The purpose of this note is to place on record two rare crinoids and a blastoid recently found at Coplow Knoll, Clitheroe. One of the crinoids belongs to a new species of Camerata now named Steganocrinus westheadi in honour of its finder, Mr. Stanley Westhead, of Clitheroe. The genus Steganocrinus has not hitherto been recorded from English Carboniferous rocks so that its occurrence at Coplow is noteworthy. The other crinoid, here temporarily assigned to “Pachylocrinus” conicus (Phillips), shows a considerable portion of the arms and was found by the author on a visit to Coplow last year. No other specimen of this species so complete has yet been recorded. On a later visit in the autumn of the same year a single finely preserved specimen of a blastoid was found. In its general characters this specimen does not appear to differ from Orophocrinus pentangularis (Miller), and in ordinary circumstances would call for no special comment here. Blastoids, however, are so rare at Coplow that the occurrence of this specimen, the only one ever found by the author at, or known to him from, this locality, is deemed worthy of record.

A Remarkable little fossil fish, Eucenturus paradoxus, was described by Traquair (1905) from a single specimen from the Calciferous Sandstone Series of Ardross, Fifeshire. Traquair's description is as follows: “This extraordinary little organism measures 2⅜ inches in length, of which ½ inch may be allotted to the head, and ¾ inch to the body, and 1⅛ inch to the tail. The head is a mass of calcareous matter, in which something suggestive of a broad curved mandible can be seen, but admits of no further description. The body, ⅜ inch broad in front, is composed of a greyish film, which, when examined by a strong lens, is seen to consist entirely of minute, slender, slightly-curved and sharp-pointed spinelets. The tail is tapering in form, consisting of amorphouslookingcalcareous matter, but on each side (assuming that the creature is crushed vertically) is a conspicuous row of double spinelets arranged exactly opposite each other. From a common base arise two spinelets, which are placed close together, and nearly parallel to each other; one of them, the anterior, being only half the length of the posterior one, which just behind the body may attain a length of 1/16 inch, though towards the end of the tail they become smaller; both spinelets are slender, slightly curved, round in transverse section, smooth externally, sharply pointed, and traversed internally by a central tubular pulp cavity. No trace either of internal skeleton, or of limbs, or of fins of any sort can be seen.”

Shumardiid trilobites had a small, unique morphology, and formed a key constituent in trilobite faunas during the Cambrian–Ordovician. Because of their unusual morphology, they have been the subject of research s, into various aspects such as their life habit, functional morphology, evolutionary origin and ontogeny. Originally, a flat, adult-like protaspid morphology was suggested for shumardiids, but subsequently a bulbous protaspid morphology interpreted to be associated with metamorphosis was also suggested for this unique trilobite group. This article documents the ontogeny of the two co-occurring shumardiid trilobites, Akoldinioidia latus Park and Kihm and Koldinioidia choii Park and Kihm, from the middle Furongian Hwajeol Formation, Taebaeksan Basin, Korea. Interestingly, protaspides of the two shumardiids have a bulbous morphology. Given the stratigraphic occurrences of the two shumardiids, it can be inferred that commutavi protaspis appeared quite early in the shumardiid evolution. The co-occurrence of the two closely related trilobites is reminiscent of sexual dimorphism, although further evidence is required to prove it. The appearance of metamorphosis-undergoing protaspides in the Furongian shumardiids may have been due to the onset of increasing ecological pressure in the early phase of the Great Ordovician Biodiversification Event.

The Foraminifera of the Chalk were treated of in Nos. 89 and 90 of the Geol. Mag., November and December, 1871, with the view of aiding collectors and authors in their arrangement of these numerous and puzzling microzoa in their catalogues and cabinets. We shall be rendering further service to students, if we refer them to the Rev. Henry Eley's clear and useful, though somewhat hard, drawings of the Foraminifera usually found in the English Chalk and Flint. These were published ia his “Geology in the Garden; or, the Fossils in. the Flint Pebbles.” 8vo. London, 1859.

White marble in Glen Dessarry, West Highlands of Scotland, occurs as three lenses associated with schists and calc-silicate rocks. The minerals identified in all these rocks are apatite, biotite, calcite, chondrodite, clinochlore, clinozoisite, diopsidic-pyroxene, dolomite, epidote, forsterite, garnet, hornblende, magnetite, phlogopite, plagioclase, potash-feldspar, pyrites, quartz, scapolite, sillimanite, sphene, vesuvianite, zoisite.

Two parageneses may be distinguished. One, due to high-grade regional metamorphism, apparently with little or no introduction of material, is a diopsidic-pyroxene, forsterite, phlogopite, calcite, dolomite association forming white marble. The other association occurs as veinlets and small irregular bodies in the white marble. It appears to be due to circulating solutions in which pyroxene and forsterite were unstable. Minerals of this paragenesis include potash-feldspar, plagioclase, scapolite, hornblende, minerals of the epidote group, calcite, and quartz. In certain localities scapolite formed at the expense of plagioclase and was succeeded by crystallization of epidote.

Gravity and aeromagnetic data sets provide systematic coverage over the whole of the Welsh Basin. Physical property information shows considerable overlap in densities within the Lower Palaeozoic and Precambrian formations, with relatively few units of the exposed succession being strongly magnetic. While the geophysical anomalies cannot be interpreted unambiguously in terms of these sources, the data can still be used to test different geological models and to indicate the range of possible solutions. The major fault zones are seen to influence the anomaly patterns in a variety of ways, reflecting a combination of differing near-surface contrasts and effects within the underlying basement. The general increase in gravity values towards Cardigan Bay may originate from the lower crust, and the large amplitude aeromagnetic low seen over Cardigan Bay indicates that a distinctive change in the character of the crust occurs here. Two-dimensional modelling in central Wales shows that a westward thickening of the Welsh Basin, to a maximum of about 10 km, may also be significant. It is necessary to postulate a separation of the base of denser, Lower Palaeozoic rocks from the underlying, more magnetic basement in order to account for offsets in anomaly source locations. This implies the presence of less dense Cambrian sediments and/or non-magnetic components of the Precambrian basement.

Within the Tethyan Zone of Central West Nepal, the Nilgiri Limestone is the dominant unit. The significance of the separation of the Larjung Formation is questioned in the light of new outcrops examined, and the Nilgiri Sandstone is described. Recumbent fold structures are correlated between Annapurna, Nilgiri and Dhaulagiri. Between these mountains the Thakkhola graben faults are continued southwards, and estimates are made of the magnitude of their throws.

Spore nomenclature and palaeobotanical nomenclature follow exactly the same rules. In both there are difficulties which must be understood historically.

A character of the suture-line that has received considerable attention lately is the obliquity with regard to the radius. Of course, it had long been noticed that suture-lines may vary in the form and foliation of their elements (brachyphyllic, dolichophyllic, and leptophyllic suture-lines of Mojsisovics, and euryphyllian and stenophyllian suture-lines of Haug) as in their general course. There maybe (externally) a strong convexity forward (Cyclololus), a straight (Sphenodiscus) or wavy line (Pseudosageceras), or a convexity backward (Protengonoceras). Again, the suture-line may be inclined strongly forward towards the umbilicus (Cheltonia) or have a retracted or dependent inner portion (Psiloceras). It is this Litter obliquity that has been used as a generic and even family distinction, e.g. by Mr. Buckman, to determine the affinity of Bredya with Hammatoceratidse, and not Hildoceratidæ.

Lastly a reference must be made to the nu-delta structures which characterize the contact zone between the continent of Eastern Asia and the floor of the Pacific. in the Sakhalin-Yezo-Kuriles system we find, by experiment, that the northern part of the system was pressed towards the continent to a greater extent than the southern part of it. This is a consequence to be naturally expected. In the Kuriles we find a succession of fractures which prove, beyond any doubt, that the region to the west of those lines effected a southerly or south-westerly horizontal shear against the Pacific. Such a movement not being parallel to the continental border, would necessarily arouse a lateral compression between the continent and the ocean base. Now since the southern terminus of the triangular area covered by the system lies against the Inshan zone which behaved as a strengthening rib on the part of the continental mass against lateral pressure, it would be extremely difficult for the southern apex of the triangular area to shift westward. On the other hand the northern part of the area does not encounter such extraordinary resistance. Consequently the whole area suffers a counter-clockwise twisting movement with the result that the nu-delta system was generated. In this way we are able to understand how the Sakhalin-Yezo-Kuriles system was produced through a southward movement of Eastern Asia.

Anyone who studies the relation of the rocks of the Lizard Peninsula to those immediately to the north must realize that Porthallow, the little village in a sheltered cove near St. Keverne, is a critical locality in the problem, and one indeed that may hold the key to the solution of the relative ages of the rocks on either side of the sinuous line called the Lizard Boundary. Porthallow is at the eastern extremity of that line. The western extremity is on Polurrian Beach, near Mullion, where a very clear fault with a breccia about 22 feet thick separates two totally distinct formations, sandy and argillaceous killas on the north from hornblendegneiss on the south. At Porthallow, however, although there are cliffs on either side of the cove washed by the sea, the geology is far from having the textbook clearness of Polurrian Beach and there is room for much difference of opinion. Text-fig. 1 is a sketch-map of the locality based on the Ordnance Survey 25 in. to the mile map, and first the main features of the geology will be described. For the neighbouring country the reader is referred to the Survey 1 in. map (Sheet 359) and to the 6 in., Sheet lxxxi N.E.

This paper describes in detail hydroplastic structures, which are ‘odd’ kinematic indicators in the basal part of the Eocene Middle Rus Formation. Such structures were previously ignored or falsely interpreted. These hydroplastic structures are found in the massive limestone exposures on the King Fahd University of Petroleum and Minerals (KFUPM) campus. They occur in relation to a principal displacement zone along the boundary/interface between the Lower/Middle Rus, which is referred to as the Rus soft-sediment detachment. The structures are fist-sized vugs associated with carrot- or comet-trail imprints (VCT structures) which were previously translated calcite geodes that have been weathered out. VCT structures show transport/slip towards the NNW (345°) and are found on flat to low-dipping surfaces classified as Y, R and P shears with respect to the orientation of the Rus detachment. Palaeostress analysis indicates an Andersonian transtension stress regime, though it does not facilitate the activation of the Rus soft-sediment detachment. Detachment activity occurred due to the negative effective principal stress σ 3′ and the abnormally low frictional coefficient caused by fluid pressure. The soft-sediment Rus detachment can be considered a ‘sensitive stress sensor’ for the Zagros collision since it indicates the Arabian platform’s instability in the wider area of the Dammam Dome during the Late Eocene. This instability is attributed to the inception of the Zagros collision, which was previously considered to occur during the Oligocene based on the well-established pre-Neogene unconformity.

Very hard cemented chalk stacks and crusts found locally in the upper part of the Cretaceous Chalk of north Norfolk, UK, are related to solution features. The solution features, mainly pipes and caves, formed after deposition of the overlying Middle Pleistocene Wroxham Crag, probably by routing of sub-glacial, or glacial, melt-waters derived from late Pleistocene glaciers. New geochemical (particularly stable isotope) data shows that cementation of the chalks, although related spatially to the solution features, was not caused by glacier-derived waters. The carbon isotope composition of the chalk cements is typically around −9.5‰, indicative of biologically active soils. Moreover, the oxygen isotope compositions of the cements, around −5‰, are incompatible with water δ18O values much below −9 to −10‰ (which probably precludes isotopically negative glacier-derived water), as resulting palaeo-temperatures are below zero. Taken together, the isotope data suggest chalk cementation occurred under interglacial conditions similar to the present. Dissolved calcium carbonate for cementation came from dissolution of reworked chalk in overlying MIS 12 glacial tills.

It is not proposed to discuss the merits of the generic name applied to a group of Univalves so characteristic of and so abundant in the Jurassic rocks. Melania, Eulima, and Chemnitzia have each of them served in turn, and in adopting Chemnitzia after D'Orbigny, the late Dr. S. P. Woodward observed that the “Melaniœ” of the Secondary rocks are provisionally referred to this genus. Pictet and Campiche include the Chemnitziœ and Phasianellœ of the Oolites in one genus Psendomelania, thus preserving to a certain extent the old generic appellation.

In the year 1861 I communicated to the Geological Section of the British Association, which that year met at Manchester, a description of certain fossils discovered by J. H. Cockburn Hood, Esq., in the Canterbury Settlement of the Middle Island of New Zealand; which fossils, kindly submitted to me for description by that gentleman, were afterwards presented by him to the British Museum.

This fine specimen, which has been so faithfully rendered in two views by Miss G. M. Woodward, was thund by me, together with portions of other individuals of the genus, in some red finely-sandy or silty beds, interstratified with grits, in the Cutting of the new road on the eastern side of Lincombe Hill at Torquay. The beds are traversed by a coarse cleavage dipping south, which usually ignores the hard grit bands. We may call them for the present the “Lincombe, Warberry, and Smuggler's Cove grits,” and their probable equivalents will be considered shortly.

The ammonite species Cymbites laevigatus (J. de C. Sowerby) is fully described and illustrated for the first time. Nomenclatural problems are discussed. The interpretation of the genus Cymbites, and of its type species, Amm. globosus, is reviewed.

In my brief paper published in this Magazine for 1880 (Decade II. Vol. VII. p. 404), I mentioned that pebbles of felstone were not uncommon in the Bunter conglomerate on the northern part of Cannock Chase. Since that time, as opportunity has occurred, I have been making a more special study of these pebbles, and think it may be worth while publishing a description of some of the commoner varieties, as a contribution to the lithology of this interesting deposit and a help to the determination of the question of the origin of its material. I believe that I have observed most of the varieties, which commonly occur in the district, but do not pretend (for circumstances have not allowed of this) to have made anything like a complete collection. Many of my specimens have been derived from the broken materials spread upon some roads newly made over the portion of the Chase in the vicinity of Rugeley, but several of them were obtained in a large pit in the Bunter itself, by the side of the railway on the road to Hednesford, and I was able by a careful search in it to identify most of the varieties that I had collected elsewhere. I cannot say that erratics are absolutely unknown in this district, but they are extremely rare, and there is practically no danger of making a mistake as to the source of the pebbles. These pebbles of felstone (to use an inclusive term) appear to be by no means rare. I think one could hardly search a couple of square yards of a newly “metalled” road without picking up a fragment. Now and then specimens are found with a dark ground-mass, and occasionally one which seems to be an indurated felspathic breccia; but in the majority there is a certain common character, though there are many varietal differences. These have a compact ground-mass, varying from a pale brick-red (the commonest) to some tint of pinkish-grey.