There are in the Kidston Collection of Fossil Plant Slides sections of four specimens of Lepidodendroid stems, from different Scottish localities in the Carboniferous Limestone Series, which were grouped together by the late Dr Kidston as “Lepidodendron Langi n.sp.” The specimens may be referred to as Nos. 1—4, and the various localities and the numbers of the slides by which the specimens are represented in the Kidston Collection are enumerated here for convenience of reference.

The Middle Jurassic is a poorly sampled time interval for non-pelagic neosuchian crocodyliforms, which obscures our understanding of the origin and early evolution of major clades. Here we report a lower jaw from the Middle Jurassic (Bathonian) Duntulm Formation of the Isle of Skye, Scotland, UK, which consists of an isolated and incomplete left dentary and part of the splenial. Morphologically, the Skye specimen closely resembles the Cretaceous neosuchians Pachycheilosuchus and Pietraroiasuchus, in having a proportionally short mandibular symphysis, shallow dentary alveoli and inferred weakly heterodont dentition. It differs from other crocodyliforms in that the Meckelian canal is dorsoventrally expanded posterior to the mandibular symphysis and drastically constricted at the 7th alveolus. The new specimen, together with the presence of Theriosuchus sp. from the Valtos Formation and indeterminate neosuchians from the Kilmaluag Formation, indicates the presence of a previously unrecognised, diverse crocodyliform fauna in the Middle Jurassic of Skye, and Europe more generally. Small-bodied neosuchians were present, and ecologically and taxonomically diverse, in nearshore environments in the Middle Jurassic of the UK.

It has been long known that in various parts of Africa, the natives are in the habit of subjecting to the ordeal of poison parties who are suspected of crimes. On the east coast, we meet with Tanghinia venenata, yielding the Tanghin poison-nut of Madagascar; and on the west coast, seeds and barks of different kinds have been employed as ordeals,—the sources of which, however, have not been hitherto fully ascertained.

Dr Kirk, naturalist to the Livingstone Expedition, states, that the Manganja tribe, in the south-east of Africa, believe in a God, and in medicine, or the ordeal which he directs as the means of discovering crime. If the ordeal causes vomiting, it shows innocence; if it acts by the bowels, crime, and the person is put to death. But the doctors have a good knowledge of which to give, for there are different plants used.

Several granites and basement gneisses along the southern margin of the Siberian Craton were sampled to obtain precise age constrains and compositional isotopic data. The analysed granite plutons are interpreted to have been emplaced between 1880 and 1850 Ma, and are related to Palaeoproterozoic collisional and post-collisional events. Pb-Pb whole data of a granulite (1884 ± 26 Ma) and a two mica granite (1821 ± 29 Ma) constrain these U-Pb single zircon ages. Sr, Nd and Pb-Pb isotope data reveal the crustal origin of the investigated rocks and the reworking of Archaean material. Nevertheless, a minor influence of a mantle component is still visible in the Pb isotopes. Geodynamically, the magmatic and metamorphic ages in the Kitoy area are linked to several Early Proterozoic events along the southern margin of the Siberian Craton. Since these events are all older than the assembly of Rodinia (about 1·4 Ga ago) the collisional processes are linked to the consolidation of the Siberian Craton itself in Early Proterozoic times.

The Kidston Collection of fossil plant slides in the Botany Department of the University of Glasgow contains a number of sections of a very notable stem labelled “Lepidodendron textum, Kidston, n.sp.” No mention is made of this species in any of Dr Kidston's publications, but the correspondence relevant to the Collection indicates the history of the slides. This may be briefly summarised.

As early as 1883, Dr Kidston had received from Mr J. Coutts two sections (Nos. 51 and 52) of this stem, which had been collected by the latter at East Kilbride, Lanarkshire, Scotland, from the Carboniferous Limestone Series of the Calderwood Beds (Hosie Limestone) in the Lower Limestone Group. Dr Kidston postponed description of this stem till he had better sections at his disposal; the specimen, however, was lost, and it was not till many years later that he rediscovered it in Dr John Young's collection in the Glasgow Municipal Museum, and had more sections cut from it (Nos. 1144–1153). No manuscript notes of Dr Kidston's descriptive of these slides have been found, with the exception of a pencilled reference in his manuscript slide catalogue, opposite Nos. 51 and 52, to the “foliar bundles—there is an appearance as if there was a development of secondary xylem, whereas the axial bundle has no secondary wood.”

Locally abundant and diverse brachiopod faunas, associated with unstable outer shelf and slope environments, occur throughout the Barr and Ardmillan groups (middle Llanvirn–upper Ashgill) in the Girvan district of SW Scotland. A dataset of 350 brachiopod species from 30 horizons through the Middle–Upper Ordovician succession forms the basis for a description of brachiopod diversity through the succession and comparison with global patterns and trends through this time interval. The Middle Ordovician Barr Group incorporates shallow water carbonate and clastic facies, characterised by Valcourea confinis, with deeper-water facies. The trilobite-dominated Albany Group preserves outer shelf biofacies. Deep-water facies occur in the Balclatchie Formation of the lower Ardmillan Group, including an early occurrence of a Foliomena-type species. High diversity brachiopod faunas occur in clastic facies, though many of the biofacies have a transported component to them. Representatives of the deep-water Foliomena fauna occur intermittently throughout the Upper Ardmillan Group, appearing in both the Whitehouse and Drummuck subgroups. This distinctive assemblage of small, thin-shelled brachiopods, including Dedzetina, Christiania, Cyclospira and Foliomena itself, is interbedded with a variety of other less cosmopolitan deep-water assemblages, including the Onniella–Skenidioides and Lingulella–Trimurellina associations. Shallower-water environments in the middle Ashgill Lower Drummuck Subgroup hosted the Fardenia–Eopholidostrophia association in sands, and the Christiania–Leptaena association in muds and silts. The remarkable Lady Burn Starfish Beds in the upper part of the group contain a variety of brachiopod-dominated assemblages, including the Eochonetes and Plaesiomys–Schizophorella associations, transported from various shelf locations, within a very diverse mid Ashgill biota. The upper Ashgill High Mains Formation contains abundant elements of the terminal Ordovician Hirnantia fauna, including Eostropheodonta, Hindella and Hirnantia itself, but also some taxa more typical of the Laurentian Edgewood Province. As a whole, the changing brachiopod biodiversity biofacies reflect environmental fluctuations, on this part of the Laurentian margin, driven by mainly eustatic and tectonic events against a background of global biotic radiation.

A Small picrite sill of critical significance is examined in detail, from top to bottom, with particular reference to the distribution and crystallization of the olivine. Statistical evaluation of the sizes of olivine crystals establishes a gradation from large phenocrysts to small groundmass crystals. The micrometric data indicate that, while the feldspar content has remained constant, there is an inverse relationship between the distribution of olivine and pyroxene. This relationship, viewed in conjunction with the common tendency toward skeletal crystallization of the olivine and its gradation in size, amounts to substantial evidence that much of the olivine rapidly crystallized at the time when the sill was emplaced. At a few places, the sandstones and grits, into which the sill has been intruded, have been fused. Where it has penetrated a dolerite dyke along its direction of strike, a non-porphyritic facies, with very much less olivine, is associated with xenoliths of peridotite and of fused sandstone. It is inferred, from the field relationships, that this non-porphyritic facies was intruded as a liquid, containing xenoliths, in advance of the picrite. The chemical composition of this liquid is more calcic than basalt. It is concluded that this earlier calcic liquid was followed by a later magnesian (picritic) liquid and that these liquids have probably a deep-seated genetic relationship with feldspathic peridotite. Further research must be directed toward investigating this relationship both experimentally and in picrite—peridotite rock associations.

In their account of the Orlock Bridge Fault of Northern Ireland and its presumed continuation into the Scottish Southern Uplands (the Kingledores Fault) Anderson and Oliver (1986) provide welcome detail in support of major strike-slip movement. However, their identification of the Kingledores Fault as a line of massive strike-slip movement is based on a number of assumptions which are permissible only because biostratigraphical control is generally sparse. In particular the assertion that the Kingledores Fault is a “giant step in the diachronous southerly ascent of the turbidite base” is founded largely on a misinterpretation of evidence recorded by Peach and Horne (1899), Griffith and Wilson (1982) and others.

Stable isotope data from the East Kirkton succession are used to elucidate the extent of hot-spring influence in the palaeoenvironment by constraining conditions of deposition of the silica and the formation of sulphides.

Petrographically silica occurs as chert laminae thought to be primary, and as patchy chert considered as replacive. No evidence for biogenic silica was observed. For 20 silica samples δ18O was measured for structural oxygen and δD for bound water. δ18O(SMOW) varied between +21 and +27‰ with no sample groupings related to petrography. The range in δD(SMOW) was from −50 to −90‰ with lower values characterising replacive or altered silica; water contents of both petrographic groups were similar. A plot of δ18O versus δD for the laminated primary silica defines a grouping about the line defined by Scottish agates (Fallick et al. 1985). This suggests for the unaltered silica a formation temperature of about 60°C and a fluid containing a strong component of meteoric water. The data imply a Lower Carboniferous meteoric water δ18O composition of −3‰ and δD of −15‰, consistent with the known palaeolatitude.

The only sulphide observed was pyrite; 34 samples were selected from a wide variety of lithological and textural occurrences. δ34S(CDT) ranges widely and continuously between +8 and −34‰ with no strong mode. The sulphur appears to be derived from several sources, and pyrite formation from a variety of conditions as indicated by such wide ranging data, but for the samples with the lowest δ34S the involvement of bacteria in sulphate reduction is inferred.

39. In the first part of this paper, read to the Royal Society of Edinburgh in April 1862, and published in their Transactions, I explained the principles of a method devised by me in 1850 for ascertaining the absolute conducting power of substances capable of being formed into long bars; and I also stated the general results of experiments made in 1851 on the Conductivity for heat of wrought Iron.

40. I explained in Art. 14 of that paper, that the publication of the results had been for ten years withheld, partly in consequence of the state of my health which completely interrupted the experiments, but still more from the defective graduation of some of the thermometers used, which made it necessary to submit the instruments to a careful scrutiny, and to repeat with the duly corrected numbers the whole of the elaborate projections of the curves and calculations from them, on which the accuracy of the final results of course depends.

The modes of life and environments of the extant agnathans (cyclostomes) are discussed in relation to their adaptations to temperature, light, oxygen and salinity. As their antitropical distribution indicates, both hagfishes and lampreys are cold water groups. Since hagfishes live in deeper waters than lampreys, they are not exposed to the marked seasonal changes in temperature and light which influence major events in the lamprey life cycle. Both groups tend to be nocturnally active, either burrowing during daylight as in the case of larval lampreys (ammocoetes) and most hagfishes, or showing cryptic behaviour as in the case of adult lampreys. Olfaction plays a major part in the location of prey, presumably aided in adult lampreys by their eyes and sensitive electrosensory system. Rates of standard oxygen consumption, ventilatory frequency and heart rate of adult lampreys increase at night. Standard oxygen consumption is relatively low in ammocoetes (as it also is in hagfishes) but increases markedly during metamorphosis into the adult lamprey. Ammocoetes and hagfishes, and to a lesser extent adult lampreys, are resistant to reduced environmental oxygen tensions. Differences in the oxygen dissociation curves of ammocoetes, adult lampreys and hagfishes can be related to differences in the characteristics of their monomeric haemoglobins and their environments and modes of life. The extraordinary tolerance of the hagfish heart to hypoxia is a reflection of a robust capacity for glycolysis, an LDH isozyme geared towards anaerobic functioning and a low work output. The hagfishes, which are restricted to marine waters, are osmoconformers. The osmolality of their blood, which is almost wholly attributable to inorganic ions, is virtually identical to that of full strength sea water (c. 1000 mOsmkg−1). By contrast, the osmolality of the blood of larval and adult lampreys when in fresh water is only 205-260 mOsm kg−1, i.e. about one quarter to one fifth of those of hagfish, and these rise only to 240-270 mOsm kg−1 in the adults of anadromous lampreys in sea water. The regulation of ions by adult lampreys is achieved by mechanisms similar to those adopted by teleosts. The implications of the contrasting ionic and osmotic physiology of the two living groups of agnathans are discussed in relation to their possible environmental history and against the background of their Carboniferous fossil representatives.

During the cruise of H.M.S. “ Triton ” a small but very interesting collection of Pycnogonids was made. Mr John Mueray sent it over to me, and asked me to prepare a report on it, which I gladly undertook to do.

Significant new material of Late Devonian Gogo Formation fish fossils is still surfacing. Collecting in the past decade has uncovered the first Gogo shark fossils (Gogoselachus plus another new undescribed taxon), the first acanthodian (Halmacanthodes ahlbergi), the first coelacanth, as well as the first placoderm embryos. Recent studies have elucidated the nature of placoderm claspers, pelvic girdles, synarcuals and embryos, the structure of their teeth, a description of well-preserved muscles in placoderms, and how muscles attach to bones. Molecular biomarkers have also been identified in Gogo fossils. There are now five basal ray-fin fishes in the fauna, including one undescribed new taxon. The lungfish fauna from Gogo is the most diverse known for any Devonian site, with 10 genera and 12 species. The dermal skeleton and endocast of the dipterid Rhinodipterus kimberleyensis have been described in detail from CT scans; and the ontogenetic stages of neurocranium formation in Griphognathus. New specimens of the tetrapodomorph fish Gogonasus andrewsae have shed further light on its endocranium, pectoral girdle and fin. Through their exceptional preservation of both hard and varied kinds of soft tissues, the Gogo fishes remain crucial for resolving key debates on the diversification, physiology, biomechanics and phylogenetic relationships of early gnathostomes.

In this paper I give an account of observations made during a visit in 1879 to the Færöe Islands in company with my friend Mr Amund Helland of Christiania. The principal object of our journey was to examine the glacial phenomena of the islands, but we studied so far as we could the various rockmasses of which the group is composed, and constructed a geological sketchmap to show the line of outcrop of coal, the disposition of the strata, the direction of dykes, and the trend of the glaciation. I have only to add, that all the observations recorded in the following pages were made in concert with my friend, and I am glad to say that we were quite at one in our general conclusions.

Having been requested to act on a Committee of the British Association, appointed to devise and apply methods for measuring the comparative intensity of earthquake shocks, and having been shewn several ingenious contrivances by Mr David Milne (who suggested the inquiry) Lord Greenock, and other persons, an apparatus occurred to me which should unite the requisites of Simplicity, Compactness, Comparability, and an easy adjustment of Sensibility according to circumstances.

Mr Milne had not failed to distinguish the ends for which instruments (which for obvious reasons were to be self-registering) ought to be devised, such as the measurement of horizontal concussions, of vertical elevation, and of heaving or angular motion of the surface. It is no part of my present object to consider the probable movements of the soil in earthquakes. I limit myself to the description of a single instrument intended to measure lateral shocks, such as are experienced by objects placed upon a table which is abruptly shoved forwards.

Concerning the affinities and systematic position of this very remarkable Devonian fish, there has hitherto prevailed very great uncertainty. The two original specimens, discovered by Mr C. W. Peach, in the Old Red Sandstone of John O’Groat’s, Caithness, and described by Sir Philip Egerton, left us in complete ignorance as to the osteology of the head and the dentition, while the evidence they afforded as to the structure of the pectoral fins was by no means so clear as might have been wished for. To quote from Sir Philip's description:—“ The bones of the head, with the exception of a small fragment of the operculum, are wanting, but the impressions left upon the matrix show that they were sculptured in rather a bold pattern, not unlike the ornament on some of the cranial bones of some of the Holoptychii, and consequently differing in this respect from the corresponding parts in Dipterus. The pectoral fins are very indistinctly seen. They appear to have had a short obtuse lobe forming the base, and extending therefrom a set of numerous fin-rays more elongated than those forming the pectoral fin in Dipterus.” To Dipterus, however, in Sir Philip Egerton's opinion, its affinities pointed, as far as could be gathered from the structure of the body as displayed in the specimens, his description concluding as follows:—“ The absence of all evidence as to the dental apparatus of Tristichopterus is much to be regretted. On other points the affinities between this genus and Dipterus are so striking that they cannot be classified in separate families. Accordingly he assigned to Tristichopterus a place along with Dipterus in the family of “Cœlacanthi,” the term being used in its former extended sense, not as now restricted to the peculiar genera Cœlacanthus, Undina, Holophagus, and Macropoma.

The distribution of Arenig graptolite faunas and zones of differing metamorphic fades help to establish a polyphase imbrication history for the complex. A further complication is introduced by the presence within the imbricate stack of lava sequences of comparable age but with contrasting geochemical signatures of island-arc and oceanic island basalts, and oceanic island sequences of markedly different Arenig ages. Strike-slip mechanisms appear the most likely means of introducing such a disparate assortment of elements into the Ballantrae complex and an origin in a continental margin transform zone is preferred.

Forty-six years ago James Geikie published the third edition of his book, The Great Ice Age, where he expressed the view that there were five main cold periods, separated by four warmer, within the Pleistocene. Despite the enormous research by glaciologists undertaken since Geikie's time no one has yet disproved this fundamental concept; indeed, research, though perhaps casting out some of the evidence used by Geikie, has only supported his hypothesis. Yet the works of this great geologist are neglected and apparently scorned, for the terminology which he set up in plain English to indicate his five glacial periods, determined by a very wide survey, has been discarded in favour of a Continental nomenclature having only a local significance. In this work I follow Geikie in naming glacial periods, first, second, third, etc., for this has a world-wide application. It is from the writings of this master, and also those of Professor J. E. Marr of Cambridge, that I gathered the general ideas expressed here in Part I, (a), (b), and (c).

The most serious gap in our knowledge of the anatomy of the British Actiniaria has been the almost complete absence of structural data referring to the genus Phellia. The present paper deals with all the British species belonging to this genus, and adds some notes on other forms.

I wish to make the following acknowledgments. I have received a grant from the Royal Society, which has rendered possible the work described. I am indebted to my wife for preparing serial sections of the species of Phellia, and for drawing text-figs. 2, 3, 5, and 8. I also wish to thank Miss E. M. Stephenson for text-figs. 1, 9, and 10. Text-figs. 1, 6, 7, 11, and 12 have been reproduced before in my Ray Society Monograph on the British Sea Anemones (and text-fig. 12 in the Journal of the Marine Biological Association also), but their repetition here is essential for the demonstration of the several points which they illustrate.