Immediately W of the islands of Uist in the Outer Hebrides is a wide, low-gradient submarine shelf on which glacifluvial deposits of Devensian age and calcareous sand accumulated. Following moulding by Devensian ice, the Lateglacial landscape of the littoral zone of the Uists became a series of low-lying bedrock ridges and basins. The analysis of sub-tidal organic deposits has shown that in the early Holocene this landscape supported water bodies, marshes and a vegetation mosaic of Betula-Corylus woodland and Calluna vulgaris-herbaceous taxa open ground. The submergence of this littoral area during the Holocene Marine Transgression, together with wave action typical of the position on the Atlantic margin, led to the transfer onshore of submarine shelf deposits, so creating machair (sand plain) landscapes. This brought about vegetational changes, eventually creating calcareous grasslands. The timing of these events was asynchronous, being location- and site-specific due to variations in the configuration of the littoral zone. Although the date of the initial transfer of sand is unknown, evidence from the sub-tidal deposits indicates that a major incursion of sand, in North Uist, occurred c. 7600 BP (8450–8340 cal BP). The same source also suggests that a further major sand movement took place during the period 5800–4200 cal BP, a period of widespread sand drift in NW Europe. The analyses of the sub-tidal deposits have also reinforced the current theory of machair evolution.

The development of the Midland Valley of Scotland from Silurian times is re-examined. Earlier (Cambro-Ordovician) terrane accretion of the Midland Valley Terrane to the Laurentian continent by sinistral strike-slip continued to control basin development, sedimentary facies distribution and deformation from Llandovery through to at least early Devonian times. A widespread Mid- to Late-Wenlock strike-slip event has been recognised. This event is variable in its effect, but may indicate a direct link between the Midland Valley, Southern Uplands and Grampian terranes, suggesting that the terranes were juxtaposed by Mid-Wenlock times. In the Midland Valley this event was followed by a renewed phase of basin development with the deposition of ?Pridoli-Lower Devonian clastic sediments which was interrupted by the Lower Devonian volcanic event. There was a shift northwards in the focus of Lower Devonian basin development which was accompanied by a diachronous deformation event across the Midland Valley which resulted in inversion/uplift from early to middle Devonian times. This phase of deformation, uplift and erosion may be related to end-Caledonian transpression.

Lower Cambrian shallow-water carbonates enclosing microbial structures are documented for the first time from the upper Lastours Member of the Montagne Noire (southern France). Microbial organisms constructed self-supported boundstones resulting in the formation of exclusively microbial-accreted buildups, which exhibit three main types of non-skeletal microbialites: planar stratiform stromatolites, dome-shaped stromatolites and nonlaminated (thrombolitic) biostromes. In addition, thrombolitic boundstones display four distinct microbial microstructures: clotted and Renalcis-like forms, branching bushy forms, clusters of unbranching straight filaments and crustose forms.

The upper member of the Lastours Formation records an upward transition from a shalydominant open shelf to a protected shelf environment bounded by a surface representing a major subaerial exposure. Initially, at the inception of the highstand systems tract, flat stratiform stromatolites formed on open sea subtidal shaly substrates, while stacked domal stromatolites developed in peritidal areas which record subaerial exposure. In contrast, prograding shoal barriers of the transgressive systems tract favoured the establishment of thrombolitic boundstones in protected (back-shoal) environments.

A review of the faunistic composition of the coleopterous taphocenoses from Bembridge Marls is given. Only two families (Cupedidae and Carabidae) have been recorded from this site before. A total of 31 families have been revealed and determined in the course of the recent study, and 42 species have been described: Agabus latissimus Ponomarenko, sp. nov. and Ilybius gratshevi Ponomarenko, sp. nov. from Dytiscidae; Neothanes europaeus Ponomarenko, sp. nov. from Carabidae; Spercheus punctatus Ponomarenko, sp. nov., Spercheus wightensis Ponomarenko, sp. nov. from Spercheidae, Hydrochara woodwardi Ponomarenko & Soriano, sp. nov. and Berosus barclayi Ponomarenko & Soriano, sp. nov. from Hydrophilidae; Ochthebius rossi Kirejtshuk, sp. nov., Eolimnebius fossilis Kirejtshuk, sp. nov., Hydraenites gracilimmus Kirejtshuk, sp. nov., Metacoxites ventritalis Kirejtshuk, sp. nov., Davidraenites gratshevi Kirejtshuk, sp. nov., D. interruptus Kirejtshuk, sp. nov. and D. spurcus Kirejtshuk, sp. nov. from Hydraenidae; Aphodius vectis Krell, sp. nov. and Pentodon dorcus Krell, sp. nov. from Scarabaeidae; Scirtes calcariferens Kirejtshuk & Ponomarenko, sp. nov., Scirtes khnzoryani Kirejtshuk & Ponomarenko, sp. nov., Scirtes metepisternalis Kirejtshuk & Ponomarenko, sp. nov., Scirtes wightensis Kirejtshuk & Ponomarenko, sp. nov., Contacyphon insularis Kirejtshuk & Ponomarenko, sp. nov., Contacyphon involutus Kirejtshuk & Ponomarenko, sp. nov. and Contacyphon kozlovi Kirejtshuk & Ponomarenko, sp. nov. from Scirtidae; Eucinetes nikolaevae Kirejtshuk & Ponomarenko, sp. nov. from Eucinetidae; Macropunctum rossi Alexeev, sp. nov. from Elateridae; Byrrhites bembridgensis Kirejtshuk, sp. nov. from Byrrhidae; Paralichas striatopunctatus Kirejtshuk, sp. nov. from Ptilodactylidae; Trixagus barclayi Kirejtshuk, sp. nov. from Throscidae; Themus (?Telephorops) polyaki Kirejtshuk, sp. nov. from Cantharidae; Attalus flexus Kirejtshuk, sp. nov. from Malachiidae; Epuraea (Epuraea) kozlovi Kirejtshuk & Kurochkin, sp. nov., Phenolia (Lasiodites) vanescens Kirejtshuk & Kurochkin, sp. nov., Prometopia europaea Kirejtshuk & Kurochkin, sp. nov., Cyllodes argutus Kirejtshuk & Kurochkin, sp. nov. and Coxollodes palaeogenicus Kirejtshuk & Kurochkin, sp. nov. from Nitidulidae; Telmatophilus britannicus Kirejtshuk & Kurochkin, sp. nov. from Cryptophagidae; Corticariites kozlovi Kirejtshuk, sp. nov. from Latridiidae; Orthoperites antiquus Kirejtshuk & Kurochkin, sp. nov. from Corylophidae; Octotemnites sepultus Kirejtshuk, sp. nov. from Ciidae; Cyclodinus efficax Kirejtshuk, sp. nov. from Anthicidae; and Plateumaris robustus Kurochkin & Kirejtshuk, sp. nov., Plateumaris rubiconis Kurochkin & Kirejtshuk, sp. nov. and Plateumaris wightensis Kurochkin & Kirejtshuk, sp. nov. from Chrysomelidae. Byrrhites Kirejtshuk, gen. nov., Corticariites Kirejtshuk, gen. nov., Davidraenites Kirejtshuk, gen. nov., Eolimnebius Kirejtshuk, gen. nov., Hydraenites Kirejtshuk, gen. nov., Metacoxites Kirejtshuk, gen. nov., Octotemnites Kirejtshuk, gen. nov. and Orthoperites Kirejtshuk & Kurochkin, gen. nov. are proposed as taxa, partly as formal ones with generic rank and include species described herein. For Plateumaris rubiconis sp. nov., a new subgenus Necrodexis Kurochkin & Kirejtshuk, subgen. nov. is proposed. A brief review of the published fossil records for the groups considered in the paper is made. The probable ecological circumstances of the lives of the groups and species considered are discussed in the paper, and comparison with other Palaeogene sites and some conclusions on probable climatic circumstances have been elaborated. The taxonomic interpretation of three fossil species from the Caenozoic is reconsidered. It is shown that the genus Miocyphon Wickham, 1914 can be scarcely regarded as a close relative of representatives of either Dascillidae or Scirtidae. ‘Phenolia' incapax Scudder, 1890 and Lithomacratria Wickham, 1914 are regarded here without family attribution, the first as a member of Cucujiformia (i.e., out of Nitidulidae) and the latter as a member of the superfamily Tenebrionoidea (i.e., out of both Anthicidae and Pyrochroidae).

Since the report on the Hydroids collected by the Scotia was completed, almost three years ago, I have had an opportunity, thanks to the kindness of Dr W. S. Bruce, of looking through the enormous mass of material brought together by him during his Antarctic voyages. The search, begun in the hope of finding a few minute species—which, since many are epizoic on other forms of marine life, might readily be overlooked on cursory examination—has resulted in the addition of no less than 25 forms to the 36 already recorded. Deducting from this total of 61 forms two varieties, it appears that the Scotia collection contains in all 59 distinct species. Few, indeed, of these have been obtained in truly Antarctic latitudes—subantarctic or temperate seas having furnished the greater number—but this result is in accordance with the findings of the majority of the recent Antarctic expeditions. Dr Billard, in summarising the results of the Belgian, Swedish, and French expeditions, states that the known Hydroid fauna of Antarctic regions comprises only 32 species. But from his list he has, I think unjustly, excluded South Georgian records. His list, moreover, published before the valuable paper by Professor Hickson and Mr Gravely on the Discovery Hydroids was issued, necessarily makes no reference to the large number of forms recorded by them from Victoria Land.

Historic type and referred material of the aetosaurian taxa Typothorax coccinarum, Episcoposaurus horridus and Episcoposaurus haplocerus are redescribed and the non-aetosaurian material identified and removed, a task previously considered “hopeless”. Reexamination of the original material reveals that the holotypes of E. haplocerus and probably T. coccinarum are not diagnosable at the species level and therefore are nomena dubia. The next available names for material referred to these taxa are Desmatosuchus spurensis and E. horridus respectively, although it may be more desirable for reasons of taxonomic stability to attempt to petition for a neotype in the latter case. The redescription of historical specimens is necessary to determine their nomenclatural validity. The use of referred specimens as proxy “type” specimens is problematic, as these referrals were originally made not on the basis of apomorphies, but rather on biostratigraphic and/or geographical assumptions which are inherently circular and cannot be unambiguously supported.

Pegmatites at the East Kemptville Sn-Zn-Cu-Ag deposit occur within a F- and P-rich, 370 Ma topaz-muscovite leucogranite, the most evolved phase of the chemically zoned Davis Lake Pluton. Structural observations and geochronology indicate that the leucogranite intruded into an active shear/fault zone environment. Pegmatites are preferentially located near the roof zone of the intrusion and include: (1) quartz-feldspar pods (≤ 1–2 m) aligned parallel to a foliation in the leucogranite. Such pegmatites have marginal aplites or may be cored by aplites; (2) aplite-pegmatite zones with well-developed crenulate and unidirectional solidification textures; and (3) muscovite-bordered miarolitic cavities lined with quartz-feldspar ± cassiterite. Associated with areas of pegmatites are irregular- to cuspate-shaped zones enriched in muscovite. Mineralogically the pegmatites are simple, consisting of clear to black quartz, albite, microcline perthite and muscovite; topaz may be enriched in aplites coring pegmatites and coarse euhedral cassiterite is rare.

Chemically the leucogranites marginal to pegmatites are similar to the host leucogranite, but some aphanitic felsic dykes indicate extreme differentiation, as reflected by REE depletion and P-enrichment. Enrichment of pegmatitic feldspar in P2O5 (to 1 wt. %) indicates that melts contained 2–3 wt. % P2O5, whereas muscovite chemistry (to 5 wt. % F) reflects the F-rich nature of the melt. Trace and REE contents of pegmatitic feldspars are consistent with local segregation of volatile-rich melts to form pegmatites rather than extreme crystal-chemical fractionation.

Fluid inclusion studies of pegmatitic quartz and cassiterite indicate the presence of a highly saline brine (40 wt. % eq. NaCl; Na > K > Fe > Mn > Ca > Sr) of magmatic origin. Isochores modelled for a 40 wt. % eq. NaCl fluid constrain pegmatite formation at 550–600°C, thus the depressed solidus is consistent with the volatile-rich (F, P, H2O) nature of the melt. Stable isotopes demonstrate that a magmatic fluid (δ18OH2O = +5·5 to +10‰, δDH2O = −33 to −41‰ for 450–500°C) equilibrated with the pegmatites and the system cooled abruptly at c. 425°C.

The low volume of pegmatite at East Kemptville suggests that the melt was not near volatile saturation, instead pegmatite generation is interpreted to have resulted from rapid decompression related to the active shear zone setting of the granite. Although feldspar chemistry reflects a local segregation model, the chemistry of aphanitic dyke rocks indicates that the leucogranite did evolve into a more fractionated melt. The local presence of cassiterite in pegmatites and miarolitic cavities indicates that locally, saturation of Sn occurred, but not throughout the EKL where elevated Sn contents are attributed to infiltration of mineralising fluids (i.e. deuteric alteration).

In Strathaird, Tertiary lavas occupy an area of about 7 square miles and are up to 1000 ft. thick. Most of the sequence consists of alkaline olivine basalts but there is also a flow of trachybasalt and a thin group of picritic lavas. Pyroclastic rocks are rare.

The area lies along the south-eastern margin of the Cuillin gabbro and thermal metamorphism is evident to a varying degree over the whole of the lava outcrop. In the immediate vicinity of the gabbro the lavas have been recrystallized to pyroxene-bearing hornfelses, and these rocks are followed outwards by a broader zone characterized by the presence of actinolite, chlorite, albite and epidote. In the outermost of the three zones, which extends for at least 3 miles from the gabbro, thermal effects are limited to the local growth of chlorite, albite and epidote. When compared with Turner's (1958) scheme of metamorphic facies the inner zone is equivalent to the pyroxene hornfels and sanidinite facies whereas the two outer zones form subdivisions of the albite-epidote hornfels facies. The hornblende hornfels facies appears to be only poorly represented by a few hornfelses found on the outer boundary of the inner zone.

The metamorphism was not progressive since the mineral assemblages of each zone developed independently from unmodified lavas. There is evidence that a small amount of silica was added to some of the inner zone lavas during metamorphism.

Eight new chemical analyses of metamorphosed basalts are presented, together with one new analysis of a metamorphosed bole.

The lead isotope compositions of 61 galenas from central and southern Scotland vary markedly between different regions. Most galenas from the southern Grampian Highlands yield isotope ratios (206Pb/204Pb 17·77 ± 0·25, 207Pb/204Pb 15·47 ± 0·05, 208Pb/204Pb 37·63 ± 0·26) less radiogenic than those from Midland Valley galenas (18·22 ± 0·12, 15·55 ± 0·05, 38·13 ± 0·14) whilst galena lead from the Southern Uplands (18·28 ± 0·12, 15·56 ± 0·03, 38·21 ± 0·18) is more radiogenic than that from the southern Midland Valley (18·12 ± 0·06, 15·52 ± 0·02, 38·06 ±0·10). The change in isotopie composition across the Highland Boundary fault reflects the presence or absence of Dalradian rocks which included a magmatic component of lead. Galenas from the Dalradian sequence in Islay, where igneous rocks are lacking, have a composition (18·14±0·04, 15·51±0·01, 37·90±0·02) more like Midland Valley galenas. In the Southern Uplands, galenas yield lead isotope ratios similar to those of feldspars from Caledonian granite (18·30 ± 0·14, 15·57 ± 0·04, 37·96 ± 0·15) analysed by Blaxland et al. (1979). The similar ratios reflect the incorporation of Lower Palaeozoic sedimentary rocks into the granite magma, rather than a granitic source for the mineralisation. The granites were then thermal-structural foci for later mineralising fluids which leached metals from the surrounding rocks. Within the Midland Valley, galenas hosted in Lower Devonian-Lower Carboniferous lavas are notably more radiogenic (18·31 ±0·12, 15·58 ± 0·06, 38·20 ± 0·16) than sediment-hosted galenas (18·14 ± 0·07, 15·52 ± 0·02, 38·08 ± 0·10). The Devonian lavas at least may have inherited lead from subducted (? Lower Palaeozoic) rock incorporated in the primary magma.

Well-preserved compression material of Zosterophyllum myretonianum Penhallow from the Lower Old Eed Sandstone in Angus has yielded additional information about the structure of this plant, one of the earliest known types of vascular land plants. It is the earliest plant in which the structure of the epidermal cuticle, stomata and complete tracheids has been clearly demonstrated. The basal regions of the plant are found to consist of branching axes some with arrested or dormant side branches. Simple dichotomy into two equal and similarly orientated branches is rare. H-type branching and some modifications of it are of frequent occurrence in the basal region of the plant. Parts of this region of the plant have no stomata although a cuticle was present. The upright fertile axes rarely branched.

Lepidodendron calamopsoides sp. nov. is described from petrified protostelic stems formerly considered identical with Levicaulis arranensis Beck. The stems range from 2 to 20 mm. diameter and some possess leaf-cushions usually about 10 × 1 mm.

Three specimens are known showing the transition from stem to rooting organs. Secondary xylem has only been seen in the transition region and rooting organs. The latter resemble Calamopsis dubia Solms-Laubach now considered to be part of the closely related Lepidodendron saalfeldense.

At the time of his death Dr Duerden was contemplating the preparation of a paper of this nature, and it is felt by Mrs Duerden that had he been able to express his wishes in this connection he would appreciate a record of the conclusions made by him. No one realised more than Dr Duerden himself the gaps which are still present in our knowledge and interpretation of the grouping of follicles and fibres in the mammalia, and this work is certainly not meant to be taken as representing Dr Duerden's final view or those of his colleagues at the Wool Industries Research Association. In view of the unique value of much of the material the present notes are intended, therefore, to form a basis and reference, firstly, for workers engaged in the general development of any mammalian coat from a morphogenic and phylogenetic point of view, and secondly, for those interested particularly in factors concerned in the formation of different types of fleeces in sheep. The conception of the follicle bundle as a discrete and basic genetic unit largely determining the initial form of the wool staple is of the highest importance in studies on the inheritance and developmentof fleece characters.

In the Proterozoic complex of the Schirmacher region of East Antarctica, a retrograde pressure–temperature (P–T) history has been inferred through quantitative geothermobarometry and fluid inclusion studies of the mafic granulites. Microthermometric investigations of the fluid phases trapped in quartz and garnet identified three types of inclusions, namely, earliest pure CO2 inclusions (0·987–1·057 g cm−3), CO2–H2O inclusions and aqueous inclusions.

The temperature and pressure of metamorphism have been estimated through different calibrations of geothermometers and geobarometers. The mineral reactions and compositional zoning in the minerals record P–T conditions from nearly 837 ± 26°C, 7·1±0·2 kbar to 652 ± 33°C, 5·9 ± 0·3 kbar. A good correlation between the fluid and mineral data is observed. The isochores typical of highdensity CO2 fluids fall well within the P–T box estimated by mineral thermobarometry. The abundance of primary CO2 inclusions in early metamorphic minerals (notably quartz and primary garnet) and the general correspondence between fluid and mineral P–T data indicate a ‘fluid-present’ carbonic regime for the high-grade metamorpism; however, from the present data largescale CO2 advection could not be envisaged. The subsequent stages involved a decrease in CO2 density, a progressive influx of hydrous fluids and the generation of retrograde amphibolite facies metamorphism in the area.

The estimated P–T conditions of the region suggest that the rocks were metamorphosed at a depth of 19–24 km, with a geothermal gradient of c. 3°5C km−1. The estimated P–T conditions of the rocks imply a clockwise P–T–t path with a gradual decrease in temperature of around 250°C and a decrease in pressure of around 1700 bar. They have a dP/dT gradient of ≈7 ± l bar °C−1, arguing for an isobaric cooling history of the terrane under normal thickened crust after the underplating of mantle-derived material.

In 1861, in a part of the province of Otago, New Zealand, not previously botanically explored, I made, among other botanical collections, one of Lichens and Fungi. The number of new species and varieties proved to be considerable, amounting to about 20 per cent. of the whole lichens, and 40 per cent. of the whole fungi, collected. Since my return home, I have submitted (with a view specially to the study of the minute anatomy of the reproductive organs and their contents) the new species (and varieties) in question—some of them repeatedly—to microscopical examination: the results whereof are contained in the notes which follow.

The Mucorales have a wide geographical distribution and for seventy years they have been the subject of investigation both in Europe and in America. In this country, however,little research has been done on this group, the only workers being Bayliss-Elliott (1930) who has investigated the microflora of the Dovey salt marshes, Dale (1912, 1914) who examined the fungus flora of soil at Cambridge, and Brierley (1923, 1927, 1928) who has done considerable work on soil study. Although certain of the Mucorales were isolated by the last named, he was mostly concerned with the general methods of soil culture. The important quantitative technique was devised by Brierley (1927). Oudemans and Koning (1902) were the first to show the presence of Mucors in the soil. They examined the soil fungi in Holland and isolated two new species of Mucors. Möller (1903) investigated the fungi found in Pine mycorrhiza and obtained a further four new species. Hagem (1907, 1910) studied the morphology and physiology of seventeen Mucors from the soil of Norway, seven of which were new species. In 1908 Lendner published his “Les Mucorinées de la Suisse,” an important contribution to the study of this group of fungi. A criticism which might be levelled at this work is that it is difficult to ascertain from it whether or not Lendner used pure cultures on which to base his descriptions. He merely states that “dilution methods used in Bacteriology were employed,” no mention of monospore cultures being made. Further important work on this group has been done by Korpatschewska (1909), Namy-slowski (1906, 1920), Naumov (1914, 1924, 1935), Ling-Young (1930), Johann (1932), Jensen (1912, 1931), and in the Kryptogamenflora der Mark Brandenburg (1935) Zycha gives a complete revision of the classification of the Mucorales. A survey of the geographical distribution of this group of fungi is found in the work of Niethammer (1935), while further classification has been done by Linnemann (1936). In America, Povah (1917) and Waksman(1916, 1917, 1922, 1927) have both added considerably to our knowledge of the Mucorales in the soil.

The causes of compositional diversity in the Tuolumne Batholith, whether source heterogeneity, magma mixing, or fractional crystallisation, is a matter of longstanding debate. This paper presents data from detailed mapping and a microstructural and major element, trace element and isotopic study of an elongate lobe of the Half Dome granodiorite that protrudes from the southern end of the batholith. The lobe is normally zoned from quartz diorite along the outer margin to high-silica leucogranite in the core. Contacts are steep and gradational, except for the central leucogranite contact, which is locally sharp: magmatic fabrics overprint contacts. A striking feature of the lobe is the 18 wt SiO2 range comparable to that observed for the entire Tuolumne Batholith. Feldspar-compatible elements (Sr and Ba) decrease towards the centre, while Rb increases. Light and middle REEs show a smooth decrease towards the centre of the lobe. Calculated initial isotopic ratios of 87Sr/86Sr(i) and εNd(t) have identical values within error across the lobe, except in the central leucogranite, the most silica rich phase, which shows a slightly more crustal signature. Field, structural, geochemical and isotopic data suggest that fractionation was the dominant process causing compositional variation in this lobe. It is envisioned that this fractionation/crystal sorting occurred in a vertically flowing and evolving magma column with the present map pattern representing a cross-section of this column. Thus the areal extent of the lobe represents a minimum size of interconnected melt at the emplacement level of the Tuolumne Batholith and, given its marginal position, limited width and proximity to colder host rocks, implies that fractionation in larger chambers likely occurred in the main Tuolumne Batholith magma chamber(s).

The genus Anaspides was founded in 1894 by Mr G. M. Thomson of Dunedin, New Zealand, for the reception of a very remarkable Schizopod Crustacean which he had discovered in a fresh-water pool at an altitude of 4000 feet on Mount Wellington in Tasmania. The very striking peculiarities of the animal, the absence of a carapace, the presence of plate-like gills attached to the bases of the thoracic legs, and the possession of an auditory organ in the peduncle of the antennules, led its discoverer to regard it as the type of a new family of Schizopods, the Anaspidæ, while suggesting that it might be entitled to “even higher specific rank.” I have had an opportunity of examining three specimens of Anaspides presented to the Museum of University College, Dundee, by Dr Chas. Chilton of New Zealand, and from the dissection of one of these I have been able to supplement, in some important points, Mr Thomson's account of the external anatomy of the animal. I wish also to call attention to the remarkable resemblance, indicative I believe of close affinity, which Anaspides bears to certain Palaeozoic Crustacea belonging to a group hitherto supposed to be unrepresented among living forms. The present paper has been prepared under the direction of Prof. D'Arcy W. Thompson.

Harmaline is one of two alkaloids found in the seeds of Peganum Harmala, a strong-smelling herbaceous plant belonging to the order of Rutaceæ. This plant grows to a height of from 1 to 3 feet, is much branched, and profusely covered with leaves. It is found wild in S. Europe, Asia Minor, Egypt, Arabia, N.W. India, and Siberia. It is the Πήγανον ἄγριον (wild rue) of Dioscorides, Πήγανον being the name still applied in Greece to several species of Ruta.