula, Cucullella, Or- MET POUENGY siogabuctecch awch -siseoes this, Petraia, Murchisonia, Grap- tolites latus. View Hill Creek, Upper Yarra, 35 | Jentzna, Petraia, Theca, Starfish. miles east of Melbourne......... { Orthis, Atrypa, Leptzena, Stropho- | mena, Rhynchonella, Pentame- Yerring, ditto, ditto ............++. 4 rus, Petraia, Stenopora, Crinoid | stems, Holopella, Esmondia, \ Starfish, Cheirurus (30). 538 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar 10, Locauity. GENERA, &C. Calymene, Belerephon, Psammo- Simmonds Bridge, Upper Yarra, bia, Othoceras, Nucula, Leptzna, 40 miles east of Melbourne ... Atrypa, Strophomena, Pentame- rus, Cycloceras, Conularia. Anderson’s Creek, 25 miles east ( Stenopora, Palzopora, Favosites, of Melbourne. Impure lime Petraia, Orthis, Spirifer, Crinoid BEQUE# Ficeesen status cine ter cet ss stems. : : Stenopora, Calymene, Pentamerus, Deep Creek, ditto, ditto ............ Atrypa. Watson’s Creek, Upper Yarra, 15 miles east of Melbourne......... Orthis, Avicula, Actinocrinus, Stenopora, Cyathocrinus. Pleurodictyum (2 sp. new), Beyri- chia, Petraia, Pleurotomaria, Portlockia, Orthoceras, Favo- Woori Yalloch Creek junction sites, Atrypa, Bellerophon, San- with Yarra, 45 miles east of guinolites, Cheirurus, Pentame- Melboumme 0.202 eve ace vat rus, Conularia, Orthis, Cucul- lella, Lichas, Loxonema, Steno- pora, Palzopora, Actinocrinus, | Spherexochus. iplograpsus rectangularis, D. pris- tis, Didymograpsus, Siphono- treta. { Atrypa, Strophomena, Pentamerus, Holden, 18 miles N. by W. from f D Melbourne: (A525 oe ee Keilor, 10 miles N. W. from Mel- BOUENC ove an sence cease ce cnemeter sees Thence 75 miles N.W., Graptolites in great variety, and Lingule. No other in the beds to the N.W. Thus we have about 60 genera of Silurian fossils, including many new species. } Graptolites, Cheirurus. 2. On the GoLD-FIELD of BALLAARAT, Victoria. By Mr. Jonn Purutrs, C.E., Surveyor in the Government-Service of Victoria. (Communicated by Sir R. I. Murchison, V.P.G.S.) -[Abstract.] Aut the Victorian gold-fields are near granite, and some are on it. The granite at Ballaarat is fine and even-grained ; and the schists lie against it. Between these rocks the junction is abrupt; there is little or no gneiss, and no porphyritic or other veins were ob- served. The schists are greenish, and are occasionally chloritic, micaceous, aluminous, and siliceous, and are traversed by quartz- veins, from less than an inch to one foot in thickness. The schists in the upper portion are more quartzose, and contain oxides of iron ; lower down they are more aluminous and contain pyrites. Their strike is rather uniform, nearly coinciding with the true meridian, while the cleavage and quartz-veins are not regular in strike. The workings at Ballaarat have exhibited a section of 300 feet in thickness, consisting of gravels, sands, clays, and trap-rocks. The oldest drift or gravel (a beach-like conglomerate) is found not in the 1858. | PHILLIPS—BALLAARAT. 539 deep section, but on the surface of the schist-country. It is regarded as of marine origin by the author, and is composed of quartz, and contains gold at its base. Another drift has been deposited in gullies cut through the oldest drift and deep into the schists. This also is auriferous, and is covered by an ancient humus, which, in the deep section, is found to contain stems of trees, and to be covered over by a trap-rock enclosing upright trees. This fossil wood is usually but little altered in its texture and ligneous qualities ; its colour is changed from that of red birch to cocoa or lignum-vite. But some of it has passed into jet ; and both the charred and the uncharred woods have Sketch-plan of a part of the Valley of the Yarrowee, showing the relations of the ancient and the existing gullies. NaS \ — \ \ 4 \ i tt \ \ Z \ \ \ MN han ( i NYA WN rity mrt si i Ss 4 Wt NAN MA \ \ Te “st <"-=>,aT RENE ae Se — FR wv a. Schists. ec. Gravels, mostly diluvial and partially lacustrine. d. Gravels, marine (?). e. Former course of the river aud its branches. f. Present river-course. Diggings. Elevation. Depth. Diggings. ] 1182 190 9 Milkmaid. 2 1200 162 10 Malakoff. 3 1250 130 11 Nightingale. 4 1280 180 12 Golden Point. 5 1300 160 13 Gravel-pits. 6 1325 165 14 Bakery Hill. 7 1347 115 15 Canadian. 8 1430 22 16 Black Hill. (Some other points of elevation 17 Lady Berkeley. are given on the plan.) 18 Eureka. VOL. XIV.—PART I. 2N 540 PROCEEDINGS OF THE GEOLOGICAL sociETy. [March 10, much bright pyrites in them. The flora of this old land-surface resembles that of the present day. This first trap is covered by green and brownish clay and sand, which are succeeded by another trap, having a line of charred vege- table matter at its base, and also having a similar covering of clay and sand. These clay- and sand-deposits are regarded by the author as being of lacustrine origin; the volcanic rocks having dammed up the old river-courses that formed the gully-drifts, and caused the drainage water of the region to be accumulated in lakes. The next deposit is a coarse ochreous quartzose drift, considered by the author to be the effect of some sweeping deluge; and this is also overlaid by a third bed of trap-rock, with the charred remains of a forest intervening. This trap is covered by a mottled clay of pure quality, also regarded as lacustrine. A fourth trap succeeds, covered by a superficial quartzose drift (of diluvial origin, according to the author), and lying on one side of the schistose hills, which are clearly denuded on the other. In the basin of the Yarrowee, which is covered chiefly with this gravel, the author traces the run of the “ gold-leads” or old gullies, which have only an approximative resemblance to the ramifications of the present river (see the Plan). These ancient gullies or leads had a very uniform fall, which, from the smallness of the contents of the gullies, must have been as rapid as 16 in 1000, while the present fall of the Yarrowee is only 8 in 1000. Mr. Phillips urges that all the basin between the oldlchegee may be wrought by the aid of the water-power of the Yarrowee,—a thou- sand horse-power being now allowed to run waste, which, by means of reservoirs could be made available. The author adds that silver-nuggets have been reported on good authority to have been found within thirty miles of Ballaarat. He further observes that, whilst surveying the district, oscillations of the spirit-bubble indicated a rocking of the earth, and that the country in places sounds hollow, like a wooden bridge, horses even noticing it in passing. 3. On the GoLD-pDIGGINGS at Creswick CREEK and BALLAARAT. By Mr. W. Repaway. (Communicated by Sir R. I. Murchison, ViP-G:S.) . [ Abstract. ] Mr. Repaway noticed first the “bluestone” or concretionary basaltic lava at Creswick Creek, which composes also the rough bouldered surface of the country to a great extent. In the plains | formed of this voleanic rock, small lakes or water-holes, from 3 to 12 feet in diameter, are in some places frequent. At Creswick Creek the different diggings perforate varying thick- nesses of the bluestone, from 17 to 20 feet. Under this is 30 feet of solid clay ; then darkish-coloured quartzose gravel, with abundant remains of wood, to a depth of about 80 feet ; and under this the — T= 2 1858. | OWEN—ZYGOMATURUS. 541 “‘outters,”’ “leads,” or ‘* runs”’ of auriferous quartzose gravel—or *‘ wash-dirt ’’—are met with on the surface of the slate or on pipe- clay. The pits vary considerably in the sections they afford. The fragments of wood in the gravel are of all sizes, from tree- trunks 3 or 4 feet in diameter, to branches and twigs; and this drift is throughout impregnated with woody particles, giving it a black appearance, especially towards the bottom. The cones of the “honeysuckle,”’ or Banksia*, have been found not unfrequently in this drift. These are very brittle; but the wood is often well pre- served. Thin horizontal layers of very hard rock are imbedded in the gravel. Some of the “gutters”’ or “leads” were drawn by the author on plans, showing their course beneath this drift across the present gullies and from hill to hill—especially the “‘ Black Lead” and the ** White Lead,” underlying Little Hill,—one of them having a branch from under Clarke’s Hill, and both uniting before passing under Slaughter Yard Hill. At Ballaarat, Mr. Redaway observed, in a pit on Sevastopol Hill, two layers of bluestone (the second bed about 80 feet thick) above the gold-drift or ‘‘ wash-dirt,” together with stiff clays and quartzose gravels. Here the author traced some gold-runs—the ‘ French- man’s Lead,”’ ‘‘White Horse Lead,” and “ Terrible Lead ’?—running parallel to each other in a direction transverse to that of the present gully, and from hill to hill. Like all other “leads,” these rise generally in the neighbourhood of a quartz-vein (‘‘ quartz-reef”’), are shallow at first, 2 or 3 feet in depth, and gradually get deeper. os 4. On some OUTLINE-DRAWINGS and PHoToGRAPHs of the SKULL of Zygomaturus trilobus, MacuEay, from AustRALtIA. By Pror. Owen, F.R.S., F.G.S. | [ Abstract. ] (The publication of this Memoir is unavoidably postponed.) ABour a month since, Prof. Owen received from Sir R. Murchison seven photographs, three of which are stereoscopic, of perhaps the most extraordinary Mammalian fossil yet discovered in Australia. These photographs, with a brief printed notice of their subject by William Sharp Macleay, Esq., F.L.S., and some MS. notes by J. D. Macdonald, M.D., R.N., had been transmitted to Sir R. Murchison by His Excellency Governor Sir W. Denison, from Sydney, New South Wales ; and by desire of Sir Roderick the Professor brought the subject under the notice of the Geological Society of London, to whom Sir Roderick desires to present the photographs on the part of His Excellency Sir W. Denison. Professor Owen had some weeks previously received from George Bennett, Esq., F.L.S., of Sydney, outlines of the same fossil skull, * Some of the cones brought by Mr. Redaway were submitted by Sir R. Mur- chison to the late Dr. Robert Brown, who identified them as belonging to the Banksia. 2N 2 542 PROCEEDINGS OF THE GEOLOGICAL SocteTy. [Mar. 10, made by him on the reception of the specimen by the authorities of the Australian Museum at that town; and the Professor had penned notes of his comparisons of these sketches before receiving the photographs and descriptions of the fossil skull from Sir R. I. Mur- chison. This. unique and extraordinary skull of a probably extinct Mam- mal, together with other bones, but without its lower jaw, were found at King’s Creek, Darling Downs,—the same locality whence the entire skull and other remains of the Diprotodon had been ob- tained. Mr. Macleay has described the fossil under notice as belonging to a marsupial animal, probably as large as an Ox, bearing a near approach to, but differing generally from, Diprotodon. He has named it Zygomaturus trilobus. 'The skull has transversely ridged molars, and a long process descending from the zygomatic arch, as in the Megatherium and Diprotodon, and exhibits an extraordinary width of the zygomatic arches. The skull at its broadest part, across the zygomata, is 15 inches wide, and is 18 inches long. In Diprotodon the skull is about 3 feet long by 1 foot 8 inches broad ; so that while the latter must have had a face somewhat like that of the Kangaroo, the Zygomaturus more resembled the Wombat in the face and head. Prof. Owen stated that, from the evidences afforded by the photo- graphs, he finds the dentition of this upper jaw to consist of three incisors and five molars on each side, of which the first appears to be c . 3—3 0—0 1—1 4—4 a premolar and the rest true molars, 7.e. 7. —-, c.—, p.—,m.— , agreeing, in this formula, with Macropus and Diprotodon. 'The mo- difications of this dentition resemble those of the latter genus in the retention of the premolar after the last true molar has come into its place, and in the superior size of the first, as compared with the second and third incisors. He then described in detail the sockets of the incisors, and the form and conditions of the molar teeth, which are highly characteristic of the marsupiality of this huge and most strange extinct quadruped. The cranial characters, which were next described, equally elucidate this affinity. The peculiar facial bones were then described in detail, that portion in advance of the orbits forming, as it were, a short pedunculate appendage to the rest of the skull, increasing in a remarkable manner in both ver- tical and lateral extent as it approaches the muzzle, but not offering sufficient evidence of having borne a nasal ‘horn, as thought to be probable by Mr. Macleay. The cavity of the nose is divided by a bony septum,—a character which Prof. Owen has lately found to exist also in a rare species of living Wombat—to a much greater ex- tent than in other known marsupials. Wholly concurring in Mr. Macleay’s conclusions as to the marsupial nature of the fossil in question, Prof. Owen dees not find, in the absence of an opportunity of comparing the structure of the teeth themselves, that it exhibits evidences of a generic distinction from Diprotodon. The Professor suggested, however, that probably the lower jaw, when found, may show some peculiarities of dentition and proportions similar to those 1858. | ROSALES—BALLAARAT. 543 on which he had founded the genus Nototherium, with one species of which, NV. Mitchell, the cranium in question agrees in size. oe 5. On the Gouiv-Dicernes at Batuaarat. By Henrique Rosaes, Esq. (in a letter to W. W. Smyth, Esq., Sec. G.S.) ** By the aid of machinery, and through the alteration of the mining- regulations granting extended claims, the old ground has been pro- fitably re-worked: and, by the introduction of the frontage-system, which, according to the difficulties to be overcome, grants extensive claims on new ground, the present ‘leads,’ most of which are N.W. of the Gravel Pits, under the townships, are advantageously worked. The amalgamation of three or more claims is also allowed, the miners having then to put down only one shaft. «The engines most in use are stationary, of from 15 to 20 horse- power, with winding and reversing gear. To the end of the winding- gear-shaft is attached the crank for the pump; and the motion is also taken to drive a puddling machine, which is nothing but the arrastra working without mercury. The depth of sinking averages about 300 feet, of which in some instances there are as much as 200 of basalt to be cut through. «« At the junctions of the Frenchman’s and White Horse Leads, in the Eldorado, the remains of a tree were found in an undisturbed position, with the roots fast in the wash-dirt. “It might also be interesting to you to know that at Poverty Point the deep gold-channel, with a N.W. strike (figs. 1 & 2, 1,1), is Fig. 2.—Vertical plan of the * Runs.” Fig. 1.—Horizontal plan of te ; the “ Runs.” ¥ = 2 XK : Ey pane aa 1. Present water-course, at“the surface. 2. An older water-course, or “run.” 3. The oldest and lowest “run,” or ‘ gold-channel.” crossed at about 140 feet higher by the shallow gold-channel (2,2\, which has a strike of N.E. by E., and which again, in its turn, is crossed at a level of 20 or 30 feet still higher, by the present water- course (3,3), the strike of which is W.” 044 DONATIONS TO THE LIBRARY OF THE GEOLOGICAL SOCIETY. From April 1st, 1858, to June 30th, 1858. I. TRANSACTIONS AND JOURNALS. Presented by the respective Societies and Editors. AMERICAN Journal of Science and Arts. 2nd Series, vol. xxv. No. 74. March 1858. From Prof. B. Silliman, For. Mem. GS. A. A. Gould.—Obituary notice of Prof. J. W. Bailey, 153. J. Wyman.—Batrachian Reptiles from the Coal-formation of Ohio, 158. T. E. Clark.—Fiehtelite, 164. R. Owen.—Classification of the Mammalia, 177. G. J. Brush.—Chaleodite, 198. L. Agassiz.—Contributions to the Natural History of the United States [noticed], 202. T. S. Hunt.—Ophiolites, 217. W. P. Blake.—Chalchihuitl of the Mexicans, 227. C. Johnston.—Microscopical Preparations, 233. R. P. Stevens.—New Carboniferous Fossils, 258. Dumas.—Equivalents of the Elements, 267. Buff and Wohler.—New Compounds of Silicon, 270. Wobhler and Deville.—New researches on Boron, 271. J. Pliicker.—Magnetic Induction of Crystals, 272. H. Falconer.—Mastodon, 274. E. Daniels.—Geological Survey of Wisconsin, 275. J. Dawson.—Pliocene Deposits of Montreal, 275. J. Hall.—Crinoids of New York, 277. DeMorlot.— Cervus euryceros? in Canton Berne, 279. A. R. Wallace.—Former Connexion of Australia, New Guinea, and the Aru Islands, 280. Earthquake in Italy, 280. W. Stein.—Coal of Saxony, 283. bie Harsiate Remains near Mexico, 283. D. Owen.—Geological Survey of Kentucky, 283. Tab Lesquereux and H. D. Rogers.—New Species of Fossil Plants from the Pennsylvanian Coal-fields, 286. J. G. Norwood.—Geological Survey of Illinois, 286. DONATIONS. 545 American Journal of Science and Arts (continued). T. S. Hunt.—Silicates of Alkalies and Metamorphic Rocks, 287. R. B. Smyth.—Extinct Volcanos of Victoria, Australia, 289. G. M. Sanders.—System of Instruction in the Practical Use of the Blow-pipe [noticed]. 300. G. C. Swallow.—Permian Strata in Kansas, 305*. —. No. 75. May 1858. Agassiz.—Contributions to the Natural History of the United States {noticed ], 321. T. S. Hunt.—Extraction of Salts from Seawater, 361. J. J. Dana.—Fifth Supplement to Dana’s ‘ Mineralogy,’ 396. T. S. Hunt.—Origin of Feldspars, 435. Euphotide and Saussurite, 437. Von Hauer.—Equivalents of Cadmium and Manganese, 438. F. B. Meek and F. V. Hayden.—Fossils of Nebraska, 439. Permian Fossils of Kansas and New Mexico, 442, 451. Kosakewitsch and Hallstrém.—Rise of the Shores of the Baltic, 443. Walferdin.—Temperature of the Earth at great depths, 443. W. E. Logan.—Geological Survey of Canada, 444. Miscellaneous, 446. Assurance Magazine. Vol. vii. part 5. No. 31. April 1858. Atheneum Journal for April, May, and June. From C. W. Dilke, Esq., F.G.S. Notices of Scientific Meetings, &c. J. C. Warren.—Description of a Skeleton of the Mastodon giganteus, 495. R. P. Gregg and W. G. Lettsom.—Manual of Mineralogy of Great Britain, 497. Sir W. Jardine.—Memoirs of H. E. Strickland [noticed], 746. Bent’s Monthly Literary Advertiser. Nos. 647-650. | Berlin. Monatsbericht Konig]. Preuss. Akad. Wissensch. Sept.— Dec. 1857. Ehrenberg,— Ueber die organischen Lebensformen in grossen Tiefen des Mittelmeeres, 538. Brussels. Annuaire de Académie Royale des Sciences, des Lettres et des Beaux-Arts de Belgique, 1858. J. J. @O. d’Halloy.—Notice sur André Dumont, 91. Bulletins de Académie Royale des Sciences, des Lettres et des Beaux-Arts de Belgique. 26™° Année, 2™° Série, 1857. Vol. i. Vol. ii. Dewalque.—Sur les grés liasiques du Luxembourg, 345 (map). _ De Koninck.—Sur deux nouvelles espéces siluriennes du genre Chiton, 190 (plate). | _._ Mémoires Couronnés, et autres mémoires publi¢s par l’Aca- démie Royale des Sc., etc. de Belgique. Collection in 8vo. Vol. vii. 1858. A. Perrey.—Documents sur les tremblements de terre au Pérou dans la Colombie et dans le bassin de Amazone. 546 DONATIONS. Caen. Bulletin de la Société Linnéenne de Normandie. Vol. i Année 1855-56. 1856. E. Deslongchamps.—Une coupe géologique a Eurecy (Calvados), 17 (plate). nue Sur le Cornbrash 4 Lion-sur-mer (Calvados), 25 (plate). E. Suess.—Sur le genre Meganteris, 56 (plate). E. Deslongchamps.—Sur deux nouveaux Brachiopodes des Terrain’s Crétacés du Dép. de la Manche, 68 (plate). Sur la Géologie de la presqu’ile Nord, dép. de la Manche, 76. A. Perrier.—Sur le Kelloway-rock et le Cornbrash des environs d’Argetan, 81. KE. Deslongchamps.—Catalogue des Brachiopodes de Montreuil-Bel- lay, 95 (plate). Sur le genre Eligmus, 105 (plate). Levavasseur.—Fossiles tertiaires de Fleury-la-Riviére, 119. Promenade géologique 4 Harcourt, 126. Canadian Journal of Industry, &c. New Series, No. 15. May 1858. T. S. Hunt.—Theory of Igneous Rocks and Volcanos, 197. EK. J. Chapman.—Assaying Coals by the Blow-pipe, 208. New Canadian Trilobites, 230. Agassiz.—Contributions to Natural History [noticed], 243. Geological Survey of Canada, 260. Permian Rocks in the United States, 261. Fossil Batrachians from the Coal-strata of Ohio, 261. Chalcodite, Saussurite, &c., 262. Alleged discovery of Gold in Western Canada, 262. Canadian Naturalist and Geologist, and Proceedings of the Natural History Society of Montreal. Vol. iu. Nos. 1&2. 1858. Things to be observed in Canada, 1. Metallurgy of Iron, 13. Results of Geology, 67. Permian Fossils in Kansas, 80. Geological Survey of Canada, 81. T. S. Hunt.—Extraction of Salts from Seawater, 97. W. E. Logan.—Ice in the St.. Lawrence, 115. J. Hall.—Graptolithus, 139 (plate). Chemical Society, Quarterly Journal. Vol. xi. part 1. April 1858. F. Field.—Arseniates of Baryta, Lime, and Magnesia, 6. J. Liebig and C. Daubeny.—Chemical Action of Roots in Soils, 53. Cherbourg. Mémoires de la Soc. Imp. Se. Nat. de Cherbourg. Vol. ive .1856. Bonissent.—Sur le gisement de quelques roches du département de la Manche, 281. E. Liais.—Appareil destiné 4 puiser de l’eau de mer, 289. Colliery Guardian. Nos. 13-16, 18-26. March to June, 1858. W. W. Smyth.—Mineralogy, 196, 197, 212, 213, 228, 229, 244, 245, 323, 339, 388; Coal, 356, 372; Salt and Barytes, 404 ; Meusaae phism oe Rotks, 340; Sertiueion: o00.23/ 05 404 A. C. Ramsay.—Strata, Fossils, Glaciers, 197, 213, 229, 245; Central Heat, 275; Volcanos, 292; Earthquakes, 308. R. Owen.—Fossil Birds and Reptiles, 198, 214, 229. H. Mackworth.—Smelting Iron-ore, 198 ; Boring, 277 ; Metals, 230. M. Fryar.—Coal, 214. DONATIONS. 547 Colliery Guardian (continued). E. W. Binney.—The Lower Coal-field of Lancashire, 246. Henry.—Chemistry of Minerals, 275, 292; Blowpipe, 308. R. Owen.—Fossil Reptiles, 276, 293, 309. J. A. Phillips.—Progress and Present State of British Mining, 277. J. Tennant.—Composition of Rocks, 294, 309; Mineralogy, 340, 389. L. Brough.— Working Mines, 310. C. Sanderson.—Iron, 310, 325. R. Godwin- Austen.—Probability of Coal beneath London, 341. R. Owen.— Oolitic Crocodilia, 357. Museum of Practical Geology, 357. T. Sopwith.—Dean Forest Coal-field, 373. H. D. Rogers.—Anthracite of Pennsylvania, 375. P. S. Hamilton.—Coal-fields of Nova Scotia, 375. A. Melville—Geology, 389, 405. J. W. Watson.—Ironstone of Dean Forest, 390, 406. Iron-districts of Great Britain, 405. Copenhagen. Videnskabelige Meddelelser fra den naturhistoriske Forening i Kjobhavn for Aarene 1849 og 1850; og for Aaret 1852. From Sir C. Lyell, F.G.S. Critic. Nos. 408-410. Notices of Scientific Meetings, &c. France. Congrés Scientifique de France. 22™¢ Session, 1855, vol. i. 1856. G. P. Scrope.—Sur les Phénoménes Volcaniques, 779. Geologist. Vol.i. Nos. 4, 5,6. April to June, 1858. G. E. Roberts.—Lower Carboniferous beds of the Clee Hills, 121. G. P. Bevan.—Geology of Beaufort and Ebbw Vale, South Wales, 124. S. J. Mackie.—Common Fossils, 134, 238. J. Morris.—Stratigraphical Catalogue of British Fossils, 138, 189, 233. J. E. Vaux.—Lord Dufferin’s notices of Volcanic Phenomena in Ice- land, 142, 175. T. L. Phipson.—Foreign Geological Notices, 149, 194, 243. P. Gervais.—Teeth of Auchitherium from the Isle of Wight, 153. D. T. Ansted.—Gold in Wales, 154. A. C. Ramsay.—Physical Structure of Merionethshire and Caernar- vonshire, 169 (plate). L. de Koninck.—New Paleozoic Crinoids, 178. J. Buckman.—Coal-seeking, 184. T. R. Jones.—Artificial Human Foot-prints, 204. J. W. Watson.—Ironstone of the Forest of Dean, 218. P. B. Brodie.—Geology of Gloucestershire, 227. T. R. Jones.—Preparation of Chalk, Clay, and Sand for the Micro- scope, 249. J. Prestwich.—British localities for Fossil Mammalia, 251. Notes and Queries, 155, 205, 253. Reports of Societies, 162, 210, 257. Reviews, 167, 213, 263. Grahamstown Eastern Province Magazine. Vol.i. Nos. 8 and 10. From Dr. R. N. Rubidge. A. G. Bain.—Geology of South Africa, 396. ! H. Hall.—Physical Features of South Africa, 432. A. G. Atherstone.—Geology of Uitenhage, 518. 548 DONATIONS. Great Britain, Geological Survey. Annual Report of the Director- General of the Geological Survey of the United Kingdom, the Museum of Practical Geology, and the Government Schvol of Mines &c., 1858. Halle. Zeitschrift fir die gesammten Naturwissenschaften, her- ausgegeben von dem Naturw. Vereine fiir Sachsen u. Thiringen in Halle, redigirt von C. Giebel und W. Heintz. Vol. viii. 1856. Fr. Bruns.—Analyse von Oberharzer Bleischlacken, 495. R. Eisel.—Zur Umgebung von Gera [ Zechsteingebirge ], 16. C. Giebel.—Das Kreidegebirge in Thiiringen, 169. —. Ueber Saurier- und Fisch-Reste aus dem Thiiringer Keuper, 422 (plate). . Br. Kerl.—Arbeiten im Metallurgisch-chemischen Laboratorium zu Clausthal, 477. C. Kuhlemann.—Analyse von eimigen Oberharzer Mineralien, 519. Nilsson.—Ueber fossile in Schonischer Kreide gefundene Saurier und Fisehe, 504. C. Giebel.— Geologische Uebersicht der vorweltlichen Insecten, 174. E. Séchting.—Mineralogische Notizen, 517. Von Strombeck.—Das Alter des Flammenmergels im Nordwestlichen Deutschland, 349. Suckow.—Mineralogische Notizen, 289 (plate). Weichsel.— Mineralogische Vorkommnisse in den Braunkohlenlagern von Helmstadt und Leesen, 346. Zinken.—Die Geognostische Verhaltnisse der Umgegend von Bern- burg, 344. Geologische, Oryctognostische und Palaeontologische Notizen. Voli mm, ©1857. C. Chop.—Ueber die Zahne und Fischreste aus dem Schlotheimer Keuper, 127 (plate). G. K. Gerlach.—Analyse eines Triphillius, 149. C. Giebel.—Dichelodus, ein neuer Fisch im Mansfelder Kupferschiefer, 121 (plate). Zur Fauna des lithographischen Schiefers von Solenhofen (neue Insekten, Krebs, Holothurien), 378 (2 plates). H. Neimke.—-Erfahrung bei der Sprengarbeit in den Oberharzer Gruben, 11. C. Oberbeck.—Ueber die Schichtung und falsche Schieferung der Wissenbacher Schiefer und die Beziehung derselben zu den darin auftretenden Diabasen im Nordwestlichen Theile des Harzes, 22 (3 plates). C. Prediger.—Beitrage zur hypsometrischen Kenntniss des Harzge- birges, l. C. Gicbel-Die Palaozoischen Arten der Gattung Capulus, 162. —. Die Erdschiitterung in Sachsen und Thiiringen am 7 Juni 1857, 438. ——. Ueber Hm. Bornemann’s Entdeckung der Kreideformation in Thirimgen, 455. Von Gross.—Ueber die Ordnung einer geognostischen Gesteins- sammlung, 153. Purgold.—Von den Krystallen und ihrer Entstehung, Pe Séchting.— Paragenesis von Weissbleierz und kohlensaurem Kupfer- oxydhydrat, 168. Stiehler—Die Flora im Quadersandsteme des Langenberges bei Quedlingburg, 452. | DONATIONS. 549 Halle. Zeitschrift fir die Gesammten Naturwissenschaften, &c. Vol. ix. 1857 (continued). Weichsel.— Alte Berg- und Hiitten-werke am nordlichen Harzrande, 459. j Geol., Oryct. und Pal. Notizen. Heidelberg, Verhandlungen des Naturhistorisch-medizinischen Ver- eins zu. Nos. 2 to 4. G. Leonhard.—Ueber emige Mineralien aus der Umgegend Heidel- bergs, 45. Blum.—Ueber die Ursachen der Bildung verschiedener Krystall- formen bei ein und demselben Minerale, 78. H. G. Bronn.—Ueber ein verstemertes Dattelpalmenblatt, 84. Blum.—Mineralogische Mittheilungen, 103. H. G. Bronn.—Zur Fauna und Flora der bituminésen Trias-Schiefer von Raibl m Karnthen, 108. Illustrated Inventor. Nos. 22 and 24. Notices of Scientific Societies, &c. Daubrée.—Artificial Minerals, 334. A. Delesse.—On Metamorphism, 382. Institution of Civil Engmeers, Proceedings. Nos. 6-20. J. Henderson.—Dressing Tin- and Copper-ores in Cornwall. G. Robertson.—Hydraulic Mortar. International Association for obtaining a Uniform Decimal System. What is the Best Unit of Length? Report presented by the Council of the International Association, &c. 1858. Journal of the Indian Archipelago and Eastern Asia. Vol. ii. new Series. No. 3. From J. R. Logan, Esq., F.G.S. G. W. Earl.—Physical Geography of S.E. Asia and Australia, 278. Linnean Society, Journal of the Proceedings. Vol. ii. No. 8. May, 1858. Literary Gazette, for April, May, and June. From L. Reeve, Esq., F.G.S. Notices of Scientific Meetings, &c. W. B. Carpenter.—On Foraminifera, 357. R. P. Gregg, and W. G. Lettsom.—Manual of the Mineralogy of Great Britain and Ireland [noticed], 371. Hugh Miller.—Cruise of the Betsey [noticed], 585. Annual Report of the Geological Survey, 613. London, Edinburgh, and Dublin Philosophical Magazine. 4th Series, vol. xv. No. 100. April 1858. From R. Taylor, Esq., F.G.S. F. M. Jennings.—The Lakes and Rivers of Damascus, 260. C. J. F. Bunbury.—The Genus Neuropteris, 318. T. Huxley.—Cephalaspis and Pteraspis, 319. Plesiosaurus, 320. C. Forbes.—Coal in Southern Chili, 321. Crabs thrown up in Payta Bay, 321. . I. Murchison.— Paleozoic Rocks of the N.W. Highlands, 322. G. G. Gemmellaro.—Gradual Elevation of the Coast of Sicily, 325. T. F. Jamieson, K. Macnab, and R. Mason.—Elevation of Land, 325. a 550 DONATIONS. London, Edinburgh, and Dublin Philosophical Magazine. 4th Series, vol. xv. No. 101. May 1858. J. Tyndall and T. H. Huxley.—Structure and Motion of Glaciers, 365. A. R. C. Selwyn.—Gold-fields of Victoria, 400. J. Phillips, Gold-field of Ballaarat, 401. W. Redaway.—Gold-diggings of Creswick Creek and Ballaarat, 402. R. Owen.—Zygomaturus trilobus of Macleay, 403. No. 102. June 1858. EK. J. Chapman.—Assaying of Coals by the Blowpipe, 433. Buff and Wohler.—New Compounds of Silicon, 457. H. Rosales.—Gold-diggings at Ballaarat, 483. J. C. Moore.—Silurian Rocks in Ayrshire, 482. G. W. Ormerod.—Rock-basins on Dartmoor, 484. J. Leckenby.—Kelloway Rock of Yorkshire, 484. N. T. Wetherell.—Nodules of London Clay and Crag, 484, S. V. Wood.—Fossils of Red Crag, 485. Wohler.—Nitrurets of Tungsten and Molybdenum, 488. Longman’s Monthly List of New Books. No. 184. Madrid. Memoria que comprende los Trabajos verificados en el afio de 1855 por las diferentes Secciones de la Comision encargada de formar el Mapa Geoldgico de la Provincia de Madrid y el General del Reino. 1858. C. de Prado.—Seccion Geolégico-paleontolégica 9 (map). J. V. y Piera.—Seccion Geoldgica del Este de Espana, 11. I. G. de Salazan.—Resefa de los Trabajos practicados en la Provincia de Leon durante el ano 1855, 23. Moscow. Bulletin de la Société Impériale des Naturalistes de Mos- cou. Année 1856, Nos. 2-4. KE. Eichwald.—Beitrag zur Geographischen Verbreitung der fossilen Thiere Russlands, 406, 555. E. Kirévsky.—Description d’une Chaux Carbonatée sur des Monti- cules de Sable dans les Steppes de l’Asie Centrale, 454. R. Hermann.— Untersuchung des Wassers der Narsan-Quelle, 307. H. J. Holmberg.—Geognostische Reise nach Ost-Finland, 503. G. von Jaeger.— Ueber emen durch ringformige Erhohungen (Wachs- thumsringe ?) ausgezeichneten hochst wahrscheinlich fossilen Stoss- zahn des Elephanten, 609 (plate). Erdbeben in Sselenginsk, 636. ———=-, Amncellt57. Ne: 1. R. Hermann.— Ueber Niobium, 3. V. Kiprijanoff.—Fisch-Ueberreste im Kur skschen eisenhaltigen Sand- steme, 151 (2 plates). E. Eichwald.—Zur Geographischen Verbreitung der fossilen Thiere Russlands, 192. Nordenskiold.— Ueber Lazurstein und die mit demselben vorkom- menden Mineralien, 213. G. Romanovsky.— Ueber die Verschiedenheit der beiden Arten, Chz- lodus tuberosus, Gieb. und Dicrenodus okensis, Rom., 290 (figures.) ——_—_—- e Newport. Catalogue of the Isle of Wight Museum im Newport. From E. P. Wilkins, Esq., F.G.S. ee ee ee ee aad oe : DONATIONS. 5p kL Paris, L’Ecole des Mines: Annales des Mines. Cing. Sér. vol. xii. 6° livraison de 1856. Bibliographie, i. Daubrée.—Sur le striage des roches, sur la formation des galets, des sables et du limon, et sur les décompositions chimiques produits par les agents mécaniques, 535. Lan.—La Sierra-Morena et le Nord de l’Andalousie, 561 (plates). Ville.—Les travaux du laboratoire du service des mines de la pro- vince d’Alger, 629. Lan.—De |’école des mineurs de St.-Etienne, 693. Delesse.—Sur le métamorphisme (suite), 705 (plate). Sur la mortalité des mineurs dans le district de Saint-Just en Penwith (Cornwall), 773. Sur lextraction de la houille dans l’Oural, 781. Sur le projet d’éclairage des mines par le gaz, 782. Exploitation de l’anthracite dans les terres de l’armée du Don, 783. rey mines du canton de Caratal (république de Venezuela), 800, Sur des expériences relatives aux moyens d’absorber la fumée de la houille, 804. Mines de fer des Etats—Unis, 805. Production des métaux dans le monde entier, 834. —. Bullet. Soc. Géol. France. Deux. Sér. vol. xiv. feuillet. 33-38. E. Piette.—Sur le gite des Clapes (Moselle), 513. Marcel de Serres.—Sur l’identité de ? Echinus lividus de ? Océan avec celui de la Méditerranée, 518. P. Marés.—Sur la constitution générale du Sahara dans le sud de la province d’Oran, 524. Th. Ebray.—Profil géologique du chemin de fer d’Orléans. Partie comprise entre Iteuil et Chatellerault, 538. EK. Piette. Description des Cerithiuwm enfouis dans les dépéts batho- niens de |’Aisne et des Ardennes (Plates V. VI. VII. VIII.), 544. Se. Gras.—Sur la réalité de l’association des plantes houilléres aux coquilles lasiques dans les Alpes, et comment on peut l’expliquer (Plate IX.), 562. Th. Ebray.—Sur lage du caleaire 4 chailles des départements du Cher, de la Niévre et de l’Yonne, 582. J. Barrande.—Sur louvrage de M. le professeur Geinitz, intitulé : Les houilles du royaume de Saxe (Die Steinkohlen des Konigreichs Sachsen), 586. A. Buvignier.—Sur le terrain jurassique de la partie orientale du bas- sin de Paris, 595. —— ——. Table pour la treizi¢me vol. Vol. xiv. feuil. 39-45. A. Buvignier. — Sur le terrain jurassique de la partie orientale du bassin de Paris (fin), 609. Ch. Laurent.—Puits artésiens du Sahara oriental (Plates X. XI. XII.), 615. Guiscardi.—Sur les émanations gazeuses des champs Phlégréens, 633. G. Bornemann.—Sur les phénoménes volcaniques, et sur la géologie de I’ile de Sardaigne, 635. ee 552 DONATIONS. Paris. Bullet. Soc. Géol. France. Deux. Sér. vol. xiv. feuillet. 39-45 (continued ). : J. Fournet.— De Vendomorphisme du spilite d’Aspres-les-Corps (Isére), 644. E. Bayle.—Sur quelques espéces de Rudistes (Plates XIII. XIV. XV.), 647. G. Dewalque.—Sur lage des grés liasiques du Luxembourg, 719. Vol. xv. feuil. 1-6. Ch. Lory.—Equisse d’une carte géologique du Dauphiné (PI. I.), 10. P. de Rouville.—Sur les environs de Saint-Affrique (Aveyron), 69. H. de Saussure.—Description d’un volean étemt du Mexique, resté , Inconnu jusqu’a ce jour, 76. Ebray.—Sur les Nautiles a cloisons sinueuses, 87. Casiano de Prado.—Sur quelques fossiles paléozoiques d’Espagne, 91. Daubrée.—Sur le métamorphisme et recherches expérimentales sur quelques uns des agents qui ont pu le produire, 93. Philadelphia Academy of Natural Sciences, Journal. New Series, vol. i. Part 4. 1858. T. A. Conrad.—New Cretaceous Fossils from Tippah County, Miss., 323 (2 plates). Photographic Society, Journal. Nos. 65-67. Quarterly Journal of Microscopic Science ; including the 'Transac- tions of the Microscopical Society of London. No. 23. April 1858. W. K. Parker.—The Miliolitide, 53 (plate). Royal Astronomical Society, Memoir. Vol. xxvi. 1858. » Monthly Notices. Vol. xvii. 1857. Royal Geographical Society, Journal. Vol. xxvii. 1857. Sir R. I. Murchison.— Anniversary Address, xciv. W. C. Grant.—Vancouver Island, 268 (map). Dr. Livingstone.—Interior of Africa, 349 (map). - Proceedings. Vol. ii. No.2. March 1858. A. S. Waugh.—Mounts Everest and Deodanga, 102 (map). Royal Literary Fund. A Summary of Facts drawn from the Records of the Society, &c.; and Report of the Proceedings, March 12, 1858. Royal Society. List of Fellows. 1857. Report on the Adjudication of the Copley, Rumford, and. Royal Medals; and appointment of the Bakerian, Croonian, and Fairchild Lectures. 1834. , Transactions. Vol. 146. Part 3. 1856. —,——.. Vol. 147. Parts 1 and 2. 1857-58. H. J. Brooke.—Geometrical Isomorphism of Crystals, 29 (4 plates). R. Owen.—Scelidotherium leptocephalum, 101 (2 plates). J. Tyndall and T. H. Huxley.—Structure and Motion of Glaciers, 327. P. Yorke.—Siliea, 533. —— DONATIONS, 553 Royal Society, Proceedings. Vol. ix. No. 30. 1858. W. Thomson.—Interior Melting in Ice, 141. R. Owen.—Placodus laticeps, and the Saurian Nature of the Genus, 157. T. S. Hunt.—Some Magnesian Rocks, 159. Scarborough Philosophical and Archeological Society. Twenty- sixth Report. 1858. Society for the Suppression of Mendicity. Fortieth Report. 1858. Society of Arts, Journal. Nos. 279-291, 293. S. Bleekrode.—Platinum of Borneo, 360. J. Wilson.—Productions and Resources of Canada, 402. C. Sanderson.—Iron, 381. Somersetshire Archeological and Natural-History Society, Proceed- ings during the years 1856-7. 1858. W.A. Jones.—Bone-caverns of the Mendips, 25. South Wales Institute of Engineers, Proceedings. Vol.i. No. 1. January 1858. From E. Rogers, Esq., F.G.S. Statistical Society of London, Journal. Vol. xxi. Part 2. June 1858. Stuttgart. Wirttemb. naturw. Jahreshefte. Dreizehnter Jahrg. drittes Heft. 1857. A. Oppel.—Die Juraformation Englands, Frankreichs und des siid- westlichen Deutschlands, 289 (plate). Surrey Archeological Society, Transactions (Collections), for the years 1854-55. Vol.i. Part 1, 1856; and Part 2, 1858. University College, London, Proceedings at the Annual General Meeting, 24th February, 1858. Warwickshire Natural-History and Archzeological Society, Twenty- second Annual Report. 1858. Zoological Society, Proceedings, Nos. 339-349. Il. GEOLOGICAL CONTENTS OF PERIODICALS PURCHASED FOR THE LIBRARY. Annals and Magazine of Natural History. 3rd Series, vol. i. No. 4. April 1858. T. R. Jones.—Palzozoic bivalved Entomostraca of North America, 241 (2 plates). R. Owen.— Lectures on Paleontology (Relations of the Archegosau- rus), 317. -- No.5. May 1858. J. MacAdam and W. Thomson.—A new fossil Cirripede, 321. T. R. Jones.— Paleozoic bivalved Entomostraca from Canada, 340. J. Prestwich.—The Ground beneath us [noticed], 362. R. Owen.— Ichthyosaurus and Plesiosaurus, 388. — $= 554 DONATIONS. Annals and Magazine of Natural History. 3rd Series, vol. i. No. 6. June 1858. R. Owen.—Fossil Crocodiles of the Oolite, 456. Quenstedt.—The Dorsal Cavity of certain Ammonites, 465. Edinburgh New Philosophical Journal. New Series, No. 14. Vol.vii. No.2. April 1858. W.S. Symonds.—Carboniferous and Old Red deposits, 222. H. C. Sorby.—Ancient Physical Geography of the South-east of England, 226. G. C. Moreno—Voleano of Pichincha, 290. J. M‘Bain.—Skull of a Wombat from the bone-caves of Australia, with remarks on the Marsupiata, 308. A. Rose.—Hematites in Ayrshire, 309. A. Taylor.—Artesian Spring in Linlithgowshire, 310. C. Maclaren.—Great Irish Elk, 327. —. Earliest Animal Life, 328. L. Horner.—Antiquity of the Human Race, 328. H. C. Sorby.—Microscopical Structure of Crystals, 331. J. W. Dawson.—Pliocene deposits at Montreal, 333. E. de Verneuil.— Vesuvius, 333. W. R. Holmes and W. H. Campbell.—Expedition to the Gold-fields of Caretal, 334. Leonhard und Bronn’s Neues Jahrbuch fiir Min., Geogn., Geol. und Petref. Jahrgang 1858. Erstes Heft. H. G. Bronn.—Zur triasischen Fauna und Flora der bituminosen Schiefer von Raibl, 1 (5 plates). A. Knop. —Histologisch merkwiirdige Erscheinungen an Gang-ge- steinen aus dem Hochstatter Thale bei Auerbach an der Bergstrasse, 509. Perimorphosen von Kalkspath und Epidot m Granat, 33 (plate). ¥. Rocwer —Zweites Exemplar von Archeoteuthis Dunensis aus dem Thonschiefer von Wassenach am Laacher See, 55. Letters; Notiges of Books, Mineralogy, Geology, and Fossils. Jahrg. 1858. Zweites Heft. H. G. Bronn.—Beitrage zur Fauna und Flora der bicuaineee Schiefer von Raibl, 129 (4 plates). ——. Ueber die Farnen-sippe Chiropteris (Kurr), in Lettenkohl-Sand- stein, 143 (plate). N. Girard.—Ueber die Melaphyre in der Gegend von Ilfeld am Harze, 145 (plate). C. Bergemann.—Ueber Ehlit, ein Phosphor- und _Vanadinsaures Kupfer-Oxyd, 190. Letters; Notices of Books, Minerals, Geology, and Fossils. oe III. GEOLOGICAL AND MISCELLANEOUS BOOKS. Names ge Donors in Italics. Abert, J. W. Report of an Expedition on the Upper Arkansas and through the country of the Camanche Indians, in the fall of the year 1845. From Sir C. Lyell, F.G.S. DONATIONS. 555 Abich, H. Ueber die Erscheinung brennenden Gasesim Krater des Vesuv im Juli 1857, und die periodischen Veranderungen, welche derselbe erleidet. 1858. Adams, C. B. First Annual Report on the Geology of Vermont. 1845. From Sir C. Lyell, F.G.S. Adams, J. Descriptive Sketch of St. Paul’s Island, at the entrance of the Gulf of St. Lawrence. 1835. From Sir C. Lyell, F.G.S. Archiac, A.d@’. Etudes Géologiques sur les départements de l Aude et des Pyrénées-orientales. 1857. Histoire des progrés de la Géologie de 1834 4 1856. Tome Septiéme, Formation Jurassique (2° partie). 1857. Histoire des progrés de la Géologie (Notice of). 1858. Bache, A. D. Report of the Superintendent of the Coast Survey for 1848. From Sir C. Lyell, F.G.S. Baddeley, F. H. Geological Sketch of the most South-eastern por- tion of Lower Canada. 1835. From Sir C. Lyell, F.G.S. . On the Magdalen Islands. 1833. From Sir C. Lyell, ~FAG.S. Bakewell, R. On the Falls of Niagara, and on the Physical Struc- ture of the adjacent Country. 1830. From Sir C. Lyell, F.G.S. Barrande, J. Observations sur les rapports de la Stratigraphie et de la Paléontologie. 1854. From Sir C. Lyell, F.G.S. Bayo, J. Esquerra del. Die Bergwerke von Hiendelencina in der Provinz Guadalajara (Spanien). From Sir C. Lyell, F.G.S. Bechi, EF. Studi sulla formazione dei Soffioni Boraciferi, e nuovi metodi praticati in Toscana per ottenere dai medesimi |’ Acido ibaricos\s1Sase Berkley, J. J. Paper on the Bhore Ghaut Railway-incline. 1858. Binney, Amos. The Terrestrial Air-breathing Mollusks of the United States and the adjacent territories of North America. Edited by A. A. Gould. Vols. i.-and ii. 1851. Vol. iii. (plates), 1851- 57. From Dr. A. A. Gould and Dr. D. D. Storer. Bland, T. Description of Two New Species of North American Helicide. 1858. Brumby, R.T. A Brief Account of the Analysis of the Blount, Shelby, and Talladega Springs (Alabama). 1838. From Sir C. Lyell, F.G.S. Buist, G. Notes on certain discoloured Appearances met with on the Surface of the Sea in warm latitudes. 1854. From Sir C. Lyell, F.G.S. Bunsen, R. Ueber den innern Zusammenhang der pseudovolkani- schen Erscheinungen Islands. From Sir C. Lyell, F.G.S. Ueber die Processe der vulkanischen Gesteinsbildungen Is- lands. From Sir C. Lyell, F.G.S. VOL. X1V.—PART I. 20 556 DONATIONS. Catullo, T. dA. Prospetto degli Scritti publicati da Tomaso Antonio Catullo, Professore, &c., compilato da un suo amico e discipulo. 1857. Cooper, W. Notices of Big-bone Lick. 1831. From Sir C. Lyell, F.G.S. Cotta, B. Erzgangbildung in der Sohle eines Flammofens der Konigl. Muldner Schmelzhiitte bei Freiberg. 1851. From Sir C. Lyell, F.G.S. Daubrée, M. Observations sur le Métamorphisme, et recherches experimentales sur quelques-uns des agents qui ont pu le pro- duire. 1858. Recherches expérimentales sur le striage des Rocker di aux phénoménes erratiques, sur la formation des Galets, des Sables et du Limon et sur les décompositions chimiques produites par les agents mécaniques. 1858. Davy, H. Six Discourses delivered before the Royal Society. 1827. From the Royal Society. Dawson, G. W. Familiar Letters to the People of Nova Scotia on the Useful Minerals of the Province. (Nos. 5 and 6.) 1848. From Sir C. Lyell, F.G.S. Dekay, J. E., L. C. Beck, T. A. Conrad, W. W. Mather, E. Em- mons, L. Vanuxem, J. Hall. Reports on the Natural History of the State of New York. 1838. From Sir C. Lyell, F.GS. Delaharpe, J. Notice sur la Géologie des environs de St.-Gervais (Savoie). From Sir C. Lyell, F.G.S. Delesse, Md. Métamorphisme des Reches (suite). Deville, Ch. Ste.-Cl. Etudes de Lithologie. From Sir C. Lyell, F.G.S. . Mémoire sur les Roches Volcaniques des Antilles. 1851. From Sir C. Lyell, F.G.S. Lettres 4 M. Elie de Beaumont sur ’éruption du Vésuve du 1 Mai 1855; Lettre 4 M. Dumas sur quelques produits d’éma- nation de la Sicile. 1856. From Sir C. Lyell, F.G.S. Dickeson, W., and A. Brown. Report on the Cypress Timber of Mississippi and Louisiana. 1848. From Sir C. Lyell, F.G.S. Ducatel, J.T. Annual Report of the Geologist of Maryland. 1840. From Sir C. Lyell, F.G.S. Egerton, Sir P.de M:G. Fossil Fishes of Great Britain [From the Decades of the Geol. Survey]. 1852-57. Emmons, E. Geology of the Montmorenci. 1841. From Sir C. Lyell, F.G.S. Gaudry, A. Recherches Scientifiques en Orient entreprises par les ordres du Gouvernement, pendant les années 1853-54. Partie Agricole. 1855. DONATIONS. 557 Gaudry, A. et E. Lartet. Mémoire sur les Résultats des Recherches paléontologiques entreprises dans l’Attique. 1856. From Sir C. Lyell, F.G.S. Gazetteer of the State of New York [Geological portion]. 1842. From Sir C. Lyell, F.G.S. Gemmellaro, C. Nuovi schiarimenti sulla Teoria dello Zolfo. 1854. From Sir C. Lyell, F.G.S. Gesner, A. Report on the Geological Survey of Prince Edward Island. 1847. From Sir C. Lyell, F.G.S. Giddins, E. An Inquiry into the causes of the Rise and Fall of the Lakes ; to which is annexed a letter to Dr. H. H. Sherwood on his Theory of Magnetism. 1838. From Sir C. Lyell, F.G.S. Goeppert, H. R. Ueber den versteinten Wald von Radowenz bei Adersbach in Bohmen, und iiber den Versteinungsprocess iiber- haupt. 1858. Hall, J. An Address delivered at the Anniversary Meeting of the Harvard Natural-History Society, May 24, 1848. From Sir C. Lyell, F.G.S. Niagara Falls, their Physical changes, and the Geology and Topography of the surrounding country. From Sir C. Lyell, F.G.S. Hall, J. Report on Canadian Graptolites [Geological Survey of Canada] (with Plates 1, 3, 4, 5, 6, 8). 1858. Hayes, G. E. Remarks on the Geology and Topography of Western New York. 1838. From Sir C. Lyell, F.G.S. Heer, O. Beschreibung der angefiihrten Pflanzen und Insekten. From Sir C. Lyell, F.G.S. Hill, S. W., L. W. Campbell, and C. Whittlesey. Reports: Phcenix Copper Company. 1855. From Sir C. Lyell, F.G.S. Hitchcock, E. Report on certain points in the Geology of Massa- chusetts. 1853. From Sir C. Lyell, F.G.S. Holmes, F. S. Remains of Domestic Animals discovered among the Post-pleiocene fossils in South Carolina. 1858. Hon, H. le. Périodicité des grands déluges résultant du mouvement graduel du la ligne des apsides de la terre. 1858. Horsfield, T., and F. Moore. A Catalogue of the Lepidopterous Insects in the Museum of the Hon. East IndiaCompany. Vol. 1. 1857. From the Hon. Hast India Company. Houzeau, J.C. Histoire du Sol de PEurope. 1857. Jackson, C. T., and A. A. Hayes. Remarks on the Alabama Meteoric Iron. 1844. From Sir C. Lyell, F.G.S. Jardine, Sir W. Memoirs of Hugh Edwin Strickland. 1858. Jennings, F. M. On the Lakes and Rivers of Damascus. 1858. Jones, T. Rupert. Notes on the Palzeozoic Bivalyed Entomostraca. No. IV. Some North American species. 1858. 202 558 DONATIONS. Keilhau, B. M. Darstellung der Uebergangs-formation in Norwegen (Uebersetzt von Dr. C. Naumann). 1826. From Sir C. Lyell, F.G.S. ——. Efterretningen om Jordskjelv i Norge. 1833. From Sir C. Lyell, F.G.S. Kelly, W. On the Temperature of the Springs at Quebec. 1835. From Sir C. Lyell, F.G.S. Koninck, L. de. Mémoires de Paléontologie [Chiton, Crinoides]. 1857-58. Kries, F. Von den Ursachen der Erdbeben und von den magneti- schen Erschemungen. 1827. From Sir C. Lyell, F.G.S. Lartet, E. Note sur un grand Singe fossile qui se rattache au groupe des Singes supérieurs. 1856. From Sir C. Lyell, F.G.S. Lartet, E. Sur les Migrations anciennes des Mammiféres de l’ Epoque actuelle. 1858. Eea, I. Observations on the genus Unio, together with descriptions of new species in the family Unionide. Vol. vii. part 1. 1857. Logan, Sir W. E. Geological Survey of Canada. Reports of Progress, 1844, 1845-46, 1846-47, 1847-48, 1848-49, 1849-50, 1850-51, 1851-52 ; and Report on the North Shore of Lake Huron, 1849. From Sir C, Lyell, F.G.S. , and others. Geological Survey of Canada. Report of Pro- gress for the years 1853-56, and Atlas of Plans of various Lakes and Rivers between Lake Huron and the River Ottawa. 1857. Lyons.—Commission Hydrométrique de Lyon. Résumé des Observa- tions recueillées en 1857 dans le bassin de la Saone. 1858. From the Hydrom. Commission of Lyons. Macadam, James. On a new fossil Cirripede. 1858. Magnetical and Meteorological Observations made at the Hon. E.I.C. Observatory, Bombay, in the year 1856, under the Superintendence of Lieut. K. F. T. Fergusson. 1857. From the Hon. E.I.C. Mather, W. W. First Annual Report on the Geological Survey of the State of Ohio. 1838. From Sir C. Lyell, F.G.S. Maury, M. F. The Amazon and the Atlantic Slopes of South America. 1853. From Sir C. Lyell, F.GS. Menteath, J. S. Memoir on the Geology of the Snowdon Range of Mountains, as connected with its Scenery, Soil, and Productions. From Sir C. Lyell, F.G.S. Meyer, H. von. Reptilien aus der Steinkohlenformation in Deutsch- land. Milligan, J. Reports on the Coal-basins of Van Diemen’s Land. 1849. From Sir C. Lyell, F.G.S. Montagna, C. Ghiacitura e Condizioni del Terreno Carbonario di Agnana. 1857. SEO DONATIONS. 559 Morton, 8. G. Synopsis of the Organic Remains of the Ferruginous Sand Formation of the United States. From Sir C. Lyell, F.G.S. Murray, J. An account of the Progressive Improvement of Sunder- land Harbour and the River Wear. 1849. From Sir C. Lyell, F.G.S. Nicollet, I. N. Report intended to illustrate a Map of the Hydro- graphical Basin of the Upper Mississippi River. 1843. From Sir C. Lyell, F.GS. Northcote, A. B. On the Brine Springs of Worcestershire. 1855. From Sir C. Lyell, F.G.S. Noulet, J. B. Du Terrain Eoctne Supérieur considéré comme l’un des Etages constitutifs des Pyrénées. 1857. From Sir C. Lyell, F.G.S. Olmsted, D. Notice (by S. Elliot) of the Report on the Geology of North Carolina, 1824-25. 1828. From Sir C. Lyell, F.G.S. Oppel, A. Die Juraformation Englands, Frankreichs und des siid- westlichen Deutschlands. Viertes Heft. 1858. Weitere Nachweise der Kossener Schichten in Schwaben und in Luxemburg. 1858. Owen, R. Description of a small Lophiodont Mammal (Pliolophus vulpiceps, Owen) from the London Clay near Harwich. 1858. Parliamentary Reports. From Sir P. Egerton, Bart., F.G.S. Further papers relative to the Recent discovery of Gold in Australia, Feb. 28, 1853. 1853, , Aug. 16, 1853. 1853. —, Feb. 1854. 1854. —, Dee. 14, 1854. 1855. ——, July 1855. 1855. ——, Feb. 1856. 1856. —, July 24, 1856. 1856. —, July 25, 1856. —, Aug. 25, 1857. 1857. Pictet, F. J. Matériaux pour la Paléontologie Suisse. Livr. 9-11. 1857-58. ——,. Notice sur les Poissons des Terrains Crétacés de la Suisse et de la Savoie. 1858. et A. Humbert. Description d’une Emyde nouvelle (Emys _Etalloni) du Terrain Jurassique Supérieur des Environs de St.- Claude. 1857. Prestwich, J. On the Correlation of the Eocene Tertiaries of En- gland, France, and Belgium (Part i.). 1855. . On the Thickness of the London Clay ; on the Relative Posi- - tion of the Fossiliferous Beds of Sheppy, Highgate, &c.; and on the Bagshot Sands in the Isle of Sheppy. 1854. Quetelet, A. Observations des Passages de la Lune et des Etoiles de méme culmination. 560 DONATIONS. Rennie, G. On the Employment of Rubble béton, or Concrete, in works of engineering and architecture. 1858. Review of the ‘‘ Reports on the Geological Relations, Chemical Ana- lysis, and Microscopical Examination of the Coal of the Albert Coal-mining Company, &c. 1852. From Sir C. Lyell, F.G.S. Rogers, H. D. Address on the Recent Progress of Geological Re- search in the United States. 1844. From Sir C. Lyell, F.G.S. Five Annual Reports on the Geological Survey of the State of Pennsylvania. 1836-1841. From Sir C. Lyell, F.G.S. and W. B. On the Geological Age of the White Mountains. From Sir C. Lyell, F.G.S. Rogers, W. B. Report of the Progress of the Geclaene Survey of the State of Virginia for the year 1840. From Sir C. Lyell, F.G.S. and H.D. Contributions to the Geology of the United States. 1843. From Sir C. Lyell, F.G.S. Scacchi, A. Dei Solfati doppi di Manganese e Potassa. 1857. From Sir C. Lyell, F.G.S. Scrope, G. P. The Geology and Extinct Volcanos of Central France. 2nd edition. 1858. Seguenza, G. Richerche Mineralogiche sui Filoni Metalliferi di Fiumedinisi e suoi dintorni in Sicilia. 1856. From Sir C. Lyell, F.G.S. Sella, Q. Sulla Legge di Connessione delle Forme Cristalline di una stessa sostanza. 1856. From Sir C. Lyell, F.G.S. Senoner, A. Il Museo di Storia Naturale dei Signori A. e G. B. Villa di Milano. Sewell, H. D. Travertine or Calcareous Tufa. 1835. From Sir C. Lyell, F.G.S. Shepard, C. Analysis of Meteoric Iron from Cooke County, Ten- nessee. 1842. From Sir C. Lyell, F.G.S. On Washingtonite. 1842. From Sir C. Lyell, F.G.S. . A Report on the Geological Survey of Connecticut. 1837. From Sir C. Lyell, F.G.S. Sismonda, Ange. Essai Géognostique dans les deux vallées voisines de Stura et de Vinay. 1831. From Sir C. Lyell, F.G.S. Sismonda, E. Note sur le Terrain Nummulitique Supérieur du Dego, © des Carcare, etc. dans lApennin Ligurien. 1856. From Str C. Lyell, F.G.S. Skey, J., and W. Kelly. Analysis of a Mineral Water sent from Gaspé. 1835. From Sir C. Lyell, F.G.S. . Statistics of Georgia [with Geological Map]. 1849. From Sir C. Lyell, F.G.S. Steininger, J. Bemerkungen iiber die Versteinerungen, welche in dem Uebergangs-Kalkgebirge der Eifel gefunden werden. 1831. From Sir C. Lyell, F.G.S. DONATIONS. 561 Taylor, 4. The Geological Difficulties of the Age-Theory. 1858. Taylor, R.C. Additional information on the Fucoides alleghaniensis. 1834. From Sir C. Lyell, F.G.S. . Geology and Natural History of the North-eastern extremity of the Alleghany Mountain Range, in Pennsylvania, U.S. 1835. From Sir C. Lyell, F.G.S. - Notes on Natural Objects observed while staying in Cuba. 1836. From Sir C. Lyell, F.GS. The Farewell Livingstone Festival. 1858. From Sir R. I. Mur- chison, .F.G.S. Totten, J. G. On Deepening the Channel at the Mouth of the Mississippi River. 1839. From Sir C. Lyell, F.G.S. Troost, G. Fifth Geological Report, Tennessee, 1839 ; and Sixth, 1841. From Sir C. Lyell, F.G.S. Tuomey, M. First Biennial Report on the Geology of Alabama. 1850. From Sir C. Lyell, F.G.S. Villa, 4. Intorno agli Studj Geologici e Paleontologici sulla Lom- bardia del Sacerdote Prof. A. Stoppani. 1858. Villa, G. B. Osservazioni Geognostiche e Geologiche fatte in una gita sopra alcuni colli del Bresciano e del Bergamasco. 1857. Walchner, Fr. A. Darstellung der geologischen Verhaltnisse der am Nordrande des Schwarzwaldes hervortretenden Mineralquellen. 1853. From Sir C. Lyell, F.G.S. Widmann, H. von. Erlauterungen zur geognostischen Karte Tirols und Schlussbericht der administrativen Direction des geognostisch- montanistischen Vereines fiir Tirol und Vorarlberg. 1853. From Sir C. Lyell, F.G.S. Zigno, A. de. Flora fossilis Formationis Oolithice. Le Piante fossili dell’ Oolite. Puntatai. 1856. * * - o vie [ es ° Ne * > wy? 4 . + - > ae | ’ 4 ¥ “ea Py 4 a 1 \ j Pate ; ; i . . a , : . ‘ " rth t rs A z 4] v , : du i 7 J ' - < é x t oh ; by & 4 * ‘ * . . . ‘ . ‘ * , = ws “it Ag ; p. A ae es oe Fe ; 12%) % ef 4 ; Laity 7 Cs) P ¢ 7 vd 517 P f « 7 j {7 , } : t ~ ”, « fy ; “PAE , a ‘ f aii ral is { het “ee “oP ercpar i ; gle ‘ tee £1 Fe; VR. VER) Opa ae a eo Tae id : : “ : ee ee +t [ i 1% PROF] Bey lone! eg ee bel eb yeahs Sete Cpe oe ae 4 7) - y ol a oy it ‘ H oe A } = ees Yue Oe é * 4 & eAhipia ne) eat PaaS f Pero ee igah x *D asetmatia? f ‘Sie - ALPHABETICAL INDEX TO THE PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | The fossils referred to are described, and those of which the names are printed in italics are also figured. | ABERDEENSHIRE, pleistocene deposits of, 509. Abernethy, Mr. Macnab, on superficial deposits, 532. Acropagia corbis ?, 142. Ammonia from volcanos, C. Daubeny, on the evolution of, 295. Ammonites brevispina, 28. — Daveei, 29. —— fimbriatus, 139. Jamesoni, 27. — Jurensis ?, 138. — Raquinianus?, 138. — Uralensis?, 138. Andalusia, Prof. D. T. Ansted, on the geology of the southern part of, 130. Anniversary Address of the President, Major-General Portlock, xxiv.—clxiii. See also Portlock, Major-General. Annual Report, i. Ansted, D. T., on the geology of the southern part of Andalusia between Gibraltar and Almeria, 130 ; noticed, CXXXIX. Apiocrinites incrassatus, 135. Artificial crystals, structure of, 454. Ascoceras Barrandit, 180. Ascoceras, Mr. Salter, on the occur- rence of, in Britain, 177. Astarte complanata, 138. pulchella, 146. quadrata, 146. Atlas and Axis of Plesiosaurus, 288. Australia, gold-fields of Victoria, 533, 538, 540, 543. ——, Prof. Owen on the skull of Zy- ie trilobus of Macleay, from, = the extinct voleanos of Victoria, ra he Bactrites, Sandberger, 180. Baily, W. H., descriptions of fossil invertebrata from the Crimea, 133 ; noticed, exli. Baltic provinces, geology of the, 36; Silurian rocks of the, 48. Ballaarat, Mr. Selwyn, on the gold-field of, 534. , Mr. Rosales, on the gold-diggings at, 543. , Mr. Redaway, on the gold-dig- gings at, 540. , Mr. Phillips, on the gold-field of, 588. Basalts of Victoria, 232. Basement bed of the Oolite, 101. Bath, section of the Oolites near, 87. Beckles, 8. H., bones of the hind-foot of the Iguanodon, discovered by, 174. Belemnites breviformis, 27. elongatus, 27. paxillosus, 27. Bigsby, J. J., on the paleozoic rocks and fossils of the state of New York ; Part I., 241, 335; Part IT., 305, 497: ; noticed, cl. Birdseye limestone, J42. Black River limestone, 341. Bone-cave near Melbourne, 536. Bones of the foot of Iguanodon, 174. Boring through the chalk at Harwich, 249. Bornemann, on the production of am- monia, noticed, cix. Boulder-clays, upper and lower, of the Gorlston Cliffs in Norfolk, 171. Boulder of granite found in the white chalk near Croydon, Mr. R. Godwin- Austen on a, 252. Bradford Clay in Gloucestershire, 116. INDEX TO THE PROCEEDINGS. Bransby, section at, 94. Brodie, P. B., note on the occurrence of a new species of fish in the Upper Keuper Sandstone in Warwickshire, 165 ; noticed, Ixxxvi. Buccinum angustatum, 151. —— corbianum, 152. —— Daveluinum, 151. dissitum, 152. — Doutchine, 151. moniliforme, 151. obesum, 151. Buckman, J., on the Oolite rocks of Gloucestershire and North Wilts, 98; noticed, cxxxviii. Bulimus Sharmani, 148. Bunbury, C. J. F., on a remarkable specimen of Neuropteris, with re- marks on the genus, 243; noticed, xclil. Bunter Sandstein of the Odenwald, 222. Calamophyllia Stokesii?, 135. Calciferous sandstone, 339, 430. Cape Media, section of, 206. Caudagalli grit, 374, 437. Cardinia concinna, 30. Cardium equistriatum, 137, 138. amplum, 144. carinatum, 144. — conniacum ?, 141. corbuloides, 145. erassatellatum, 145. Demidoffi, 144. —— Edouardi, 145. Fittoni, 144. — macrodon, 14. ovatum, 145. —— paucicostatum, 145. protractum, 144. pseudocardium ?, 145. squamulosum, 144. — subedentulum, 145. Verneuilii, 145. Catskill limestone, 370; rocks, 392, 438. Caithness, remains of terrestrial plants in the Old Red Sandstone of, 72; the plant-bearing Devonian beds of, 76. Cavities in crystals, 454. Cephalaspis Lyelli, 270. Cephalaspis and Pteraspis, Prof. Hux- ley, on, 267. Cerithium Cattleye, 150. cochleare, 150. —— giganteum, 143. truncatum, 150. Chalk, boring through the, at, Harwich, 249; near Croydon, boulder of granite found in the, 252; fossils of the, 259; Mr. R. Godwin-Austen, on the extraneous rocks from the, 252. Changes of level in South Wales, 532. Charing, fossils found in the iron- sandstones on the North Downs at Lenham and, 382, 334. Chazy limestone, 341. Chemung rocks, 388, 438. Chili, Dr. C. Forbes on the coal found to the south of Concepcion in, 294. Cidaris Blumenbachii, 135. glandifera, 135. Cirencester, Oolitic fossils from, 117. Cleavage, observations on, cxxXx. Cleveland, iron-ore of, 96. Clinton rocks, 353, 432. Coal-beds of Southern Chili, 294; of Yorkshire, 89. Coast of Sicily, elevation of, 504. Coast-sections near Scarborough, 86. Cockburn, C. F., note on the geology of the neighbourhood of Sebastopol, and the Southern Coast of the Crimea, by, 161. Comoseris irradians, 134. Committee, Report of the Library and Museum, ili. Coniferous wood, fossil from Caithness, Conoclypus conoideus, 143. Coralline limestone of Schoharie, 362, 432. Coral-rag of Gloucestershire, 125. Cornbrash of Gloucestershire, 119; of Yorkshire, 92. Corniferous limestone, 376. Cotteswolds, oolite of the, 101. Crabs thrown up in Payta Bay, 294. Crania spinulosa, 140. Cranium of Plesiosaurus, 292. Craters in Victoria, 227. Creswick Creek, Victoria, Mr. Redaway, on the gold-diggings at, 540. Cretaceous fossils found in the Crimea, 139, 155. Cretaceous sea, conditions of the, 259. Crickley Hill, section at, 106. Crimea, descriptions of fossil inverte- brata from the, 133; cretaceous fossils found in the, 155 ; the geology of Sevastopol and the Southern Coast of the, 161; jurassic fossils found in the, 153; tertiary fossils found in the, 158; summary of fossil in- vertebrata from the, 161. Croydon, boulder of granite found in the white chalk near, 252. Crystals, Mr. Sorby, on some pecu- _ larities in the microscopical strue- ture of, 242, 453. Cyclostoma reticulatum, 148. Cyprina Georget, 145. — naviculata, 146. INDEX TO THE PROCEEDINGS. Cyprina Pallasii, 145. ? triangulata, 146. Cyrena Media, 239. Dardanelles, geology of the, 215. Daubeny, C. G. B., on the evolution of ammonia from volcanos, 295; no- ticed, evi. Delesse, on metamorphism, noticed, exvill. Delthyris limestone, 370. Deville, Ch. St. Claire, on the gaseous products of volcanic vents, noticed, cx. Devonian beds of Caithness, with plant-remains 76; rocks of New York, 372, 437 ; plant-remains, 72. Dobrutcha, Capt. Spratt, on the geology of the north-east part of the, 204. Dogger of Yorkshire, 93. Donations to the Library, 79, 181, 307, 544. Donations to the Museum, viii. Dreissena inzequivalvis, 143. (Mytilus) rostriformis, 143. Durocher, J., on the chemical constitu- tion of igneous rocks; noticed, cxiil. Egerton, Sir P., Palichthyologic Notes, No. 10., on Paleeoniscus superstes, 164; noticed, Ixxxvi. Elephant, fossil species of, in England, 81. Elevation of the coast of Sicily, 504. Eston Nab, iron-ore of, 96. Esthonia, Silurian rocks of, 45. Estuary Sands in the upper part of Shotover Hill, 256. Exogyra columba, 141. haliotoidea, 141. Extraneous materials in the chalk, 254. Evolution of ammonia from volcanos, 295. Falconer, H., on the species of mastodon and elephant occurring in the fossil state in England, Part IJ. Elephas, 81; noticed, lxxxix. Femur of a large Iguanodon, 174. Fish, fossil, from the Keuper, 164. Floating ice in the Cretaceous Sea, 264. Fluid-cavities in crystals, 454. Forbes, C., on a quantity of crabs thrown up on the beach in Payta Bay, 294; on the coal found to the south of Concepcion, in southern Chili, 294. Forest-marble of Gloucestershire, 118. Fossil elephants, 81; fish from the Keuper, 164; from the Permian of Ireland, 165; invertebrata from the Crimea, 133, 161 ; Mammal from the London Clay, 54; plants from Caithness, 72. Fossiliferous ironsands in Kent, 333. Fossils, from Lenham, Kent, 329, 334; Shotover Hill, 239; of the white chalk, nature of the, 259; pleistocene, from Aberdeenshire, 521, 531. France, Lias of, 25. oe tertiaries of the Levant, 212. Frocester Hill, fossils from, 104; sec- tion at, 103. Fullers-earth Oolite, 100. Geikie, A., on the geology of Strath, Isle of Skye, |; noticed, cxxxvi. Gemmellaro, G., on the gradual eleva- tion of the coast of Sicily, from the ae of the Simeto to the Onobola, 504. Genesee slate, 385, 438. Geology of the gold-fields of Victory, 533; the north-east part of the Do- brutcha, 204; Strath, Isle of Skye, 1; the southern part of Andalusia, 130. Geological Survey of Victoria, list of palzozoic fossils collected by the, 537. Germany, Lias of, 25. Gervillia Maccullochii, 32. Gibson, T. F., notice of the discovery ofa large femur of the Iguanodon in the Weald clay at Sandown Bay, Isle of Wight, 175. Glaciers, observations on, cxxxi. Glacier-moraines of Ross-shire, 1'70. Glastonbury, a new Plesiosaurus from Street near, 281. Gloucestershire, Lias beds of, 24, 25; and North Wilts, Prof. Buckman on the Oolitic rocks of, 98. Godwin-Austen, R., on a boulder of granite found in the “white chalk,”’ near Croydon; and on the extrane- ous rocks from that formation, 252 ; noticed, cxxxiii. Gold-diggings at Ballaarat, Victoria, Mr. H. Rosales on the, 543; at Cres- wick Creek and Ballaarat, Victoria, Mr. W. Redaway, on the, 540. Gold-field of Ballaarat, Mr. J. Phillips, on the, 538 ; of Victoria, Mr. A. R. C. Selwyn, on the geology of the, 533. Gonioceras anceps, 180. Gorlston Cliffs in Norfolk, Mr. J. Trim- mer, on the boulder-clays of the, 171. Granite, boulder of, in the white chalk near Croydon, 252. Granites of the north-east of Ireland, the Rev. 8. Haughton, on the, 300. Granitic rocks, Mr. Sorby on, 484. Gravels at Taunton in Somersetshire, 164. Great Oolite of Gloucestershire, 111. INDEX TO THE PROCEEDINGS. Greenstone, fragments of, in the chalk, 56. Gristhorp section, 88. Gryphea cymbium, 33. dilatata, 137. incurva, 138. obliquata, 33. Hall, James, award of a Wollaston Medal and the residue of the Wol- laston Fund, to, xxii. Hambledon Hills; section of, 91. Hamilton rocks, 380, 488. Harris, W., section in Down Wood, Charing, by, 332. Harwich, Mr. Prestwich, on the boring through the chalk at, 249; Pliolo- phus vulpiceps, from the London clay, near, 54. Haughton, 8., on the granites of the north-east of Ireland (Part IT), 300; noticed, cxlv. Heidelberg, section near, 220. Helix Bestii, 148. Duboisit, 147. Hennessy, H., on the physical structure of the earth, noticed, cxvi. Herbert, E., on the mammiferous fauna of the lower tertiaries of France, noticed, Ixxxili. Hudson River rocks, 546. Hull, E., on the triassic and permian rocks of the Odenwald in the vicinity of Heidelberg, and the corresponding formations in Central England, 219 ; noticed, exliii. Huxley, T. H., on a new species of Plesiosaurus from Street, near Gla- stonbury, 281; noticed, xcii.; on Cephalspis and Pteraspis, 267 ; no- ticed, lxxxv. Tce in the Cretaceous Sea, 264. Igneous fusion, minerals formed by cooling from a state of, 476. Teuanodon, a large femur of the, from the Weald clay at Sandown Bay, Isle of Wight, 175; note by Prof. Owen on the bones of the hind-foot of the, 171. Inferior Oolite of the Cotteswolds, 101. Tnoceramus ventricosus, 31. Invertebrata from the Crimea, fossil, 138, 161. Treland, the granites of the north-east of, 300. Tron-sands of Shotover Hill, 238. Tron-sandstones, note by Mr. S8.Wood on the fossils found at Lenham and Charing on the North Downs, in the, 333; on the North Downs, Mr. J. Prestwich on the age of some, 322. Tronstones of Yorkshire, Prof. Phillips on the, 84. Isastreea polygonalis, 134. explanata?, 134. —— Greenoughii, 134. Murchisoni, 34. Isle of Wight, a large femur of the Iguanodon from the Weald Clay at Sandown Bay, 175. Jamieson, T. F., on fossil shells and striated boulders at high levels in Scotland, 509; on the pleistocene deposits of Aberdeenshire, 509. Jurassic fossils from the Crimea, 134, 153. Kelloway rock of Gloucestershire, 124. Keuper sandstone, fossil fish from the, ree of the Odenwald and England, 224. Kimmeridge Clay of Gloucestershire, 127; of Shotover Hill, 238. Kjerulf, T., on the Silurian basin of Christiania, Norway, 36. Kustenjeh, sections at, 206, 208. Ladegaards-6, Norway, section of, 38. Land of the cretaceous period, 265. Lophiodont mammal from the London clay, 54. Leckhampton Hill, section at, 108. Lenham, fossils found in the iron- sandstones on the North Downs, at Charing and, 334. Lepidodendron nothum in the old red sandstone of Caithness, 75. Levant, Capt. Spratt on the freshwater deposits of the, 212. Lias-beds in France, Germany, Glou- cestershire, and Skye, correlation of the, 25; boulders of Loch Greinord, 169; fossils from the Isles of Pabba, Scalpa, and Skye, 94; fossils of Gloucestershire, 24; and Oolites of Yorkshire, 84; Plesiosaur, from, 281. Library Committee, report of the, iii. Lima gigantea, 31. Hermanni, 31. acuticosta, 31. Lincolnshire, Oolites of, 95. Littorina monastica, 150. Livonia, Silurian rocks of, 43. Loch Greinord, Prof. Nicol on the newer red sandstone, and some other geological phenonomena near, 167. London Clay, fossil mammal from the, 54. Lyell, Sir Charles, reply on receiving for M. Hermann von Meyer the Wollaston Medal, xxii. Lycopodites Milleri, in the old red sand- stone of Caithness, 75. Macnab, K., on superficial deposits in Abernethy, 532. Malaga, geology of, 130. INDEX TO THE PROCEEDINGS. Malmo, Norway, section of, 38. Mammal, fossil, from the London Clay of, 54. Map of the volcanos of Victoria, 228. Marble-quarries of Marmora, 218. Marcellus shale, 378, 438. Marmora, section in the Island of, 213. Mason, R., on changes of level in South Wales, 532. Mastodon and elephant, species of, oc- curring in the fossil state in England, © 81. Medina sandstone, 352, 432. Melbourne, bone cave near, 536. Metamorphic rocks, Mr. Sorby on, 475. Meyer, H. von, award of a Wollaston Medal to, xxii. Microscopical structure of crystals, Mr. H. C. Sorby, on some peculiarities in the, 242, 453. Middle or newer tertiary fossils found in the Crimea, 158. Miller, J., on the plant-bearing Devo- nian beds of Caithness, 76; noticed, xcill. Minerals and rocks, Mr. Sorby on the origin of, 453. Minerals ejected from Vesuvius, 480. Montlivaltia trochoides, 135. Muschelkalk of the Odenwald, 224. Murchison, Sir R. I., and F. Schmidt, on the Silurian rocks of Esthonia, Northern Livonia, and the Isle of Oesel, 43; noticed, cxlvi. Murchison, Sir R. I., reply on receiving the Wollaston Medal for Mr. James Hall, xxii.; on the Silurian rocks and fossils of Norway and of the Baltic Provinces of Russia, compared with their British equivalents, 36; noticed, exlvi.; on the succession of rocks in the Northern Highlands from the oldest gneiss, through strata of Cam- brian and Lower Silurian age, to the Old Red Sandstone, inclusive, 531; noticed, exlviii. Museum Committee, report of the, iii. Mytilus apertus, 143. cuneatus, 30. Mytilene, section of, 213. Nailsworth, fossils from, 104. Natica prelonga, 139. Natural crystals, structure of, 468. Nautiloceras paradoxicum, 180. Nautilus pseudo-elegans, 139. Nerinza grandis ?, 138. Neuropteris flexuosa, 248. gigantea, 247. Loshii, 249. ——, Mr. C. Bunbury on the genus, 248. —— rotundifolia, 248. Neuropteris rarinervis, 248. Neuropteris, young frond of, 243. Newer red sandstone of Loch Greinord, 167. New Red Sandstone, fossil fish from, 164. New York, Dr. J. J. Bigsby on the palzozoic basin of the State of, Part I., 241,335; Part IT., 305, 427. Niagara rocks, 359, 482. Nicol, J., on the newer red sandstone, and on some other geological phe- nomena, near Loch Greinord in Ross- shire, 167 ; noticed, exliii. Nodot, L., on the organization of the Edentata, noticed, xciv. Norway, Sir R. I. Murchison and M. Th. Kjerulf, on the Silurian rocks and fossils of, 36. Norfolk, boulder-clays of, 171. North America, palozoic rocks and fossils of, 241, 335, 427. North Downs, Mr. Prestwich on the age of some sands and iron-sandstones on the, 322. North Wilts, the Oolite rocks of Glon- cestershire and, 98. Northern Highlands, Sir R. I. Murchi- son on the succession of rocks in the, to the Old Red Sandstone inclusive, 501. Nototherium, skull of, 541. Nummulites distans, 142. Raymondi, 142. Nunda rocks, 386. Odenwald and Central England, Tri- assic and Permian rocks of the, 219. Oesel, Silurian rocks of the Isle of, 43. Older tertiary fossils found in the Cri- mea, 158. Oldham, Neuropteris from, 243. Old Red Sandstone, fossil plants from the, 72. Oneida conglomerate, 350, 432. Onobola, the gradual elevation of the coast of Sicily from the mouth of the Simeto to the, 504. Onondaga limestone, 375; salt rocks, 364, 433. Oolite rocks of Gloucestershire and North Wilts, Prof. James Buckman, on the, 98. -QOolites and ironstones of Yorkshire and North Wilts, Prof. James Buck- man on the, 98. Origin of minerals and rocks, Mr.Sorby on the, 453. Oriskany sandstone, 372, 437. Orm6, Norway, section of, 38. Orthoceras bisiphonatum, 177. Ostrea arietis, 34. INDEX TO THE PROCEEDINGS. Ostrea carinata, 140. curvirostris, 141. —— flabellata, 140. frons, 140. —— gigantea, 143. hippopodium, 141. laciniata, 141. vesicularis, 140. Owen, R., on Anoplotheroid qua- drupeds ; noticed, lxxix. ; description of a small lophiodont mammal (Pholophus vulpiceps) from the London Clay, near Harwich, 54; on some outline-drawings and pho- tographs of the skull of Zygomaturus trilobus of Macleay, from Australia, 541 ; note on the bones of the hind- foot of the Iguanodon, discovered and exhibited by 8. H. Beckles, F.G.S., 174; noticed, lxxxii. Oxford Clay of Gloucestershire, 124. Pabba, Lias fossils from, 24. Paleozoic basin of the State of New York, Dr. J. J. Bigsby on the, Part I., 241, 3385; Part I1., 427; fossils of Victoria, 537 ; rocks and fossils of the State of New York, 241, 305, 427. Paleoniscus catopterus, 165. superstes, 164. Palichthyologic Notes, No. 10, by Sir P. Egerton, 164. Paludina achatinoides, 150. elongata, 239. ? subangulata, 239. supextensis?, 239. ? sp., 240. Parker, W. K., and T. R. Jones, on some Pleistocene foraminifera from Aberdeenshire, 521. Payta Bay, crabs thrown up in, 294. Pecten sequivalvis, 31. Pentacrinites basaltiformis, 13. Pentacrinus gracilis, 34. robustus, 34. Permian and Triassic rocks of the Old- enwald and of Central England, 219. Pentamerus limestone of Europe, 50; lower, 369; upper, 371. Phillips, J., on some comparative sec- tions in the Oolitic and iron-stone series of Yorkshire, 84; on the es- tuary sands in the upper part of Shotover Hill, 236; noticed, exxxv. Phillips, J., on the gold-field of Bal- laarat, Victoria, 538. Pholadomya ambigua, 29. Pholas Hommarei, 147. Photographs of the skull of Zygoma- turus (Nototherium), 541. Pictel and Humbert on Swiss palzon- tology ; noticed, xevii. Pinna folium, 30. Polystomella crispa, 143, 521. Portage rocks, 386, 438. Portland Oolite of Gloucestershire, 128; sands of Shotover Hill, 238. Portlock, Major-General (President), address on presenting the Wollaston Medal to Hermann von Meyer, xxi.; and to Mr. James Halli, with the residue of the Wollaston Fund, xxii. ; Anniversary address, February 19, 1858, xxiv.. Notices of deceased Fel- lows: Dean Conybeare, xxiv.; Mr. Joshua Trimmer, xxxii.; John Forbes Royle, M.D., xxxvii, ; Mr. Laverack, xli.; Mr. G. H. Saunders, xli.; Mr. Floresi, xlii.; Mr. William Bald, xlii.; Mr. Henry James Brooke, xliv.; Francis, Earl of Ellesmere, xlv.; Rear-Admiral Sir Francis Beau- fort, xlvii. ; Thomas Best Jervis, liv. ; George Weare Brackenridge, lx. ; William Wentworth Fitzwilliam, lxii.; M. André Hubert Dumont, Ixii.; M. P. A. Dufrenoy, Ixxi. ; M. Alcide D’Orbigny, lxxi. Re- view of geological progress, lxxix. ; Professor Owen on Anoplotheroid quadrupeds, lxxix.; on a Lophidont mammal, Ixxx.; on the bones of an Iguanodon, lxxxii., lxxxiii.; M. Ed. Hébert on the mammiferous fauna of the Lower Tertiaries of France, Ixxxiii.; Sir Philip Egerton on fish- remains from the neighbourhood of Ludlow, lxxxiv.; Professor Huxley on the affinities of Cephalaspis and Pteraspis, lxxxv. ; Sir Roderick Mur- chison on the relative position of the Ludlow strata, Ixxxv.; Sir Philip Egerton and the Rev. P. B. Brodie on a new species of Palzoniscus in the Upper Keuper Sandstone, at Rowington, near Warwick, lxxxvi.; Dr. Falconer’s description of mam- malian remains discovered at Dur- dlestone Bay, Purbeck, by Mr. W. R. Brodie and Mr. H. Beckles, lxxxyii. ; Dr. Falconer on the species of mas- todon and elephant found fossil in Britain, lxxxix.; Mr. W. Bollaert on the occurrence of bones of mastodon in Chili, xc. ; description of the crus- tacean, Tropifer levis, by Mr. C. Gould, and of the Pygocephalus Coo- peri, by Professor Huxley, xci.; de- scription by Professor Huxley of a new species of Plesiosaurus, xcii. ; Mr. Salter on some terrestrial plants from the Old Red Sandstone of Caith- ness, and Mr. John Miller on the INDEX TO THE PROCEEDINGS. Devonian beds of Caithness, xciii. ; Mr. C. J. F. Bunbury on the genus Neuropteris, xciii.; M. L. Nodot on the organization of the Edentata, xciv.; MM. Pictet and Humbert on new species of fossil Chelonia found in the Department of Jura, xcvii.; on Swiss paleontology, by M. Pictet, xevill.; the Palsontographica, by Dunker and Von Meyer, cii.; M. de Koninek on the distribution of some of the Carboniferous fossils, cv. ; Phy- sical Geology: Dr. Daubeny on the evolution of ammonia from volcanos, evi.; Mr. Robert Warington on bo- racic acid and ammonia, cvil.; M. Bornemann on the production of ammonia, cix.; M.Ch. Sainte Claire Deville on the gaseous products of volcanic vents, ex.; M. J. Durocher on the chemical constitution of ig- neous rocks, exiii.; Mr. H. Hennessy on the physical structure of the earth, exvi.; M. Delesse on metamorphism, exviii.; Mr. Sorby on microscopic examinations of the internal struc- ture of rocks, exxvi.; observations on cleavage, cxxx. ; on glaciers, Xxxi. ; and on descriptive geology, cxxxii. ; Mr. Godwin-Austen on a boulder in the chalk at Croydon, cxxxiii.: Mr. Prestwich on the boring through the chalk at Harwich, exxxiv.; Professor J. Phillips on the estuary sands of Shotover Hill, exxxv.; Mr. A. Geikie on the geology of Strath, Isle of Skye, exxxvi.; Dr. Wright on the lias-beds in France, Germany, Glou- cestershire, and Skye, exxxvui.; Pro- fessor Buckman on the Oolitic rocks of Gloucestershire and North Wilts, exxxviil.; Professor D. T. Ansted on the geology of the southern part of Andalusia, cxxxix.; Capt. T. Spratt on the geology of the Dobrutcha, and on the freshwater tertiaries of the Levant, cxl.; Mr. W. H. Baily’s de- scription of some fossils from the Crimea, exli.; the Permian forma- tion, cxlii.; Mr. E. Hull on the Odenwald, exliii.; Professor Nicol on the Red Sandstone of Loch Grei- nord, exliii.; Mr. R. Brough Smyth on the extinct volcanos of Victoria, Australia, exliv. ; the Rev. S. Haugh- ton on the chemical constitution of the granites of Ireland, exlv.; Mr. Pring’s section of the gravel-beds at Taunton, exlvi.; Mr. Joshua Trim- mer on the distribution of superficial detritus, exlvi.; Sir R. Murchison’s comparison of the Silurian rocks and fossils of Norway, as described by M. Th. Kjerulf, with those of the Baltic provinces of Russia, as de- scribed by Prof. Schmidt, and both with their British equivalents, exlvi.; and his Paper on the succession of rocks in the northern Highlands, exlvii.; Dr. J. J. Bigsby on the paleeozoic rocks and fossils of the State of New York, and his geologi- cal map of North America, cl.; on some recent observations of M. A. Fayre on the coal-beds of Taninge, Savoy, cli.; on Sir W. Logan’s Re- port on the geological survey of Canada, clii.; progress of geology in the United States and India, clv.; report on the prize for physical sci- ences for 1856, by MM. Elie de Beaumont, Fleurens, Is. Geoffrey, Sainte Hilaire, Milne-Edwards, and Ad. Brongniart, clvi.; thoughts on creation, elvili.; and notice of Mr. Gosse’s work, entitled ‘Omphalos, or an attempt to untie the Geological Knot,’ clix.; observations on the questions as to the degree of anti- quity of man, and whether man was created of one species, or in nume- rous species, clx. ; conclusion, clxiii. Potamomya Iphigenia, 147. Potash-granites of Ireland, 300. Potsdam sandstone, 338, 434. Prestwich, J., on the age of some sands and iron-sandstones on the North Downs, 322; on the boring through the chalk at Harwich, 249; noticed, CXXXIV. Pring, J. D., on the gravels at Taun- ton in Somersetshire, 164; noticed, exlvi. Planorbis cornucopia, 148. obesus, 148. Plant-bearing Devonian beds of Caith- ness, 76. Plants, fossil, from Caithness, 72. Pleistocene deposits of Aberdeenshire, Mr. T. F. Jamieson on the, 509. Plesiosaurus Etheridgii from Street, near Glastonbury, Prof. Huxley on the, 281. Pleta limestone, 45. Pleuromya Scotica, 29. unioides, 30. Pleurotoma Chersonesus, 151. laqueata, 151. Plicatula spinosa, 32. Pliolophus vulpiceps from the London Clay, near Harwich, 54. Pteraspis Banksii, 274. INDEX TO THE PROCEEDINGS. Quartz-veins, Mr. Sorby on the struc- ture of, 471. Redaway, W., on the gold-diggings at Creswick Creek and Ballaarat, Vic- toria, 540. Report, Annual, i. ; of the Library and Museum: Committee, iii. Review of geological progress, lxxix. Rhynchonella acuta, 137. Cooke, 136. pectinata, 137. senticosa, 137. variabilis, 137. Rosales, H., on the gold-diggings at Ballaarat, Victoria, 543. Rosshire, glacier-moraines of, 170; red sandstone of, 167. Roth-todt-liegendes of the Odenwald, 221. Rowington, Warwickshire, fossil fish from, 164. Russia, the Silurian rocks of the Baltic provinces of, 43. Salter, J. W., on a new genus of Cepha- lopoda, Tretoceras (Orthoceras bisi- phonatum, Sowerby); and on the occurrence of the genus Ascoceras, Barrande, in Britain, 177 ; on some remains of terrestrial plants in the Old Red Sandstone of Caithness, 72; noticed, xciil. Sandown Bay, femur of Iguanodon from, 175. Sealpa, Lias fossils from, 24. Scandinavia, Silurian rocks of, 36. Scarborough, sections near, 85. Schmidt, F., results of an examination of the Silurian rocks of Hsthonia, Northern Livonia, and the Isle of Oesel, by, 43. Schoharie grit, 374, 437; limestone, 362, 432. Scotland, pleistocene deposits of, 503 ; succession of rocks in North, 501. Scyphia Cockburnit, 134. Portlockii, 148. Secondary fossils from the Crimea, . 134. Section across the Dardanelles, 217 ; _ along the coast of Aberdeenshire, 510; at Ballaarat, 535; at Bendigo, 534; at Frocester Hill, 113; at Har- rietsham, 326; at Keilor, Victoria, 229; at Lenham, Kent, 325; at Steiglitz, 535 ; at Swindon, 128; in the Island of Marmora, 213; of a boring at Harwich, 250; Cape Me- dia, 206; of Ladegaards-6, 38; of _Mytilene, 215; of newer tertiary strata at the cliff west of the Mona- stery of St. George, in the Crimea, 162; of Ormo and Malmé, 38; of the Kippet Hills, 522. Sections at Cirencester, 114, 117, 119; at Kustenjeh, 206, 209 ; comparative, of the Oolite and Lias, 84; near Scarborough, 86; of Shotover Hill, 239; of the Lias in Skye, 6; of the Silurian rocks in Norway, 38 ; of the Yorkshire Oolites, 84. Selwyn, Alfred R. C., on the geology of the gold-fields of Victoria, 535 ; on the Tower Hill crater, Victoria, 23. Sevastopol, the geology of, 161. Shotover Hill, Prof. J. Phillips on the see sands in the upper part of, 236. Sicily, G. G. Gemmellaro on the gra- dual elevation of the coast of, 504. Silurian basin of Christiania, Norway, 36; of New York, 241, 305, 335, 427; fossils of Victoria, 537; rocks of Esthonia, Northern Livonia, and the Isle of Oesel, 43; of New York, 335, 427 ; of Norway, 36; of Russia, 43; of the Baltic Provinces, 36. Simeto to the Onobola, elevation of the coast of Sicily, from the mouth of the, 504. Skye, Lias beds in, 5; Lias fossils from, 24; the geology of Strath, Isle of, 1, Smyth, R. B., on the extinct volcanos of Victoria, Australia, 227 ; noticed, exliv. Soda-elvans of Ireland, 304. Soda-granites of Ireland, 302. Somersetshire, gravels at Taunton in, 164. Sorby, H, C., on some peculiarities in the microscopical structure of cry- stals, 242, 453 ; on the microscopical structure of crystals, indicating the origin of minerals and rocks, 453 ; noticed, cxxvi. South Wales, Mr. Mason on changes of level in, 532. Spain, geology of a part of, 130. Special General Meeting, 241. Spratt, T., on the freshwater deposits of the Levant, 212; on the geology of the north-east part of the Dobrut- cha, 204: noticed, exl. Stonesfield slate, 111. Strath, Skye, Mr. A. Geikie on the geology of, 1; Liassic beds of, 1; Lias fossils from, 24; Valley, geolo- gical structure of the, 6. Stratigraphical Table of the paleeozoic rocks of New York, 429. Street, near Glastonbury, a new species of Plesiosaurus from, 281. INDEX TO THE PROCEEDINGS. ee of crystals, Mr. Sorby on the, Summary of fossil invertebrata from the Crimea, 161. Superficial deposits in Abernethy, 532. Swindon, Oolites of, 128. Synoptical view of the palzeozoic basin of New York, 335. Table of Chemung fossils, 426; creta- ceous fossils found in the Crimea, 153 ; Hamilton fossils, 426; Ju- rassic fossils found in the Crimea, 153; middle or lower tertiary fos- sils found in the Crimea, 158 ; older tertiary fossils found in the Crimea, 158; fossils of the corniferous lime- stone, 425; the palzozoic rocks of New York, 337; Trenton fossils, 421; Triassic and Permian rocks, 995 : showing the correlation of the Lias-beds in France, Germany, Glou- cestershire, and Skye, 25. Tables of Devonian fossils of New York, 420, 424; Silurian fossils of New York, 399, 420, 422, 423, 451. Taunton in Somersetshire, J. D. Pring, on the gravels at, 164. Teleosaurus, cranium of, 292. Tenedos, section of, 213. Terebratula Jamesit, 136. numismalis, 136. 137. —_— perovalis? 136. radiata, 136. rotundata, 136. —— Strogonofii? 136. subovoides? 136. Terrestrial plants from Old Red series, 72. Tertiary beds in Victoria, 233 ; fossil mammals, 67 ; fossils from the Cri- mea, 142, 158. Thamnastrea arachnoides, 134. Thecosmilia annularis? 134. Tornatella inflexa, 147. minuta, 147. Tower-Hill crater, Victoria, 231. Trenton limestone, 343. Tretoceras, a new genus of Cephalo- poda, Mr. J. W. Salter on, 177. Tretoceras bisiphonatum, 179. Triassic and Permian rocks of the Odenwald and of Central England, Mr. BE. Hull on the, 219. Trimmer on the upper and lower boulder-clays of the Gorlston Cliffs in Norfolk, 171; noticed, exlvi. Troad, volcanic rocks of the, 214. Trochus Andersoni, 149. Trochus Beaumontii, 149. Blainvillei, 149. Corderianus, 149. __— Fenonianus, 149. —— Hommarei, 149. ——— imbricatus, 29. — Lygonii, 150. —— Murchison, 149. Pageanus, 149. —— pulchellus, 149. Sutherlandi, 150. Tully limestone, 383, 438. Unicardium cardioides, 30. Unio Stricklandii, 239. subtruncatus? 239. Upper Keuper Sandstone in Warwick- shire, the Rev. P. Brodie on the occurrence of a new species of fish in the, 165. Utica slate, 345. Venus minima, 146. semiplana, 146. Victoria, Australia, Mr. A. R. C. Sel- wyn on the gold-fields of, 533; Mr. J. Phillips on the gold-field of Bal- laarat, 538; Mr. R. B. Smyth, on the extinct voleanos of, 227. Volcanos, evolution of ammonia from, oe extinct, of Victoria, Australia, Water contained in crystals, 469. Warrington, R., on boracic acid and ammonia found in volcanos; no- ticed, cviil. Warwickshire, fossil fish from, 164. Waterlime rocks, 367. Weald Clay, large femur of Tguanodon from the, 175. Whitby, iron-beds near, 96. White Chalk, nature of the, 259. Wilts, Oolites of North, 98. Wood, coniferous, in the Old Red Sandstone of Caithness, 73. Wood, 8. V., Note on the fossils found at Lenham and Charing, in the iron- sandstones on the North Downs, 339. Woodward, S. P., on some pleistocene shells from Aberdeenshire, 582. Wright, T., notes on the fossils col- lected by Mr. Geikie from the Lias of the Isles of Pabba, Scalpa, and Skye, 24; noticed, exxxvil. Yorkshire, Prof. Phillips on the Oolites and iron-stones of, 84. Zygomaturus trilobus, of Macleay, from Australia, Prof. Owen on the, 541 saat a TRdoRe oon rage Ont sini levi ott Me fsa} a RQ Ge rh sie at lt Mae rite g 1/18) Gmaie A ; ’ . : SF ‘ A aes ‘i Vin? me ‘dee $5 A et cA Aken he Taso i; per Bath de das coh . ihe si TARE . Hire? 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