ALBERT

Description: The genus Stenandriopsis was created by S. Moore in Journ. of Bot. 44: 153. 1906 for a plant collected first by Vaughan Thompson and afterwards by Baron in an unspecified part of Madagascar. As the plate by which the description is accompanied depicts the specimen collected by Baron (n. 6708), the latter is to be regarded as the type. Stenandriopsis was referred by its author to the Justicieae, but this tribe is apparently accepted by him in the delimitation it received in BENTHAM and HOOKER’s “Genera Plantarum”, and as it is in this sense a most heterogeneous mixture, this does not greatly enlighten us. Of more importance is that Moore compares it with Crossandra Salisb. and Stenandrium Nees, i.e. with genera belonging to my subfamily Acanthoideae and referred by me respectively to the Acantheae and the Aphelandreae. However, in my paper on “The Acantheae of the Malesian Area. I. General Considerations” in Proc. Kon. Ned. Akad. v. Wetensch., Ser. c. 58: 166. 1955, I pointed out that it can not belong to the Acantheae as the corolla throat lacks the incision in the adaxial side which is characteristic for that tribe. It can not belong to the Aphelandreae either as the corolla limb is subactinomorphous instead of distinctly bilabiate. As I had to rely at that time entirely on Moore’s description and on the plate by which the latter is accompanied, I was unable to arrive at a conclusion, but I suggested that the genus might represent a new tribe of my Acanthoideae. Since then I have had the opportunity to inspect in the herbarium of the British Museum of Natural History the material on which the genus was based, for which I tender my best thanks to the Keeper, and now I am able to express a more definite opinion.

Description: During my studies of the Surinam specimens belonging to this genus my attention was drawn to the often wrong interpretation of several old species. To avoid future misidentifications it seems useful to give a short review of the American species that are known up till now. It is emphasized, however, that this paper does not have the pretension to be a monograph of the American species. For the greater part my study of the species was confined to the type material and the variability therefore is not known. However, this contribution may serve as a base for a future monograph of this interesting group. Attention is drawn to the fact that only older leaves of the plants should be studied, because the leaf apex of the younger leaves is in all species acute and the lamina may not have reached its definite form.

Description: This vegetation survey is the outcome of an investigation of the islands of the Netherlands Antilles carried out under the auspices of the Foundation for Scientific Research in Surinam and the Netherlands Antilles. The data on which the present study is based were obtained during a trip which lasted from September 1952 until October 1953. During this trip the following islands were visited: Curaςao, Bonaire, Aruba, St. Martin, Saba, and St. Eustatius. A short visit was also paid to the island of St. Kitts (B.W.I.). The present work gives an account of the actual vegetation of the Netherlands Antilles. Other studies, comprising the systematic results and conclusions of the survey, are being prepared, and will possibly be published in 1958.

Description: In my “Notes on the Acanthaceae of Java” (in Verh. Kon. Ned. Akad. v. Wetensch., Afd. Natuurk. 2nd Sect. 45, 2: 29,1948) I discussed the three epithets that had been applied to Rumph’s “Folium tinctorum” after the latter had been transferred to the genus Peristrophe, which, as is well known, was based on this species. Nees, the author of the genus, has used the name P. tinctoria, because he regarded Justicia tinctoria Roxb. as the oldest binomial that had been applied to it. This was contested both by Merrill and by Hochreutiner. Merrill was of opinion that Justicia bivalvis L (1759) was its oldest name, but as I pointed out l.c. this binomial must be regarded as a “nomen confusum”; the description indicates a Dicliptera species, whereas the plate in the “Hortus Malabaricus” and the specimina in Burman’s herbarium to which Linné referred, represent respectively Adhatoda vasica Nees and indeed “Folium tinctorum”. Hochreutiner, on the other hand, thought, that Justicia purpurea L (1753) was identical with Rumph’s plant, but this too proved to be a mistake. J. purpurea belongs, as R. Brown already had recognized, to Hypoëstes. As the binomials proposed by Merrill and Hochreutiner therefore had to be rejected, I accepted l.c. Peristrophe tinctoria (Roxb.) Nees as the correct name. This, however, is also erroneous, for Justicia tinctoria Roxb. itself is an illegitimate name, for which already long ago a legitimate one had been substituted. J. tinctoria Roxb. (1820) is a later homonym of J. tinctoria Lour. (1790). This was recognized already by Schultes (Mantissa 1: 140, 1822), who replaced Roxburgh’s epithet by roxburghiana quoting “ J. tinctoria Roxb., Fl. Ind. ed. Car. et Wall. I p. 124, n. 13 et hoc teste: Folium tinctorum Rumph. Amb. VI 51. t. XXII. f.l” adding “nomen mutandum erat ob tinctoriam antiquissimam Lour”. As Loureiro expressly stated that the plant described by him as J. tinctoria was not the same as “Folium tinctorum” of Rumph, it is clear that J. roxburghiana Schult. must be accepted as the oldest legitimate binomial for the latter. The correct name therefore becomes Peristrophe roxburghiana (Schult.) Brem. n. comb.

Description: In Juni, Juli en September 1955 werden aan de oever van het gedeelte van de Maas, dat door het Juliana-kanaal is afgesneden, resp. door een I.V.O.N.-excursie, de excursie van de Commissie voor het Floristisch Onderzoek uit de K.N.B.V. en ondergetekenden een opvallend groot aantal adventieven verzameld, waarvan een 10-tal nog niet eerder in Nederland was aangetroffen. Door de zeer lage waterstand hadden deze adventieven zich volop kunnen ontwikkelen op plaatsen, waar door het graven van grint vele kuilen waren ontstaan en op de zand- en rolsteenstrandjes aan de luwe zijde van de bochten van de rivier. De zaden en vruchten zijn wel zeker door de Maas aangevoerd van hogerop in het stroomgebied gelegen fabrieken en losplaatsen; de wolfabrieken aan de Vesdre hebben waarschijnlijk een belangrijk aandeel in deze aanvoer gehad. De gevonden soorten zijn voor een groot deel oorspronkelijk afkomstig uit het Middellandse Zee – gebied. Hieronder volgt eerst een lijst van de vindplaatsen en data, daaronder de zo goed als volledige lijst van de aangetroffen soorten. De nummers achter de soorten geven de vindplaatsen aan; de namen der voor de eerste maal in Nederland gevonden taxa zijn onderstreept. Vindplaatsen: (1) Maasoever tussen Obbicht en Grevenbicht; 7-VI, 20-VII, 23-IX-1955. (2) idem bij Meers, gem. Elsloo; 9-VI, 21-VII, 23-IX-1955. (3) idem ten N. van Grevenbicht; 8-VI-1955. (4) idem tegenover Maaseyck; 22-VII-1955. (5) idem bij Uhe en Laak; 24-IX-1955.

Description: Het aantal adventieven, dat wij tot nu toe in Friesland vonden, was zeer gering. Wel was ons bekend, dat in vroeger jaren op de terreinen van de Koopmans Meelfabrieken te Leeuwarden verscheidene (niet gepubliceerde) vondsten waren gedaan, maar het gelukte ons nooit daar enig spoor van terug te vinden. De direktie van de meelfabrieken was echter zo vriendelijk ons mee te delen, dat de graanverontreinigingen vervoerd werden naar het vuilverwerkingsterrein van de gemeente Leeuwarden, gelegen onder Wartena. In de nazomer van 1955 bezochten wij dit terrein voor het eerst en inderdaad bleken hier verscheidene adventieven voor te komen. Dat het terrein tot nog toe aan de aandacht van de floristen is ontsnapt, is ongetwijfeld te wijten aan de ligging. Men kan het n.l. alleen per vaartuig bereiken. Nu ligt het wel vlak in de nabijheid van de prachtige terreinen van “It Fryske Gea” onder Eernewoude, die bezoek genoeg trekken, maar juist dit natuurgebied lokt de floristen veel meer dan het stortterrein. Bovendien is de toegang tot het vuilverwerkingsterrein streng verboden. Wij laten hier volgen een lijst van de in 1955 tijdens twee bezoeken aangetroffen planten. Daar al het vuil van de stad Leeuwarden hier wordt aangevoerd, zal men er ook verscheidene tuin- en sierplanten onder aantreffen. De adventieven zullen practisch alle afkomstig zijn van de Koopmans Meelfabrieken. De graanverontreinigingen worden in gesloten papieren zakken aangevoerd, die op het terrein worden gestort.

Description: Het Instituut voor het Vegetatie-onderzoek van Nederland (I.V.O.N.) werd opgericht in 1930 en is thans gevestigd in het Rijksherbarium, Nonnensteeg 1 , Leiden, Het stelt zich o.a. ten doel om door stelselmatige inventarisatie een overzicht te verkrijgen van de verspreiding der in Nederland voorkomende Pteridophyta en Spermatophyta. Reeds in 1902 werd door de heren Dr. J.W.C. Goethart en W. J. Jongmans, destijds resp. conservator en assistent aan het Rijksherbarium, een aanvang gemaakt motdit biogoo grafische onderzoek. In de jaren daarna werd het met medewerking van een aantal Nederlandse floristen voortgezet, waarna men wegens de toenemende betekenis van het werk en met medewerking van de heren Goethart en Jongmans in 1930 kwam tot de oprichting van het I.V.O.N. Bij de inventarisatie werd tot voor enige jaren – het oorspronkelijke werk werd nl. in 1949 afgesloten – gebruik gemaakt van de Topografische kaart van Nederland, schaal 1 : 50.000, welke ten behoeve van het onderzoek door verticale en horizontale lijnen in vakken was verdeeld van 1045 bij 1250 m. Deze vakken, kwartierhokken genaamd, vormden de eenheden van de inventarisatie. Per kwartierhok werd nl. genoteerd welke planten daarin werden waargenomen, hetgeen gebeurde op excursies in verschillende jaargetijden, waardoor een zo volledig mogelijk overzicht der voorkomende soorten werd bereikt. De zo verkregen gegevens werden vervolgens soort voor soort in albums overgebracht, waarbij ieder album betrekking heeft op een der 62 bladen van de Topografische kaart 1 : 50.000. Tenslotte was het mogelijk om de in de albums vervatte gegevens op een kaart van Nederland te noteren, zodat een overzicht werd verkregen van de verspreiding van de betreffende soorten over het gehele land. Als resultaat werd een serie z.g. Plantenkaartjes van Nederland uitgegeven. Deze kaartjes geven, dank zij de grote volledigheid, die bij de inventarisatie bereikt werd, een betrouwbaar beeld van de verspreiding der plantensoorten. Het ligt in de bedoeling om de publicatie van deze serie Plantenkaartjes zo lang voort te zetten tot een beeld van de verspreiding van alle Nederlandse Pteridophyta en Spermatophyta verkregen zal zijn. In de nog te verschijnen kaartjes zullen daarbij alle gegevens tot en met 1949 verwerkt worden.

Description: He in het vooruitzicht gestelde literatuur-rubriek zal in het volgende nummer worden geopend.

Description: The rapid accumulation of data necessitated the issue of a new bulletin. It was with deep gratitude that I remembered, in the Xmas holidays during which I was compiling this text, the many letters received from various sides expressing appreciation for our enterprise. Editor’s hearts need sometimes a little warming; ours remains distinctly encouraged. Particular encouragement I got from the British Colonial Office which, stimulated by the Government of Malaya, has given a grant to our Foundation to cover part of the travel and accomodation expenses of Dutch collaborators in the United Kingdom, provisionally for two years. This manifest sign of appreciation from the British and Malayan Governments for our work is significant and most gratefully remembered here.

Description: Flora Zambesiaca. On page 413 I have given, unfortunately, an entirely misleading statement on the organization of this planned Flora, which will be a joint effort of the Royal Botanic Gardens, Kew, and the British Museum. There will be two editors of equal status, Mr Exell, of the British Museum, and Mr Brenan, of Kew, with an editorial Committee.

Description: Mr Smitinand, Officer-in-Charge, Section of Botany, Forest Products Research Division, Royal Forest-Department, Bangkok, Thailand, writes, that there is still a large tract of virgin tropical rain-forest in the Peninsula not yet properly explored. An expedition from any foreign country is heartily welcome with cordial co-operation.

Description: Blatter, E. & W.S. Milliard. Some beautiful Indian trees. 2nd edition revised by W.T. Steam. Publ. by Bombay Natural History Society, Bombay, India. March 3, 1955. 8°. i-xv, 1-165 pp., 43 photogr., 31 coloured plates, and text-figures; clothbound. Sh. 30/- net. A simple, illustrated guide to some of the most beautiful flowering trees to be seen in India and Pakistan. It should be of use and interest throughout the tropics as most of the plants treated are grown as ornamentals outside their native country. Thirty nine species have been fully described with accurate synonymy, and notes on distribution, gardening, uses, economic value, vernaculars, domestic uses, medicinal properties, ethnobotany, and ecology of leafshedding, flowering and fruiting seasons. In some cases also closely related species are briefly indicated or described. In appendices descriptions are given of families represented, further a key to the genera, a glossary of some botanic terms, and a bibliography to some sources of further information. An index concludes this very attractive, nicely executed, and relatively very cheap book which is a valuable educative tool to laymen and those interested in gardening in the tropics. It contains much concise adequate information on the plants treated. In a way it is a counterpart to Bor & Raizada’s Some beautiful Indian climbers and shrubs, published by the same Society.

Description: The preparation of a new account of the pteridophytes of the whole Malayan region is a very large undertaking, and when one is at the beginning of it, one cannot foresee what may happen during the course of its execution. It is in part a voyage of discovery. The work will have to be done in stages, and published in parts. To wait until it is all completed, and then to coordinate and re-arrange it before publication, would mean an unreasonably long delay. But to publish it in parts will inevitably mean that one will have new ideas about the early parts as one works on the later ones. My hope is that, when the work is finished, it will be possible to have a new and better conception of the inter-relations of the parts. Present schemes for definition of families for the great majority of ferns are no more than tentative, and that is one reason why I see no need to carry out the work in any pre-arranged sequence.

Description: Bryophyta. The new collections built up during the last years under the supervision of Prof. R. van der Wijk, Groningen, have now all been arranged and provisionally been identified by him and his collaborator Mr Margadant. Revisional work has started. Pteridophyta. A most important collaboration, anticipated for years, is that of doctors Holttum, Kew, and Alston, London, who have now definitely agreed in compiling the series II of the Flora Malesiana containing the account of the Pteridophyta. Dr Alston spent a year (Oct. 1955-Oct. 1954) in Indonesia on the invitation of the Indonesian Government. Dr Holttum has finished his large work on the ferns of Malaya; he is now finishing off an account of the bamboos of Malaya and will then set definitely to the study of Malaysian Pteridophytes. Some limited families will be worked out by both specialists as a sample.

Description: Explanation of the geological map (Northwestern part) of the province of La Coruña, Galicia, N.W. Spain Main rock groups We distinguish five main groups of rocks which probably differ in age. Whether this age difference applies only to the time of their intrusion or metamorphism or also to their sedimentary origin remains obscure. These five groups are from top to bottom in the time scale: — (1) Younger rocks, mostly not tectonized, post tectonic. To this group belong: (a) a red sandstone patch west of Malpica on the coast, unconformable on the underlying schists, age unknown; (b) the Traba granite pluton and some other plutonic rocks south of it; (c) rhyolitic or syenitic dykes south of the Traba granite; (d) a swarm of WNW striking basic dykes, mostly dolerites which are probably older than the Traba granite; (2) A group of intrusive rocks which are partly tectonized and partly not, and often have a porphyritic texture. (a) A group which we call the trondjemetic differentiation series, in the north mostly diorites, in the south gradually losing their content of dark minerals. The rocks often contain very large calcic felspar crystals. (b) A group called the Coruña granite, mostly biotite granite but with pegmatites containing muscovite. (3) A group of basic rocks, covering a large territory forming an arc with liameter of ± 60 km and consisting of gabbros, pyroxenites, serpentines and amphibolites. The coarse gabbros in the centre of its western branch are not tectonized but the omphibolites on its outer margin are often strongly tectonized. (4) A group of rocks containing migmatites, white granites, gneisses, mica schists and even less metamorphic rocks, which we call the Lage group. The muscovite granite of Lage is certainly a syntectonic granite, and is associated with migmatites and micaschists on the one hand and with much less disturbed granites on the other hand. (5) A group of rocks, showing locally a very high degree of metamorphism, which we call the “ancient complex”. It contains hornblende gneisses, amphibolites eclogites, muscovite gneisses, granite gneisses and micaschists, and occupies a long NS trending band. It differs from the Lage complex by the frequent occurence of concordant amphibolites. The relation of these groups of rocks is very doubtful in many cases but we believe that the youngest rocks are Paleozoic and the oldest Pre-Cambrian. The doleritic dykes, striking WNW are often regarded as Mesozoic or even Tertiary (Torre de Assunçao, 1950, 1951) it follows that Traba granite might also be Tertiary and could perhaps be compared to the Cintra granite of Portugal (Torre de Assunçao and Brak-Lamy, 1952) The Lage complex could be compared perhaps with the pre-Ordovician schists which have been called by Teixeira (1954, 1955) the “ante-Ordovician schistograywackes” and are perhaps Pre-Cambrian. Probably our “ancient complex” represents then an even older Pre-Cambrian orogenic cycle. On the other hand the analyses of the Rb/Sr relation (Hoja de Tuy, 1953) indicate that the pegmatites of the Lage granite are either Caledonian or Hercynian in age, as they imply ages vary between a 270 and 350 million years. The analyses are not isotopic however and one perhaps ought not attach too much value to their result. According to the field relation of the Coruña granites and the Lage migmatites or schists there can be little doubt that the Coruña granite is younger. The Coruña granite should then be Hercynian because a Caledonian orogeny is almost unknown in the Iberian Peninsula (Carrington da Costa, 1952). The intrusion of gabbroïc rocks is still more difficult to date. On the one hand it has partly been tectonized on its margin whereas the rocks of the centre are perfectly fresh, but on the other hand they are younger than the schists in which they intruded and the Lage orogeny itself. Provisionally we regard their intrusion as late-Hercynian. In general the structures of this western region of Galicia shows a dominant NS trend, bent in an arc convex towards the west. This convexity has been increased by a set of younger faults striking WNW. The schistosity of the rocks is generally parallel to the trend of their boundaries but exact measurements are mostly lacking. Discordant with the prevailing structures are the abovementioned faults, the doleritic dykes which accompany them and the intrusions of younger granites of the Traba group. Petrology 1. The Traba granite and associated rocks. — This group of rocks occurs only in the eastern coastal section of the province of La Coruña. They form either great batholiths like the Traba and the Pindo masses, or small outcrops closely related to the big batholiths as near Mugía, Leis and Caneliñas. The reddish granite generally contains biotits and Na-K felspar, and has sometimes a porphyritic texture. It never shows any preferred orientation of its minerals. Its direct thermal metamorphic zone is restricted to some tens of meters, but its influence is felt in a much larger region. Everywhere on the sheets 67 and 92 and the western half of the sheets 68 and 93 one finds numerous small stocks and dykes. These dykes consist either of hornblende syenites, fine grained dacites and quartz porphyries. A semicircular dyke system of these rocks suggests a circular zone of subsidence. Another dyke system, which also traverses the fundamental structure of the Galician system, has an approximately E—W trend. These dykes consist either of basic rocks (lamprophyres, diabase porphyries or dolerites), or of light coloured acid, aphanitic rocks. Their age is certainly younger than the Lage granite, which they traverse, and older than the Traba granite which in its turn appears to cut off the dykes. The Traba granite mass contains zones full of thin mineralized quartz veins containing cassiterite, wolframite, molybdenite and monazite. Some large quartz dykes traverse the granite from north to south. 2. The non orientated, homogeneous and porphyritic, late tectonic granites. — This group contains all those granitic masses which appear as rounded hills, which in Galicia are called “penedos”, or occupy large flat surfaces. In general they form large batholiths with well defined boundaries and cause thermal metamorphism in the adjacent rocks, but others are clearly granitizised masses. At the contacts of the latter masses one sees a gradual absorption of the rocks of the “ancient complex” accompanied by a complete reorganization of the elements. The marginal zones coutain numerous xenoliths, distributed without regular orientation, as for instance south of Mugia. When this process of absorption continues the rock becomes homogeneous and a palingenetic granite, sometimes of porphyritic texture like that of la Ruña or Monte Pedrouso, or of homogeneous grain like that of Muros, is the result. The different types are: (a) The biotite-granodiorite of Bayo, (b) The biotite-granite of La Coruña, (c) Porphyritic muscovite granite of La Ruña, (d) Homogeneous muscovite granite of Muros. a. The biotite-granodiorites of Bayo, or rocks of the trondjemitic differentiation series. — These granodiorites form elongated masses concordant with the trend of the “ancient complex” or Lage group. Apparently they have assimilated large tracts of the surrounding rocks. The most basic types contain much pyroxene and hornblende, all of them contain biotite and plagioclase, and in the most acid types the plagioclase predominates. The Bayo mass is some 50 km long and has a width varying between 1 and 5 km. The masses of Santa Comba-Negreira are also elongated in a N—S direction. b. Biotite granite of La Coruña. — In eastern Galicia there are several batholithic granite masses which resemble in many respects those of the Bayo type but cannot be included in the same group because their mineralogy and emplacement is different. They form large plutons which are not concordant with the general trend and find their greatest development in the Cambrian and Ordovician of western Galicia, for instance the Lugo granite described by Barrois in 1881. In our region the Coruña granite belongs to this group, further east we find the batholith east of Betanzos and Curtis and the large batholith of Vivero-Mondoñedo. c. The porphyric muscovite granite of la Ruña. — The Ruña mountain, 640 m altitude, gives typical exposures of these muscovite-biotite granites. The granite consists of large idiomorphic Na-K felspars up to 7 cm with quartz, muscovite and biotite, it does not show any preferred orientation beyond a faint parallel arrangement of the phenocrysts probably due to the intrusion. The mass is clearly discordant with its surrounding rocks and contains large blocks of the augen gneiss of Lage. We suppose that it constitutes a granitization product of the Lage granite, a palingenic granite in situ. Several similar masses occur in west Galicia for instance, in the Pontevedra province and south of Vigo, and also near Friol near Lugo in eastern Galicia. d. The homogeneous muscovite granite of Muros. — This type of granite is very frequent in western Galicia. The name is derived from the occurrence near the district of that name north-west of the ría de Noya. We consider it for the present as closely related to the Ruña type, more homogeneous, but of the same origin. 3. The basic rocks belonging to the “Lopolith”. — The map shows that these rocks form a discontinuous arcuate outcrop some 100 km long in the N—S direction and some 60 km wide. They dip everywhere inwards and are covered by the Ordenes schists, so that the shape of the mass resembles a dish. The petrography of the rocks is very variable, in general we can recognize: 1. Basic diorites with andesine, pyroxene and hornblende. These we find intercalated between the schists of Barrañán (Carballo sheet). 2. An extensive outcrop north of Carballo of ilmenite-rich gabbro rich in alternating with amphibolites. 3. A large mass of fresh looking olivine-gabbro, also with amphibolites, which extends from Mte Castelo to Carballo in an area of some 200 km2. This mass has on its western margin a band of pyroxenites. 4. A large mass of amphibolites east of Santiago de Compostela which contains important mineralizations of pyrrhotite and cupriferous pyrite. 5. A series of outcrops of peridotites, pyroxenites and serpentines on the southern border of the río Ulla, near Bandeira, Las Cruces and Berredo. This outcrop of basic rocks narrows north of the río Ulla and continues to the east of Mellid where it broadens again on the hills of Corno do Boy and reaches the Rías near Sobrado. North of Sobrado it broadens again and the ultra-basic rock reaches Teijeiro. After an interruption of some km the serpentines reappear near Irijoa east of Betanzos and in a small outcrop north of Puentedeume. 6. Finally we find a major outcrop of the basic rocks in the extreme north of the province from Moeche to the Cape of Ortegal, occupying the hills of the Sierra de la Capelada. The cupriferous pyrite mines of Cerdido are situated on their eastern border. We do not know yet the age of these intrusions, which might be older than we suppose now. Neither do we know much about the rocks or their structural circumstances. 4. The migmatitic granite of Lage. — This gneissic granite with two micas occupies a large area in eastern Galicia. The most typical rocks are exposed between the isles of Sisargas and Lage (Schulz, 1835). The texture of the rock is very variable (Expl. sheet Lage no. 43, Tuy no. 261, Oya no. 260), and can perhaps be regarded as an antexitic granite. In the gneissgranite we find parallel zones of migmatized schists and micaschists. Their orientation is roughly N15°E. Along the western margin of the outcrop of the polymetamorphic “ancient complex” these gneisses get an augen structure by the development of large felspatic “eyes” up to 10 cm long, surrounded by biotite perhaps indicating a kind of mylonitization. These gneisses seem to possess two planar structures at an angle of 15° to 20°, one due to the mica orientation, the other to the felspar eyes. The Lage gneisses differ from the “ancient complex” gneisses by the absence of parallel basic bands. 5. The “ancient complex”. — A narrow zone of highly metamorphic rocks extends from Malpica (sheet 44) in the north to the ria de Arosa (sheet 152) in the south. This zone of 80 km length and roughly 6 km wide is slightly convex to the west. The most typical rock is a glandular biotite-felspar gneiss, but we find also gneissic mica schists and other varieties. In the centre, between Baiñas and Mazaricos the gneisses contain riebeckite. The whole complex contains numerous parallel narrow zones or dykes of very much tectonized basic rocks, amphibolites, pyroxenites and eclogites. The fact that these rocks show a higher grade of metamorphism and often are polymetamorphic as compared to the Lage group induses us to believe them to be older. Mineralogically these rocks are characterized by the instability of their micas, biotite and muscovite, and hornblendes. The first group is often found as much deformed relics. Only in the perhaps younger riebeckite gneiss intrusions the hornblende is more stable and uniformly developed. Near Malpica biotite gneisses with some muscovite predominate, near Puenteceso and Zas biotite-hornblende gneiss and near Baiñas and Mazaricos riebeckite gneiss. Near Noya the biotite gneisses deappear. The basic rocks have their greatest development between Zas and Mazaricos. Inside the complex we can suspect many faults bringing zones of different grades of metamorphism in contact. It seems quite probable that similar zones of highly metamorphic character exist also elsewhere in Galicia. We suppose for instance that the riebeckite granite an dgranite-gneiss east of the Monte del Carrio and those of Silleda in Central Galicia belong to the same group. Perhaps the Ordenes schists of a much lower metamorphic grade above the basic rocks described before, belong to the same group. Conclusion Perhaps the complicated skeleton which we have presented here as an explanation of our map, and which is the result of numerous excursions in Galicia during recent years can be summarized in the following table: Age of orogeny Mock groups Deformation; genesis Petrographical type Alpine Traba none intrusion Traba granite Bardullas syenite Rhyolitcs Hercynian Muros weak granitization Bayo diorite Coruna granite Runa granite Maros granite t Lopolith .' Basic rocks Huronian — 800 m.y. Lage intense migmatization Granite-gneiss of Lage Augen granite of Cabrai Archean — 1200 m.y. Malpica (ancient complex) very intense migmatization Penedo granite Borneiro gneiss Baiñas gneiss Metamorphic basic rocks The correlation of the rock-groups with known orogenic periods is of course very doubtful. The reader must realize that we give this outline only in order to stimulate further research.

Description: It can hardly be denied that the expression “General Plant Morphology”, which is so often met with in botanical textbooks, has little or no meaning. A general morphology of the Plant Kingdom would have to occupy itself with those morphological features that are common to all groups of plants, which means that it would have to confine itself to the common features of the cell structure and eventually to such peculiarities as are independent of the uni- or pluricellular structure of the plant body, e.g. its enclosure within a rigid envelop. However, when we realize that there is in this respect no fundamental difference between the common features of plants and animals or, at least, of some groups of animals it will be clear that the use of the expression “General Plant Morphology” is misleading and should be avoided. What in most botanical textbooks is understood by “General Morphology” is not a morphology of the whole Plant Kingdom but only of a part of it; however, the delimitation of this part, and this is a most astounding feature, is but seldom explicitly indicated, and, moreover, proves to vary, sometimes even in different chapters of the same work. Most textbook-writers seem to agree that Algae and Fungi have a morphology of their own, and that the latter should be left to specialists in these fields; they accordingly restrict their attention either to the Embryophyta, i.e. the group which comprises the Bryophyta and the Vascular Plants, or to the Vascular Plants alone.

Description: In the course of examination of specimens in the fern collection of the Botanisch Museum en Herbarium, Utrecht, the senior author discovered a specimen of Doryopteris that seemed to be different from any species treated in the junior author’s revision of the genus. Further examination has proved this to be the case and it is here described as new. DORYOPTERIS conformis, spec. nov.

Description: The list of Marantaceae published by PULLE (1906) comprises 20 species belonging to 6 genera, the largest genus being Calathea with 8 species. It was found, however, that one of the species does not belong to the family: investigation of the type of Calathea strobilifera (Miq.) Koern., viz. Kegel 1469 [GOET], showed that it pertains to Renealmia strobilifera Poepp. et Endl. (Zingiberaceae). The record of another species, Calathea allouia (Aubl.) Lindl. appeared to be based on a misidentification: the collection Focke 893 cited under this name by PULLE (1906) belongs to C. grandis O. G. Peters. Later on PULLE (1909) recorded the occurrence of one species more of this family in Suriname, viz. Myrosma polystachya Pulle, a new species. Since then no further additions to the list of Suriname species have been published. Our investigation of the Suriname material showed the occurrence of 33 species belonging to 8 genera. In the following pages a few taxonomic and phytogeographical remarks are made on some of these genera and species; they also contain the description of a new genus.

Description: Dit Correspondentieblad stelt zich ten doel het contact te bevorderen tussen hen, die zich bezig houden met floristisch en plantensociologisch werk. Het wil de Nederlandse floristen en plantensociologen, zowel amateurs als vakbiologen, in staat stellen elkaar op vlotte wijze van hun vondsten of denkbeelden op de hoogte te brengen en zich op een gemakkelijke manier met vragen of verzoeken tot elkaar te wenden. Verder wil het trachten hen op de hoogte te houden van nieuwe literatuur, die voor de floristiek en het vegetatieonderzoek van belang is en van andere zaken, die hun belangstelling kunnen hebben. Het zal daartoe bevatten korte mededelingen van floristische en plantensociologische aard, beknopte excursieverslagen, opgaven van nieuwe literatuur, personalia, een vragenrubriek, aankondigingen van vergaderingen en excursies e.d.

Description: Op 3 Sept. jl. overleed te Deventer Dr. H.R. Hoogenraad, oud-leraar aan de Rijkskweekschool voor Onderwijzers aldaar. Zijn herbarium werd door Mevr. M.M. Doornink-Hoogenraad te Zutphen aan het Rijksherbarium geschonken. Het bevat naast buitenlands materiaal (uit W. Europa) ook een groot aantal Nederlandse planten, o.a. exemplaren van Thesium pyrenaicum Pourr., afkomstig van de enige, thans verdwenen, vindplaats bij Gorssel. De heer N.P.W. Balke te Rotterdam schonk zijn collectie Nederlandse planten aan het Rijksherbarium. De collectie is vooral van belang door het groot aantal adventievens dat zij bevat.

Description: The year of publication of the volumes can be found in the Centennial Review of the Asiatic Society of Bengal 49 (1885). Hamilton, Fr., Commentary on the Hortus malabaricus. This was published in the Trans. Linn. Soc. Lond., the four parts respectively in l.c. 13 (1822) 474-560; ibid. 14 (1824) 171-312; ibid. 15 (1826) 78-152; ibid. 17 (1835) 147- 252.

Description: Akademi Biologi, Bogor. The Indonesian Government is anxious to develop training in biology; the failure of the University of Bandung Faculty to achieve this (due to shortage in staff personnel) has necessitated making temporary use of the personnel of the Kebun Raya Indonesia towards this goal. With freedom of choice and with an extra-allowance, a number of staff members of K.R.I, has agreed to give each a few lectures at the Akademi Biologi, Bogor. The course is intended to last 3 years, when a degree can be obtained which is in standing assumed to be slightly under a bachelor’s degree. Personnel thus raised will be partly required for the Gardens, partly for teaching purposes in secondary schools; each year a few excellent students will be selected to go abroad for special training in scientific botany or zoology. Out of 300 candidates 30 have been selected. They are accomodated temporarily in the buildings of Tjibodas mountain gardens where lessons are given. Oct. 10, 1955, the Akademi Biologi was officially installed by H.E. the Vice-President Dr Moh. Hatta, and the Minister of Agriculture H.E. Moh. Sardjan. Buitenzorg Fund. Dr H.P. Bottelier, Utrecht University, who had been awarded the grant of the Netherlands Buitenzorg Fund for 1954 has, on the invitation of the Indonesian Government, prolonged his half year’s stay and has acted as Professor of Botany in the Faculty of Agriculture at Bogor for an additional year; he returned to Holland Jan. 1956.

Description: Barrett, C.: Wild life of Australia and New Guinea. 229 pp., ill., 1955. Describes in a fascinating and not too technical manner the life stories of animals of Australia, New Zealand and New Guinea. Bor, N.L.: Manual of Indian forest botany. 441 pp. A systematically planned treatise with keys to the genera and species to be found in India and Burma, with descriptions of their economic uses.

Description: THE GOLD DEPOSITS IN SURINAM AND THE DISTRIBUTION OF CONCESSIONS THROUGH THE COUNTRY The fieldwork on the occurrence of primary and secondary gold deposits in Surinam on which this thesis is based was carried out by order of the Welfare Fund Surinam (Welvaarts Fonds Suriname) during the periods December 1950—September 1952 and September 1953—January 1954. The regions investigated form part of Surinam (formerly Dutch Guiana), South America. These regions are indicated by heavy lines on the enclosed geological survey map of Surinam, after Schols and Cohen (1953) and IJzerman (1931). As participant of a medical scientific expedition to the southern borderlands of Surinam, I made investigations on the occurrence of gold in this part of Surinam. The trail of the expedition is indicated on the survey map of Surinam (enclosed map). As was stated by statistical (figure 4) and by field evidence, the goldfields of Surinam occur in the northern and eastern part of the country, south of the coastal plain. The goldfields are geo-topografically connected with an area of metamorphic sedimentary schists (Orapu-Formation and Bonnidoroseries) and, mainly epimetamorphic, basic to intermediate volcanic rocks (Balling-Formation without Bonnidoro-series). Two belts of relative concentration of goldconcessions can be constructed from the distribution of the goldconcessions through the area where the goldfields are found. Most of the workable deposits are alluvial or colluvial placer deposits, but in some places in Surinam, primary deposits of hypogene origin are worked. Here the gold is found in gold-bearing quartz veins, -veinlets and -lenses, and in gold-bearing pyrite, which is limonitised as a result of weathering, and which occur in the metasomatically altered wall rock along, as well as in, some of the goldand pyrite-bearing quartz veins and -lenses. These primary deposits, being the result of hypogene processes which are genetically related to intrusive quartzdiorites and granites, occur in the invaded bedrock of the Balling-Formation (Headley-Reef, Km 124,3 L. S., figures 21 and 22) and the Orapu-Formation (Mindrinetti goldfields, Km 93—106 L. S., figures 22 and 25). The placer gold in the alluvial and colluvial deposits of the mentioned areas must be considered to be the concentrated debris of the gold-bearing quartz veins and -lenses, as a result of mechanical transport from chemically weathered, enclosing bedrock. This is in contradistinction with earlier theories of Middelberg (1908), who thinks the placer deposits a result of mainly chemical transport by the help of supergene solutions. Transport of gold by supergene solutions as a result of weathering under most favourable conditions (Bateman, 1949) in the presence of limonitising pyrite, has occurred in some cases over short distances only, from the pyrite to the surrounding matrix. Mostly however the limonitised gold-bearing pyrites are still gold-bearing (table 9). As a process of concentration of placer gold those supergeneous processes are very unimportant. As was stated earlier by Gruttebink and de Haan (1940, 1950, 1952) and as could be reascertained during our fieldwork in the concessions of the Sarakreek Goudvelden N.V. on the upper course of the Lawa river, the placer gold is also the concentrated debris of quartz veins and -veinlets. The same holds good for most of the other investigated areas, i. c. the concession Ettenberg opposite Stoelmanseiland (survey map) and probably the concession Doorson on the southern slope of the Nassau mountains (figure 12). On the other hand in the investigated area of the Kabalebo river near Stone creek (figure 35) the conglomerates of the Orapu-Formation must be regarded as the possible sourcerock of the scarcely scattered gold in the gravels, mostly formed by quartz pebbles from the conglomerate outcrop, at a distance of some tens of metres upstream the creek. This gold shows signs of long-distance transport, because of its roundness (figure 67 e). Workable deposits of this type are not known in Surinam. The gold from the workable placer deposits was not transported over long distances from its source deposit. Therefore the geology of the underlying bedrock of the placer deposits is an important source of information with respect to the genetic relationship between the occurrence of gold and the processes of primary mineralisation, even if the primary gold deposits are not known or hidden by the result of chemical decay of the deposits and their enclosing bedrock. The genetic relation between gold in placer deposits and gold bearing quartz veins is proved by the occurrence of gold-bearing quartz pebbles in the gravels, whereas the geological processes that caused the mineralisation arc detected by the coincidence of the distribution of the placer deposits and contactzones between the Balling-Orapu-Formations and younger intrusive granites and quartzdiorites. The primary deposits have already been found or must be sought for in the invaded bedrock of the Balling- and Orapu-Formation, in the direct contact aureoles of the quartzdiorites and granites (figure 12) or at a certain distance from the outcrops of the contacts, but seldom further than 2000 m (figure 16). In the case of the Mindrinetti-goldfields (figure 25), the placer and primary deposits are concentrated on both sides of a savannah area. This savannah area consists of the weathered products of contact metasomatieally altered schists and conglomerates of the Orapu-Pormation (Grosgroup). The contact metasomatieally altered schists and -conglomerates are here considered as the contact aureole of a hidden granitic intrusion, comparable to the granite of Km 109 L. S. (figure 26). The gold-bearing hypogene deposits don't occur in the direct contactzone, but at a short distance from there, not exceeding 2000 m, along shear planes and minor faults. Study was made of the type of granites and quartzdiorites that caused mineralisation, because igneous rocks of the same mineralogical composition are found in the southern and western part of Surinam, where as far as known, workable gold deposits are not found. The granites and quartzdiorites in this part of Surinam are formed as large migmatite-granite complexes of an inhomogeneous mineralogical composition over short distances (de Munck 1953, IJzerman 1931). Because most of the Surinam granites belong to this type, the chemical analyses of the granites represent mostly granites of this migmatite-granite type. In the QLM-diagram (P. Niggli 1945) it can be seen that they belong to the pacific province (calc-alkali magma), but they are very irregularly distributed in this diagram (figure 44). There is a shifting of the plotted analyses to the side of sedimentary rocks, probably meaning that the analyses represent igneous rocks which assimilated a lot of material from the invaded rocks of a different chemical composition. These granites are interpreted as being formed by granitisation. The granitic and quartzdioritic magmas which caused gold mineralisation are characterised by their homogenity, chemically as well as mineralogically, over short and long distances. Their contacts are well marked, either by xenolith's (figure 12) or by zones of marked contact-metasomatism (Grosgroup, figures 22 and 26). Four chemical analyses of quartzdiorites which are genetically related to gold mineralisation were made. The result of the analyses are published in table 2. The analyses are plotted against the analyses of other quartzdiorites (figure 45). The same has been done for the granites. The granite of Km 109 L. S. represents an extremely acid granite (granitaplite). These granites and quartzdiorites are interpreted as real intrusive granites. As the quartzdiorites from the concessions on the upper course of the Lawa river are porfiritic, they have a double sequence of crystallisation. The gold deposits of the SE—NW goldbelt of Surinam (figure 4) and those of the concessions Ettenberg (survey map) and Doorson (figure 12) are genetically related to the intrusive quartzdiorites. The same quartzdioritic complex that causes mineralisation on the concession Doorson has been found discordantly covered by the Orapu-Formation (Schols and Cohen 1953). The conglomerates and schists of the Orapu-Formation were never seen to have been intruded by quartzdiorites. The granites of Km 109 L. S. are intrusive into the Orapu-Formation. This proves that granites and quartzdiorites of different age do occur and makes it probable, that both can have caused gold mineralisation. The quartzdiorites (granites no. 1) are supposed to be older than the granite of Km 109 L. S. (granites no. 2). The SE—NW goldbelt of Surinam is genetically related to the granite no. 1 (quartzdiorites); the B—W goldbelt of Surinam to the granite no. 2 (granite of Km 109 L.S.). For both goldbelts we can give the same sequence of events causing workable gold deposits. Only in the Mindrinetti-goldfields and near Km 124,3 L. S. (Headley-Reef) workable primary deposits, as a result of hypogene processes, are known and here have been studied especially, whereas the placer deposits on the upper course of the Lawa river and in the alluvial deposits of this river and the Marowyne have been studied especially there. As a result of the fieldwork and laboratory investigations we can subdivide the different types of gold-bearing deposits into the following groups. A. Secondary deposits 1. Deposits formed as a result of mainly mechanical transport a. Alluvial deposits. b. Colluvial deposits. 2. Deposits formed as a result of mainly chemical transport a. Residual deposits. b. Gold-bearing, deeply weathered bedrock. B. Primary deposits as a result of hypogene processes 1. Gold-bearing quartz veins, -veinlets and -lenses. a. Gold- and pyrite-bearing quartz veins. b. Gold-bearing blue quartz veins. c. genetically related, not gold-bearing turmaline-quartz veins. d. Gold- and ferberite-bearing quartz veins. e. genetically related, not gold-bearing white quartz veins. 2. Gold-bearing bedrock. a. Gold-bearing pyrite in metasomatically altered wall rock of the gold- and pyrite-bearing quartz veins. b. Gold-bearing bedrock. a. dolerites. p. granites. y. conglomerates. The workable gold deposits in Surinam must be considered to be the result of a genetic sequence of events from intrusive granites or quartzdiorites which intruded older rocks of the Balling- or Orapu-Pormation, causing goldbearing quartz veins and gold-hearing pyrites in the wall rock, which has often been altered contact-metasomatically. The placer deposits are formed from the debris of these primary deposits, mainly as a result of mechanical transport. A. SECONDARY DEPOSITS 1. Deposits formed as a result of mainly mechanical transport Most of the workable gold deposits in Surinam are of this type. The gold occurs in these placer deposits as flour gold (up to 0,1 mm), dust gold (0,1—0,5 mm) and coarse gold (more than 0,5 mm). Nuggets too occur and are called “pepieten”. The gold is marked by irregular forms, flakes and fine specks. Grutterink (1940) described some large nuggets from the concession area on the upper course of the Lawa river and states a hypogene origin of these nuggets, because chalcopyrite was found as inclusions in the gold. Morphologically the gold from the placer deposits is sharp-angular to subrounded (figure 67). Gold-bearing quartz pebbles often occur in this type of deposits. These pebbles are also sharp-angular to subrounded. More seldom fully rounded quartz pebbles occur. This proves that the transport of the gold and the gold-bearing quartz did not occur over long distances. a. Alluvial deposits The alluvial deposits can be subdivided into a. recent alluvial deposits; ß. terrace deposits. a. Recent alluvial deposits are the most common type of workable gold deposits in Surinam. The gold occurs in one or more layers of the deposits, mostly concentrated in the gravel-bottomlayer, on a kaolinitic-weathered bedrock. Examples of this type of deposits are illustrated by the figures 15, 17, 18, 23. Figure 15 represents an alluvial deposit of the Lawa river, opposite Stoelmanseiland. The deposit consists of gold-bearing sands and gravel on a kaolinitic-weathered quartzdioritic bedrock. Fine and coarse gold occurs in the gravel layer. The gold has irregular subrounded forms. Nuggets do not occur in this place. Gold-bearing quartz pebbles are found in the gravel layer. Some 1500 m upstream the river, the contact between quartzdiorite and the Balling-Formation is hidden by swampy lands and the Lawa river. In the Balling-Formation many quartz veins occur. According to the concessional, nuggets (0,5—10 grams) have been found in the area of the Balling-Formation, which is marked by more accidentated lands and ferritic weathering. So the primary deposits must be sought in this area of the Balling-Formation. Figures 17 and 18 illustrate the morphology of the gravel-covered bedrock and the distribution of goldconcentrations in the Bas Rufin (figure 16). Here the gold occurs in a gravel-layer of an average of 70 cm, resting on a kaolinitic-weathered bedrock and covered by layers of sands and clays of 2—3 m. The workable deposits are found in the bottom layer of the gravel and the first 2 or 3 cm of the weathered bedrock. Here the gold is found as fine and coarse gold, together with gold-bearing quartz pebbles and irregularly formed nuggets with rounded and subrounded forms and platy sharpangular nuggets weighing up to several tens of grams and not showing any results of transportation. In the weathered bedrock under these gravel layers, gold-bearing quartz veins occur. This proves that the gold from these deposits has partly been transported over short distances, whereas soms of the gold has to be considered as eluvial. Figure 23 shows a section, situated on the borderline of the savannah area and the hills of the gold bearing zone of De Jong Zuid and Gros Placer (figure 25). Here the gold-bearing deposits consist mostly of material of the gold-bearing zone, whereas the colluvial deposits of the savannah area prove to be barren of gold. The morphology of the gold, found in these deposits, is subrounded. ß. Terrace deposits, in Surinam prospection, is the name given to all gravel deposits above creek- or river level. Deposits of this type are illustrated by figures 5, 6, 7, 17, 18. Figures 5, 6, 7 reproduce a type of terrace deposit found in the Marowijne river. At main waterlevel, in the river and along the banks of the river we find cemented riverconglomerates, which rise up to 2 meters above waterlevel. The quartz pebbles of the conglomerates (2—20 cm) are perfectly rounded. Along the banks they are covered by sands and clays. Some of the islands (tabbetjes) in the river are the remains of older riverbank terraces (Nason). The conglomerates proved to bear a small amount of gold. The fine gold has irregular rounded forms. Deposits of this type are not worked in Surinam. Another type of terraces is found in the valleys along the creeks on the upper course of the Lawa river. This type is illustrated by figures 17 and 18. The gold in these terraces has the same morphology as the gold in the recent alluvial deposits. The terraces represent an earlier stage of the creek, which carved a valley in preexisting rocks. The terrace deposits are characterised by their topographical height above creek level and by their more ferritic appearance as a result of weathering processes above water level. Sometimes the gold in this type of deposits occurs together with limonite. b. Colluvial deposits The colluvial deposits link together the alluvial deposits of the type A. 1. a and the primary deposits of the type B. They are characterised by yellow and redbrown sandy granular clays with angular gold and quartz fragments and often ferritic iron stones. The deposits represent the slightly transported debris which resulted after the lateritic weathering of the underlying bedrock. They are transported as a result of creep and of the removal of large volumes of peliticweathered bedrock by erosion. The occurrence of quartz fragments and free gold with angular morphology in this type of deposits proves that in most instances the chemical weathering did not affect the gold to an important degree. In some cases gold-bearing limonitised pyrite is found in this type of deposits. Sometimes the colluvial deposits form a foothill plain. The colluvial deposits are affected by chemical weathering, resulting in the formation of so called “kraskouw” layers. This kraskouw, being a stage of ferritic weathering of transported material above water level, occurs in the clays of the terrace deposits too. Kraskouw is characterised by its irregular reticulated ferritic enrichment and pore-space filling by clay matter. Figures 19 a. b. c. illustrate some types of colluvial deposits. Figure 19 a represents the most common type of colluvial deposit. The clay matrix of the upper layer is washed out by erosion, by which the layer has undergone enrichment in quartz fragments and iron stones. The lower layer has more pelitic contents but also belongs to the colluvial deposit transported by creep, because quartz-fragments and gold occur, whereas the underlying bedrock does not show quartz veins. Figure 19 b illustrates colluvial deposits which cover an older terrace deposit. Kraskouw has been formed in the colluvial layers. Figure 19 c represents a deposit that has been considered as a result of filling of a creek valley with residual quartz boulders, by mainly colluvial deposits. The quartz boulders, measuring up to several cubic feet, are subrounded to angular. In this type of deposit, nuggets have been found with sharp-angular platy forms, which prove that the nuggets were formed as a result of fissure filling from gold-bearing solutions of hypogene origin (Grutterink 1940). 2. Deposits formed as a result of mainly chemical supergene processes Deposits of this type have not yet been carefully studied in Surinam. Some random observations prove the existence of this type of deposits but nowadays no workable deposits of this type are known in Surinam. These deposits seem to be a consequence of the weathering processes in primary and secondary gold deposits. They result into: a. Residual deposits. b. Gold-bearing, deeply weathered bedrock. a. Residual deposits Residual concentration of gold in the ferritic final members of the lateritic weathering of gold-bearing deposits in the form of gold-bearing quartz fragments and free gold, belongs to the type already discussed as colluvial deposits. Beside this type of residual concentration there is also another type which probably is a result of the above mentioned processes. Here the ferrites themselves are gold-bearing as was proved by van Kooten (1953). Assays of ferrites above the gold-bearing deposit of Pakira Hill (De Jong Zuid) showed a grade of 2,5 g Au/ton. b. Gold-bearing, deeply weathered bedrock Probably a piece of gold-bearing clay, which was found in the kaoliniticweathered bedrock under the gravel layers of the Rufin (figure 82), belongs to this type. The morphology of the gold and the distribution through the clay prove it perfectly impassible that this gold is placer gold, which penetrated mechanically into the clay. There is always a possibility that the gold was already formed in the unweathered bedrock by hypogene processes but this doesn't explain the clayey-weathered bedrock that is enclosed in the gold. To a certain degree some results of the limonitic weathering of gold-bearing pyrites in the quartz veins and in the contact-metasomatically altered wall rock along these veins also belong to this type, which will be treated together with B. 1. a., because the deposits formed in this way are mainly formed by hypogene processes. B. PRIMARY DEPOSITS, AS A RESULT OF HYPOGENE PROCESSES Primary deposits are only worked in the environment of the country railroad between Km 93 and Km 133. These deposits were studied especially, although here too, placer deposits of the same types which have already been discussed, are more important as contributors to the gold production of Surinam than the primary deposits. Two types of primary deposits can be distinguished. The first type is that of the Mindrinetti-goldfields and can be found in several zones on both sides of the savannah area of figure 25, between Km 99,5 and Km 105,5 L. S. (country railroad). The second type occurs near the contact of the Kabeltonalite (figure 22). The primary deposits of the Mindrinetti-goldfields lie in deeply-weathered, contact-metasomatically altered wall rock which consists of (sandy-) kaolinitesericite-quartz-bearing clays (figure 31). Often limonitised pyrite occurs in the contact zones along gold-bearing quartz veins. The kaolinitic-weathered contact-metasomatically altered wall rock is distinguished from the normal regional-epimetamorphic schists and conglomerates of the Orapu-Formation, by its colour, which is often white or a pastel shade of rose, violet, yellowbrown and redbrown; by its often high kaolinite percentage (table 5, column VI); by its unconsolidated pelitic character (table 6 and figure 50), conglomeratic relicstructure and its topographic position along goldbearing quartz veins. The normal epimetamorphic conglomerates and schists of the Orapu-Formation are weathered to a smaller degree and are still consolidated rocks. Lateritic weathering of these rocks results in the formation of ferrites which occur in the colluvial deposits on the tops and the slopes of the bills. The weathering products of the Grosgroup (figure 22) are characterised by the same weathering features as the contact-metasomatically altered rocks along the gold- and pyrite-bearing quartz veins, but here limonitised pyrite, nor gold occur. The unconsolidated sandy kaolinite-sericite-quartz clays change into the consolidated conglomerates and schists of the Orapu-Formation, loosing their pelitic character and later on their non-ferritic weathering. As was proved by two drillings into the unweathered parts of this contact-metasomatically altered bedrock, which were located by reason of the results of the laboratory investigations on the weathering products, the contact-metasomatism resulted in important changes of the mineralogy and chemistry with respect to the epimetamorphic schists and conglomerates of the Orapu-Formation. Mineralogically the contact-metasomatically altered rocks of the Grosgroup (figure 25, WFI) consist of chlorite- and calcite-bearing epidote-sericite-albitequartz schists, whereas the regional-metamorphic schists of the Orapu-Formation consist only of (chlorite-, chloritoïd- and plagioclase-bearing) sericite-quartz schists and -conglomerates. The contact-metasomatically altered wallrock of the gold-bearing zone of Pakira Hill (De Jong Zuid, LB 65) consists of a biotite-bearing quartz-sericiteepidote-albite rock. Table 4 shows the estimated mineralogical changes caused by the contact-metasomatism. The process of contact-metasomatism mineralogically results in the formation of albite and epidote mainly and also of calcite in the rocks of the Grosgroup and of biotite in the rock of the Pakira Hill. Chemically the contact-metasomatism is characterised by the supply of soda and lime into the schists and conglomerates of the Orapu-Formation, which form albite and epidote in a first stage, synchronous with desilicification of the pre-existing conglomerates and schists; whereas in a later stage carbonatisation and silicification occurred. This stage of silicification was found in the drilling WF I. Here small quartz and calcite veins cut through the newly formed albite (figure 46). In the drilling LB 65 only the first stage was found. Possibly the equivalent of the second stage of the contact-processes here can be found in the gold-bearing quartz veins. It seems very probable that the processes, which caused contact-metasomatism and those which caused gold mineralisation and quartz veins, are genetically related and that both result from the intrusion of a hidden granitic intrusion which exists under the savannah-area (figure 26). It is probable that the residual solutions which escaped from the intruding magma, reacted with the invaded bedrock. As a result of the reactions with the invaded bedrock an exchange of elements occurred, whereby the residual solution became more concentrated with Si02, whereas the invaded rock became enriched in sodium and calcium. The contactmetasomatism of the Grosgroup is here interpreted as a result of diffuse processes, whereas the gold-bearing quartz zones are the results of more concentrated solutions, which acted along shear planes and minor faults. The figures 51 and 52 illustrate the relative supply and removal of the elements, joined into groups si, al, fm, c and alk after P. Niggli (1945). In figure 51 the removal and relative concentration of elements from contactmetasomatically altered rocks to their weathering products is shown and in figure 52 the relative supply and removal from the epimetamorphic subgraywacke (WB III) to the contact-metasomatically altered rocks of the drillings WF I and LB 65 and then to the weathering product of LB 65 is shown. Figure 53 illustrates the same supply and removal of the elements on the supposition that Al2O3 was supplied nor carried off during the processes. The analyses are compared by the same calculated atom equivalent of 282 for ½(Al2O3). 1. Gold-bearing quartz veins, veinlets and lenses Figures 25 and 26 show the relations between granites, zones of contactmetasomatism and the gold-bearing and related quartz veins, as they were interpreted by field evidence and laboratory studies. Along the northern boundary of the savannah-area (De Jong Noord) five zones of gold-bearing and genetically related quartz veins are found. Each zone is characterised by its own paragenesis of the quartz veins which usually strike in a similar direction and occupy a certain area. The gold-bearing deposits occur as separated groups of quartz veins and -lenses, called reefs (figures 27, 28, 29 and 30). Thus a zone has several reefs, characterised by the same paragenesis. Every reef consists of several quartz veins and -lenses either with the same paragenesis (De Jong Noord) or of more types of quartz veins and -lenses each with their own paragenesis (De Jong Zuid). Five types of paragenesis are distinguished, being: a. Gold- and pyrite-bearing quartz veins. b. Gold-bearing blue quartz veins. e. genetically related, non-gold-bearing turmaline-quartz veins. d. Gold- and ferberite-bearing quartz veins. e. genetically related, non-gold-bearing white quartz veins. This subdivision is made of the quartz veins in the Mindrinetti-goldfields but holds good for the other concession areas too, i. c. the concessions on the upper course of the Lawa, the concession Ettenberg opposite Stoelmanseiland, Headley-Reef near Km 124,3 L. S. and Concession Doorson on the southern slope of the Nassau mountains. Some other types of paragenesis are found on these concessions but they are of secondary importance with respect to the gold-bearing primary deposits. Not all types occur on the same concession. Type d was found only at one place in Surinam (Pakira Hill, De Jong Zuid). a. Gold- an pyrite-bearing quartz veins The gold- and pyrite-bearing quartz veins are the most common and most easily discovered type of primary gold deposit of the Mindrinetti-goldfields. Here they are characterised by contact zones of metasomatically altered wall rock, as was described before. This wall rock has been altered by weathering into kaolinitic-clay and often shows schistose- or conglomeratic relicstructures. Gold-bearing, limonitised pyrite often occurs in this wall rock. Figures 27, 30 and 31 show sections through the gold-bearing primary deposits of this type, whereas figure 25 shows the distribution of the zones where reefs of this type occur (reefs marked P.). Assays of the quartz are given in table 8. Table 9 shows assays of goldbearing, limonitised pyrite from the wall rock of the quartz veins of this type. The gold occurs scattered through the quartz between the boundaries of grains and in cracks of the quartz. Gold also occurs in the surrounding matrix of the limonitised pyrite, which has been impregnated by iron oxides and hydroxides (figures 57 and 58). Here it appears as fine specks or sometimes as flaky gold in the crystal-negatives of completely-weathered pyrite. Figures 59 and 60 show the stages of weathering of the pyrite. The white parts of figure 60 are the non-weathered pyrite, surrounded by low reflecting material (limonite I). The dark grey parts further away from the pyrite also consist of limonite (limonite II). The light-grey parts represent the final stage of the weathering of the pyrite. They consist of hematite. Macroscopically visible gold is seldom encountered in these gold-bearing limonitised pyrites. One sample of the last mentioned type was presented to me by the Sarakreek Goudvelden N.V. for laboratory investigations. The figures 61 and 62 show the morphology of the gold (white) in the limonitised pyrite (grey). This morphology is considered to originate from the weathering processes of the limonite and as a result of transportation of the gold by supergene solutions. Beside gold-bearing, limonitised pyrites and gold-bearing quartzes which result from the weathering of the pyrites, primary gold of hypogene origin occurs in the gold-bearing quartz veins of this type of deposits. Figure 64 shows the outlines of primary gold from these quartz veins. As a result of limonitic-weathering of gold-bearing pyrites in the wall rock of these quartz veins, limonite and hematite walls occur which enclose the veins. Secondary enrichment has occurred on the boundary between the limonite-hematite and the quartz. Here the gold has been concentrated as a result of supergene processes. These gold-bearing limonite-hematite walls along the quartz veins are known as """"tjaps"""" in Surinam. The supergene processes however didn't contribute to the amount of gold of the gold-bearing deposits as a whole. Only slight transport and concentration over a distance measurable in cm's, resulted from these supergene processes. Of course it is possible that relative concentration occurred by carrying off of other formerly existing minerals. b. Gold-bearing blue quartz veins Gold-bearing greyblue, blue and blueblack quartz veins occur in the goldfields of Surinam. They were studied especially on De Jong Noord (figure 25), De Jong Zuid and on the concessions on the upper course of the Lawa river. One specimen of an extremely deep blueblack colour proved to enclose millions of semi-opaque inclusions. The walls of the inclusions are coated by particles of solid matter, whereas the content of the inclusions consists of liquid- and gaseous CO2. By concentrating the solid matter from the inclusions, through treatment of the quartz with HF, and by X-ray analyses of the thus obtained concentrate, the solid matter which causes the colour of the blue quartz was proved to be graphite. Primary gold of hypogene origin was studied in a specimen of bluegrey quartz from the concessions on the upper course of the Lawa river. The gold is irregularly distributed through the quartz (figure 65) and contains inclusions of three different minerals beside quartz, which is replaced by the gold (figure 66). One of the included minerals is probably chalcopyrite, which possibly encloses valleriite. The blue quartz veins on De Jong Noord are not characterised by contactzones of kaolinitic-weathered, metasomatically altered wall rock. On De Jong Zuid this type of quartz vein occurs together with the gold- and pyrite-bearing type of quartz veins in a zone of strongly contact-metasomatically altered and later weathered wall rock. Here they are probably younger than the gold- and pyrite-bearing quartz veins because they change into turmaline-bearing blue quartz veins as a transition between the gold-bearing blue quartz veins and the non-gold-bearing turmaline-bearing white quartz veins. e. Genetically related, turmaline-bearing white quartz veins On De Jong Zuid the quartz veins of this type are certainly younger than the gold- and pyrite-bearing quartz veins, because they cut through these veins. On De Jong Noord two zones of non-gold-bearing turmaline-quartz veins border the zones of gold-bearing quartz veins. d. Gold- and ferberite-bearing quartz veins Ferberite was found at only one place on De Jong Zuid. The deposit occurs on Pakira Hill in a zone of contact-metasomatically altered wall rock

Description: Dans la végétation des dunes du Languedoc J. BRAUN-BLANQUET (1952) distingue trois associations, à savoir; 1) l’Agropyretum mediterraneum parmi et sur les premières dunes basses; 2) l’Ammophiletum arundinaceae sur les dunes plus hautes; et 3) le Crucianelletum maritimae dans les dépressions et en arrière des dunes. Or, il est établi que le développement de la première association et le passage de celle-ci à la deuxième sont accompagnés d’une édification de dunes, et que la troisième provient de la dégénérescence de la deuxième. KÜHNHOLTZ-LORDAT (1923) a le premier attiré l’attention sur le rôle essentiel joué par la végétation dans l’édification des dunes du Languedoc. Les résultats de ses recherches ont été confirmés par VAN DIEREN (1934) aux Pays-Bas. Les deux auteurs ont étudié le pouvoir accumulateur du sable par les parties aériennes des plantes; mais le premier seul donne aussi quelques indications sur le rôle édificateur des parties souterraines.

Description: Une évaluation des plantes d’après leur pouvoir édificateur de dunes doit être précédée d’une description de leur structure a côté de l’étendue et de la densité des organes aériens il faut considérer d’importance capitale et décisive la structure des organes souterrains, tel que KÜHNHOLTZLORDAT (1923) et VAN DIEREN (1934) l’ont suggeré. Les organes souterrains peuvent être: des rhizomes, des racines, ou des tiges ensevelies par le sable meuble. Une comparaison des différentes qualités mène à la distinction de groupements et à la création d’un système.

Description: In the course of preparing a treatment of the Bromeliaceae for the “Flora of Suriname” four new species have been encountered and are here recorded for the first time.

Description: In het Onderbos ten Westen van Apeldoorn, dat thans door de gemeente Apeldoorn omgezet wordt in een sportpark, en dat tot dusver over het algemeen uit een arm Querceto-Betuleturn bestond, bevinden zich belangrijke overblijfselen van de middeleeuwse ijzerindustrie, die op de Veluwe gebloeid heeft van de 8ste tot . de 12de eeuw. Hiertoe behoren de twee grootste ijzerslakkenhopen van Europa, voorzover bekend, Haar aanleiding van een bericht, dat ook deze zouden verdwijnen, heeft de heer S. van der Werf, verbonden aan het Laboratorium voor Plantensystematiek en -geografie der Landbouwhogeschool, in de zomer van 1956 deze slakkenhopen botanisch onderzocht. Zij bleken een rijke en interessante flora en vegetatie te bezitten, groeiende op een in de loop van de eeuwen ontstane dunne ijzerslakkenverweringslaag, De grootste bijzonderheid was Selinum carvifolia L., die op beide hopen werd aangetroffen. Op een van beide groeide tevens Lathyrus montanus L. Deze combinatie was eveneens bekend van eikenberkenbosjes langs de Puntbeek in N.O.-Twente en van de Zevendaalse Baan bij Mook (zie: V. Westhoff, Beken en beekdalen in Twente, ins In het Voetspoor van Thijsse, Wageningen 1947), in beide gevallen in een rijk bostype van het Queroion roboris-petraeae, dat overeenkomt met het bostype van de ijzerslakkenhopen van het Orderbos, en dat ir. H. Doing Kraft voorlopig als Violeto-Quercetum aanduidt. De heer S. van der Werf zal t.z.t. de flora en vegetatie van de ijzerslakkenhopen nader beschrijven in “De Lovende Natuur”.

Description: Petasites hybridus (L.) G., M. et Sch. bloeit tijdens de winterslaap van vele floristen en wordt daardoor veelal minder aandachtig bestudeerd dan andere indigenen van vergelijkbare algemeenheid van voorkomen. Het is daarom wellicht gewenst er aan te herinneren dat zij in twee uiterlijk nog al verschillende vormen voorkomt. Vrouwelijke planten hebben talrijke hoofdjes in een vooral in de vruchttijd lang uitgerekte bloeiwijze. De hoofdjes bevatten elk vele vrouwelijke bloemen, zonder meeldraden, met goed ontwikkeld vruchtbeginsel, een zeer lange stijl en twee draadvormige stempels. De bloemkroon bestaat uit een buis met niet of slecht ontwikkelde kroonslippen. Bovendien bevinden zich in het midden van het hoofdje één of meer steriels, schijnbaar tweeslachtige, bloemen met vijf kroonslippen, vijf meeldraden en één knotsvormige stempel.

Description: Orchis simia Lamk. Bij het doorzien van het onderwijs-herbarium van de R.M. Landbouwschool te Dordrecht werd door mij het enige uit Nederland bekende exemplaar van deze soort teruggevonden. Dit exemplaar was indertijd afgebeeld in de Flora Batava, doch in tegenstelling met de meeste daar afgebeelde planten, niet aanwezig in de collecties van het Rijksherbarium of de K.N.B.V. Hoe de plant in Dordrecht is terechtgekomen, is onbekend. Zij werd verzameld in de duinen bij ’s-Gravenhage door R.H. Haverman op 28 Mei 1905 en werd onlangs door de heer J. Guittart, leraar aan genoemde school, aan het Rijksherbarium geschonken, -v.O. Een merkwaardige van Carex brizoides L. De twee bekende vind – plaatsen van Carex brizoides in ons land zijns Wolfhaag (Z.L.) en Weert. Op 22 Mei 1956 vond E.E. van der Voo deze soort in groot aantal in de Krimpenerwaard tij Stolwijks op zandig-venige grond. De zandgrond is daar opgebracht bij de aanleg van een nu opgeheven tramlijn van Gouda naar Schoonhoven. Vermoedelijk is de Carex met het zand meegekomen, De heer van der Voo is nog bezig een onderzoek in te stellen naar de herkomst van het zand; dit zou ons mogelijk op het spoor van nog een andere, tot nu toe onbekende vindplaats van C. brizoides kunnen brengen.

Description: Adamson, R.S.: The South African species of Aizoaceae. II. Tetragonia. (J. S. Afr. Bot. 21, 1955, 109-154). Key. Akiyama, S.: Carices of the Far Eastern region. Sapporo. 1955. 1-257. t. 1-248. Magnificent monograph; keys & descr. in Jap.; syn. in Engl.

Description: Bailey, L.H. G.H.M. Lawrence in Baileya 3 (1955) 27-40, portr., bibl. Cajander, A.K. M.I. Kotilainen, Ber. Deut. Bot. Ges. 68a (1955) 37-40, portr.

Description: Mr A.H.G. Alston was at the Rijksherbarium, Leyden, working on Malaysian Pteridophytes, May 27-June 11, going on to Brussels and Paris for the same aim. In honour of Prof. I.W. Bailey the Chronica Botanica Co has published an account of his writings in a special issue under the title ”Contributions to plant anatomy” (Chron. Bot. 15, pp. xxvi + 262, t. 1-23).

Description: The islands of Aruba, Bonaire and Curaçao form part of a row of small islands off the north coast of Venezuela. Aruba lies 27 km north of the peninsula of Paraguaná and 76 km west of Curaçao; it is separated from the former by a stretch of sea with a maximum depth of 180 m, and from the latter by a channel 1,300 m deep. Bonaire lies 40 km east of Curaçao and 87 km from the South American continent; it is separated from the former by a stretch of sea with a maximum depth of 1,500 m, and from the latter by a stretch of sea with a maximum depth of 1,700 m. Curaçao lies 64 km from the peninsula of Paraguaná and is separated from it by a stretch of sea with a maximum depth of 1,400 m.

Description: Pendant les étés de 1953, 1954 et 1955 j’ai effectué des travaux de terrain dans le Massif des Trois Seigneurs, Pyrénées orientales, sous la direction du Professeur L.U. de Sitter. Ces travaux de terrain comprennent entre autres le levé d’une carte géologique de la partie centrale et Sud-Ouest de ce massif. Le Massif des Trois Seigneurs est un des massifs primaires Nord-pyrénéens, situé au Nord de la „Zone axiale” et entouré de sédiments mésozoïques. Le massif est constitué entièrement de roches paléozoiques. Il doit son nom au Pic des Trois Seigneurs (2199 m) le plus haut sommet de la région.

Description: On the suggestion of Prof. Dr L.U. de Sitter I undertook in the summer of 1955 the detailed mapping of some particular intricate folding combined with some intrusive rocks of different kinds in the vicinity of the village of Las Bordas in the Valle de Arán. A grant from the Molengraaff Fund gave me financial assistance, for which I want to express my grateful thanks.

Description: Sedert 1951 werden in de vorm van gestencilde jaarverslagen de wetenschappelijke resultaten van het veldwerk in de Pyreneeën, in Asturië en elders aan geïnteresseerden, voornamelijk de medewerkers, uitgereikt Deze jaarverslagen, en ook dit verslag, werden door de eerst genoemde auteur samengesteld uit de verzamelde verslagen van alle medewerkers. Teneinde een betere vorm en een grotere verspreiding mogelijk te maken werd besloten deze jaarlijkse wetenschappelijke verantwoording in de L.G.M. op te nemen. De hier bijgevoegde kaartjes van de Pyreneeën en van het Asturische gebied (fig. 1 en 2) geven de ontwikkeling van de karteringen in tijd en ruimte weer. Enkele gebieden werden door verschillende opeenvolgende onderzoekers in studie genomen (alleen de laatste wordt dan vermeld), andere vertonen een aanmerkelijke onderlinge bedekking. De eerdere onderzoekers mogen dit niet als een onderschatting van hun verdienste opvatten, want bijna steeds berust een dergelijke verdubbeling op een groeiend inzicht nà, en dank zij, hun eigen onderzoek, hetgeen een hernieuwde opname noodzakelijk maakt.

Description: The results of a complete census of the breeding population of the White Stork (Ciconia ciconia) in the Netherlands, carried out in the year 1950 by the State Forestry Service, have been published by MÖRZER BRUIJNS and BRAAKSMA in Beaufortia 5, Nr. 45, April 15, 1955, p. 23—42. A new census was performed during the year 1955 ; it is the intention to repeat the census from now on every year. The results of the last census are even more alarming than those from 1950 (see table, p. 113). The number of occupied nests decreased from 83 nests in 1950 to 58 nests in 1955. The number of fledged young decreased from 195 in 1950 to 96 in 1955. Many nests, still occupied in 1950, were either in a state that they could no longer be used or they had vanished altogether in 1955. On the other hand some new nests have been erected in recent time, some of them yielding good breeding results. The data have been arranged in tables according to the provinces. Every nest is numbered. The numbers of the 1950 census are given in parentheses. Nests marked + means that the nest was occupied by a pair of birds, but that no young were fledged. Nests marked — means that the nest was not inhabited, or that it was visited irregularly or else occupied by one solitary bird. The number of young fledged is marked by a figure. A gale in the spring of 1955 destroyed 4 nests ; 12 eggs got lost. Fighting was reported frequently, the unfortunate result being that 3 young storks and at least 37 eggs got lost. These figures probably indicate that at present an insufficient number of nesting sites is avaible in the Netherlands. Therefore it seems worth while to try to erect new nests in localities where fighting has been frequently reported, and to repair those nests that have been visited, but remained unoccupied, owing to the poor state of the nest. In this connection Mr. W. DRIESSEN got most remarkable results with a newly erected nest, made according to a special method. This method should be used for the nests which we hope can be erected or repaired before the new breeding season. Surely the alarming decrease of the White Stork in the Netherlands is not primarily caused by housing problems, but a more appropriate condition and a greater number of nesting sites probably helps to prevent the yearly destruction of perhaps ten or twenty eggs or chicks. Photomechanical reproduction

Description: A varietate typica differt foliis submersis in lacinias 20-60 (plerumque 20-40) 1—1,8 mm latas divisis. Typus in herb. Utrecht, cultivated in aquaria.

Description: Sedert 1948 hebben J. van Dijk Jr. en ondergetekende in het moerasgebied van N.W.-Overijsel jaarlijks op verscheidene plaatsen een merkwaardige vorm van Carex diandra Schrank aangetroffen, die zowel in groeiwijze als in standplaats van de normale vorm verschilt. Dit valt daarom op, omdat Carex diandra overigens een nauwelijks variabele soort is, met een uitgesproken, beperkt milieu. Do soort komt in N.W.-Overijsel nog tamelijk veel voor, en wel, evenals bv. in het Vechtplassengebied, in do zgn. mesotrofe trilvenen, die ontstaan door verlanding van stilstaand, niet door de wind bewogen water in smalle, vaak lange petgaten (dit zijn vroeger uitgeveende gaten). Het kenmerk van oen trilveen is: 1. dat het met de waterstand op en neer gaat (dus niet vatbaar is voor inundatie), 2. dat men er bij betreding niet doorheenzakt (zoals door een drijftil), doch met vegetatie en al langzaam omlaag zakt, m.a.w. in een steeds dieper wordende plas komt te staan. Carex diandra, kenmerkend voor deze mesotrofe trilvenen, groeit er nietzodevormend. Nu komt een afwijkende, dicht zodevormende vorm van Carex diandra voor aan de oever van brede sloten en smalle kanalen, o.a. bij Wanneperveen en in de Bollemaat bij Giethoorn. Habitueel doet zij hier op een afstand aan kleine planten van Carex paniculata denken. De groeiplaats is geen verlandingszone, maar een steile, bijna loodrechte, enkele dm hoge kant, die door het jaarlijks schoonhouden van de sloten in stand blijft en waar land- en watervegetatie dus scherp aan elkaar grenzen. Aan de voet van deze kanten groeien slechts weinig soorten die daar t.o.v. de land- en waterzone een relatief optimum hebben, en dan nog met geringe frequenties dit zijn vooral Iris pseudacorus, Sium latifolium, Carex paniculata, Carex pseudocyperus, en dan hier en daar pollen van Carex diandra.

Description: Utricularia is represented in Malaysia by two main kinds of plant, i.e., aquatic and terrestrial. The aquatic species can again be divided into two main groups, those which float freely in still water and those which are more or less anchored in and beneath shallow water. All of the aquatic species consist of long branching stolons bearing leaves which are divided into capillary segments and traps. The racemes of small yellow, violet, or purple flowers arise from the stolons and project a few inches above the surface of the water. The terrestrial species (including a few which are epiphytic) consist of slender rhizoids bearing linear, spathulate or peltate leaves and traps. These grow on or just below the surface of damp soil and are usually very inconspicuous. From these rhizoids arise the flowering scapes which are erect or twine round other plants and bear a few to many small yellow, white or purple flowers. In the few epiphytic species the rhizoids grow among moss on trees or rocks. Several of the terrestrial species often grow together and as they are all superficially alike, care is necessary to avoid making mixed gatherings. Some of the species exhibit a considerable amount of variation in the size and colouring of the flowers. In collecting Utricularia spp. it is very important to ensure that the specimens are complete, i.e., with flowers, leaves and traps, and if available ripe fruits. With the aquatic species the free floating plants can be lifted complete from the water and (preferably) ”floated out” on to flimsy paper before pressing. The anchored aquatic species must be lifted out with the mud which is carefully washed away before ”floating out”.

Description: Nova Guinea. This serial is continued in a handy octavo format, onwards of new series vol. 6 (1955). It embodies contributions on botany, zoology, geology and ethnography. A new redaction committee is formed of four members for these different branches, general editor is Prof. H.J. Lam, Rijksherbarium, Leyden, secretary of the redaction is Dr M.A. Lieftinck, Mus. Nat. Hist., Leyden. Symposium on land connections across the South Atlantic with special reference to the Mesozoic of the South Atlantic Basin; of. Bull. Am. Mus. Nat. Hist. 99 (1952).

Description: Pendant les étés de 1953, 1954 et 1955, j’ai eu l’occasion d’étudier une partie des Pyrénées centrales, qui se trouve au sud de St. Girons sur le bord de la zone axiale. Le terrein étudié, mesurant à peu près 140 km2, comprend partiellement les vallées de Bethmale, du Salat et de l’Alet et entièrement les vallées d’Estours et d’Esbints. Je tiens à exprimer ma reconnaissance à la „Stichting Molengraaff” de m’avoir donné une subvention qui m’a permis d’effectuer mon deuxième stage sur la terrain.

Description: In het noordwestelijk deel van de provincie Palencia vormt de Sierra del Brezo een onderdeel van de Cordillera Cantábrica. Het resultaat van een geologische kaartering van het oostelijk gedeelte der Sierra del Brezo met zijn aangrenzend gebied is weergegeven in de hier bijgevoegde geologische kaart (schaal 1:25.000). Zowel een onderzoek der stratigrafie, als van de tektoniek leidde tot nieuwe gezichtspunten omtrent dit Palaeozoïsch gebied. Verder wordt in dit werk de petrografie van tien waargenomen gangen besproken en werd aandacht besteed aan het voorkomen van ertsen, t. w. ijzer en koper, en van steenkolen. Dit gebied, dat bijna geheel uit Devonische en Carbonische afzettingen bestaat, is zeer rijk aan fossielen. Vooral het Devoon tussen Ventanilla en San Martin heeft een rijke fauna, in het bijzonder van brachiopoden en koralen. Door middel van fossielen kon worden aangetoond, dat hier een ononderbroken afzetting voorkomt vanaf Emsien (of ouder?) tot Frasnien, met mogelijk een gedeelte van het Famenien. Als bewijs voor de invloed van de Bretonse fase kan het stratigrafisch hiaat gelden (van een gedeelte?) van het Famenien, Tournesien en het Onder-Viséen. Waarnemingen in het veld maakten waarschijnlijk, dat het hier meer een epirogenetische beweging betreft. Howel de fauna van het Carboon hier armer is dan die van het Devoon, kan de stratigrafie door plantenvondsten worden aangevuld. Hierdoor bleek het mogelijk te zijn het Carboon in zijn diverse etages onder te verdelen. Interessant is de oudste Carbonische afzetting, een roodbruin radiolariahoudend gesteente, dat een grote laterale verspreiding heeft. Dit gesteente gaat over in griotte, die plaatselijk knollen van het radiolaria-houdend gesteente bevat. Stratigrafisch volgt de Caliza de Montaña-serie, een neritische kalkafzetting met inschakelingen van schalies. Deze serie heeft een dikte van ongeveer 300 m en komt samen met het Devoon voor in grote, isoclinale plooien, die in zuidelijke richting overhellen. De jongere Namurien en Westfalien A afzettingen, ontwikkeld als een Culm-facies, bevatten geen steenkolenlagen en zijn bovendien arm aan fossielen. Belangrijk bleken de plantenvondsten in het Curavacas-conglomeraat te zijn, die duidelijk een Westfalien B of C ouderdom te zien gaven. Dit enige honderden meters dikke conglomeraat rust met een hoek-discordantie op oudere afzettingen. Hiermee werd een nieuwe orognetische fase, de Curavacas-fase, aangetoond, die ongetwijfeld in deze gebieden een sterke tektonische invloed moet hebben uitgeoefend, gezien de honderden vierkante kilometers grote uitgestrektheid van dit post-orogene conglomeraat. Afzettingen van Westfalien D ouderdom werden in het gebied niet waargenomen. Aan de voet van de zuidelijke hellingen van de Sierra del Brezo bevindt zich — hiervan gescheiden door een overschuivingsbreuk — het steenkolenvoerende Carrión-bekken. De gevonden planten wezen uit, dat dit paralisch bekken een Stefanien ouderdom heeft. Dit zijn de jongste Carbonische gesteenten, die in het bestudeerde gebied voorkomen. De orogenetische Asturische fase, die aangetoond kon worden in een aangrenzend gebied, blijkt tijdens het Boven-Stefanien een sterke tektonische invloed te hebben uitgeoefend. Hieraan zal ook ongetwijfeld het gebied van de Sierra del Brezo onderhevig geweest zijn. Het gekaarteerde Palaeozoicum vindt zijn zuidelijke begrenzing in een discordante bedekking van Mesozoïsche afzettingen, die bijna geheel tot het Krijt behoren, maar ten zuidoosten van Cervera de Pisuerga nog gedeeltelijk tot de Trias en Jura gerekend moeten worden. Mesozoïsche structuren tonen aan, dat Alpine fasen hun invloed in dit gebied hebben doen gelden.

Description: INHOUD\nPag.\nI. Inleiding.................. 1\nII. Historisch overzicht............... 3\nIII. Epidemiologie en oecologie............. 13\nIV. Klinische waarnemingen, pathologie, diagnose en behandeling .... 24\nV. Aetiologie.................. 27\nVI. Scrub itch.................. 28\nVII. Preventieve maatregelen.............. 31\nVIII. Taxonomie van de Trombiculidae . ......... 36\nIX. Conclusies.................. 44\nX. Literatuur ................. 45\nI.\nINLEIDING\nGedurende de tweede wereldoorlog, in de strijd tegen Japan, hebben de geallieerde troepen in Z.O. Azi\xc3\xab en het gebied van de Z.W. Pacific kennis gemaakt met een ernstige ziekte, scrub typhus genaamd, die in korte tijd de gevechtswaarde van de troepen aanzienlijk kon verminderen. Alleen reeds in Nederlands Nieuw Guinea, waar de ziekte voor de oorlog niet bekend was, deden zich enkele duizenden gevallen voor en het totale aantal voor het gehele gebied van Nieuw Guinea en de aangrenzende eilanden is veel hoger (ongeveer 9.000). Scrub typhus volgde als belangrijke ziekte in vele gebieden direct op malaria en was bij de troepen meer gevreesd.\nMerkwaardigerwijze werden na het vertrek van de geallieerde troepen bijna geen gevallen meer gerapporteerd, tot er zich in 1953 en 1954 plotseling weer een aantal voordeden bij de op Biak en de Padaido-eilanden gelegerde

Description: Pendant les \xc3\xa9t\xc3\xa9s de 1953, 1954 et 1955, j\xe2\x80\x99ai eu l\xe2\x80\x99occasion d\xe2\x80\x99\xc3\xa9tudier une partie des Pyr\xc3\xa9n\xc3\xa9es centrales, qui se trouve au sud de St. Girons sur le bord de la zone axiale. Le terrein \xc3\xa9tudi\xc3\xa9, mesurant \xc3\xa0 peu pr\xc3\xa8s 140 km2, comprend partiellement les vall\xc3\xa9es de Bethmale, du Salat et de l\xe2\x80\x99Alet et enti\xc3\xa8rement les vall\xc3\xa9es d\xe2\x80\x99Estours et d\xe2\x80\x99Esbints.\nJe tiens \xc3\xa0 exprimer ma reconnaissance \xc3\xa0 la \xe2\x80\x9eStichting Molengraaff\xe2\x80\x9d de m\xe2\x80\x99avoir donn\xc3\xa9 une subvention qui m\xe2\x80\x99a permis d\xe2\x80\x99effectuer mon deuxi\xc3\xa8me stage sur la terrain.

Description: Sedert 1951 werden in de vorm van gestencilde jaarverslagen de wetenschappelijke resultaten van het veldwerk in de Pyrenee\xc3\xabn, in Asturi\xc3\xab en elders aan ge\xc3\xafnteresseerden, voornamelijk de medewerkers, uitgereikt Deze jaarverslagen, en ook dit verslag, werden door de eerst genoemde auteur samengesteld uit de verzamelde verslagen van alle medewerkers. Teneinde een betere vorm en een grotere verspreiding mogelijk te maken werd besloten deze jaarlijkse wetenschappelijke verantwoording in de L.G.M. op te nemen.\nDe hier bijgevoegde kaartjes van de Pyrenee\xc3\xabn en van het Asturische gebied (fig. 1 en 2) geven de ontwikkeling van de karteringen in tijd en ruimte weer. Enkele gebieden werden door verschillende opeenvolgende onderzoekers in studie genomen (alleen de laatste wordt dan vermeld), andere vertonen een aanmerkelijke onderlinge bedekking. De eerdere onderzoekers mogen dit niet als een onderschatting van hun verdienste opvatten, want bijna steeds berust een dergelijke verdubbeling op een groeiend inzicht n\xc3\xa0, en dank zij, hun eigen onderzoek, hetgeen een hernieuwde opname noodzakelijk maakt.

Description: Three new ostracod species, each belonging to a new genus, were described by the first author (DE VOS, 1953). They had been found on the body and the legs of Limnoria lignorum, the well-known woodburrowing isopod. Since then, we have been looking for commensals in several new lots of European Limnoria, and in this way we obtained valuable new data on morphology and distribution of two of the three ostracod species described.\nMoreover, Dr. Robert I. MENZIES, La Jolla, California, kindly sent us a beautiful lot of ostracods from Limnoria tripunctata MENZIES, an isopod species from the Pacific coast of America, found in test-blocks placed at about 7 feet below mean tide level, and collected in the course of the marine wood-borer studies, Project NR 163\xe2\x80\x94084 at the Scripps Institution of Oceanography, which is supported by the U.S. Office of Naval Research.

Description: Die erste Dactylispa-Art, und \xc3\xbcberhaupt wohl die erste auf der Insel Bali gesammelte Hispina. Sie zeichnet sich aus durch die ganz d\xc3\xbcnnen, k\xc3\xb6rperlangen F\xc3\xbchler (Abb. 1). Sie sind noch d\xc3\xbcnner als die von D. spinosa WEBER, vor allem sind sie zur Spitze nicht verdickt. Sie sind den F\xc3\xbchlern von D. vethi GEST. \xc3\xa4hnlich, aber noch d\xc3\xbcnner. D. praegracilis geh\xc3\xb6rt in den Vethi-Kreis (siehe meinen 135. Beitrag, Philippine J. Sci. 83, 1954, p. 3). Sie ist dort auf p. 28 neben D. sinuispina GRESSITT zu stellen.\nGelbbraun, Halsschild mit zwei schwarzen L\xc3\xa4ngsflecken, Decken schwarz mit Ausnahme des abgeflachten Seitenrandes und der dazugeh\xc3\xb6rigen Dornen, am Hinterwinkel der Seitenrand mit seinen Dornen schwarz. \xe2\x80\x94 Stirn konvex, zwischen den F\xc3\xbchlern mit scharfem, d\xc3\xbcnnem Kiel. F\xc3\xbchler (Abb. 1) von K\xc3\xb6rperl\xc3\xa4nge, d\xc3\xbcnn, vor allem die Glieder 7\xe2\x80\x9411 sehr gestreckt wie bei D. vethi. nur ganz unwesentlich st\xc3\xa4rker als die vorher. Glied 1 lang, schlank, mit nur wenig dickerer Spitze, 2 kurz, 3 etwas l\xc3\xa4nger als 1, 4 = 5, jedes etwas k\xc3\xbcrzer als 3, 6 etwas k\xc3\xbcrzer als 5, 8 = 9 = 10, jedes so lang wie 6, 7 ein wenig l\xc3\xa4nger als seine Nachbarglieder, 11 l\xc3\xa4nger als 10, fein zugespitzt. 2\xe2\x80\x945 fein, schr\xc3\xa4g abstehend behaart, bei den folgenden ist die Behaarung dichter. \xe2\x80\x94 Halsschild quer, vordere Borstenkegel nicht erkennbar, hintere sehr klein. Seitenbewehrung 3,0, mit kr\xc3\xa4ftigen Dornen, der 3. kurz, an der Basis des Stieles der beiden anderen entspringend. Scheibe dicht punktiert, mit glatter, schmaler Mittelfl\xc3\xa4che. \xe2\x80\x94 Schildchen breit-dreieckig. \xe2\x80\x94 Decken kahl, parallel, mit breit abgesetztem Seitenrande, Hinterrand etwas schm\xc3\xa4ler. Punktreihen ziemlich regelm\xc3\xa4ssig, ohne betonte Zwischenr\xc3\xa4ume. Bedornung kurz, kr\xc3\xa4ftig. Ohne Schliessd\xc3\xb6rnchen. Zwischenraum 1 mit einigen Zusatzd\xc3\xb6rnchen, das Paar vor der Mitte am st\xc3\xa4rksten ; Raum II mit II 1 (klein), II 2, II 4, II 5 unter der Zusatzbedornung der Deckenspitze nicht erkennbar ; Raum IV mit IV 1 und IV 1 b, IV 2 (sehr klein), IV 3, IV 4 (klein), IV 5 ; Raum VI mit 3 Dornen auf der Achsel, VI 2, 3, 4 ; Raum VIII mit einer Reihe von Zusatzd\xc3\xb6rnchen, VIII 5 nicht st\xc3\xa4rker als die anderen Hauptdornen. 4 deutliche Basald\xc3\xb6rnchen und 1 Schildchen-Zusatzd\xc3\xb6rnchen. Seitenranddornen l\xc3\xa4nger als die der Scheibe, mit sehr kleinen D\xc3\xb6rnchen abwechselnd, Spitzenranddornen sehr kurz. \xe2\x80\x94 4,4 mm.

Description: Bevor ich mit der Behandlung der tiroler und bayrischen Unterarten von P. apollo L. in dieser Fortsetzung beginne, m\xc3\xb6chte ich ein Vers\xc3\xa4umnis bei der Aufz\xc3\xa4hlung der spanischen Rassen nachholen. subsp. maurilianus Fern. (Bol. Soc. Esp. p. 180, 1926), Typus Palencia, Sierra del Brezo, Villafria, ist als eine intermedi\xc3\xa4r zwischen den subsp. ardanazi Fern. und escalerae Rothsch. stehende Unterart beschrieben, was 22 \xe2\x99\x82 4 \xe2\x99\x80 mit Fundort Camasobres, Palencia, 11. 7. 1941, R. Oberthur, die ich aus dessen Sammlung erworben habe, best\xc3\xa4tigen. Ich m\xc3\xb6chte hinzuf\xc3\xbcgen, dass die \xe2\x99\x82 st\xc3\xa4rker entwickelte Vorderfl\xc3\xbcgelbinden, die \xe2\x99\x80 einen helleren Fl\xc3\xbcgelfond als die \xe2\x99\x82 \xe2\x99\x80 der Vergleichsrassen aufweisen.\nBei der Karakterisierung der Unterarten der tiroler und bayrischen Alpen ist zu den in meiner vorigen Abhandlung erw\xc3\xa4hnten Schwierigkeiten ein neuer meine Arbeit erschwerender Umstand hinzugekommen, die Tatsache, dass eine grosse Menge gezogener Apollo tiroler und bayrischer Herkunft in Umlauf gebracht wurden, ohne ausdr\xc3\xbccklich als solche gekennzeichnet zu sein; diese verst\xc3\xb6ren das einheitliche Rassenbild. Ich bin geneigt anzunehmen, dass z.B. ein erheblicher Prozentsatz der Exemplare, die J.E. Kammel in seiner verdienstvollen Arbeit \xe2\x80\x9eZur Rassenfrage des Parnassius apollo L. aus den n\xc3\xb6rdlichen und zentralen Ostalpengebieten" (Zeitschrift der Wiener Entomologischen Gesellschaft, 1943) abbildet und seiner Karakterisierung zugrunde legt, gezogene Tiere betrifft. Kammel bestreitet die hinreichende Differenzierung verschiedener Rassen, schl\xc3\xa4gt aber vor, diese als formae geographicae bestehen zu lassen. Das ist weder Fisch, noch Fleisch. Auch eine distincte geographische Form muss sich kennzeichnen lassen. Wahr-

Description: In dieser Fortsetzung werden die weiteren franz\xc3\xb6sischen und die spanischen Subspecies von Parnassius apollo L. behandelt.\nBryk zieht im Tierreich bei seiner Einteilung in Rassenkreise zum Jurassischen Kreis auch die subspecies leovigildus Fruhst. und venaissnus Fruhst., die ich indessen als zu dem franz\xc3\xb6sischen Alpenkreis zugeh\xc3\xb6rig ansehe, dem ich mich im folgenden zuwende.\nBevor ich das indessen tue, will ich noch die Beschreibung einiger franz\xc3\xb6sischer Rassen erw\xc3\xa4hnen, die ich vom Augenschein nicht kenne; ich muss mich darauf beschr\xc3\xa4nken, ohne beurteilen zu k\xc3\xb6nnen, ob es sich um bonae subspecies handelt. subsp. anneciensis Testout (Bull. Soc. Linn. Lyon XVI, p. 64, 1947, Typus Th\xc3\xb4nes, Hte-Savoie). subsp. vercorcius Testout (Bull. Soc. Linn. Lyon v. 11 und 12 No. 9 und 10, Typus Col de Romey\xc3\xa8re 1100 m). subsp. aqualensis Acheray (L\' Amateur de Papillons v. 8 p. 228-233, Typus Mont. Aignal, d\xc3\xa9pt. du Gard). subsp. francisci Le Cerf, P. Acheray et A. Reymond (Revue Fran\xc3\xa7aise de L\xc3\xa9pidopt\xc3\xa9rologie, Tome 9, No. 13 p. 227-34, 1939, Typus Monts Forez, r\xc3\xa9gion Pierre-sur-Haute et Bruyere de Brosses).\nDem franz\xc3\xb6sischen Alpenkreis geh\xc3\xb6ren an: subsp. provincialis Kheil (Ent. Z.v. 18 p. 142) Mt. La-Chens 2 \xe2\x99\x82, f. quincunx n.c. 1 \xe2\x99\x82 , 1 \xe2\x99\x80 Topotypen; St. Martin de Vesubie 12 \xe2\x99\x82 4 \xe2\x99\x80 , f. primo + tertiopicta n.c. 1 \xe2\x99\x80 , f. primorubroanalis n.c. 2 \xe2\x99\x80 , f. secundorubroanalis + fasciata n.c. 1 \xe2\x99\x80 ; St. Auban 2 \xe2\x99\x82 1 \xe2\x99\x80 , f. rubroanalis n.c. 1 \xe2\x99\x80 ; Haute-Var 4 \xe2\x99\x82 2 \xe2\x99\x80, f. flavoocellata + flavoanalis n.c.

Description: While studying the collection of recent oxen of the Museum my attention was drawn to the problem of the nomenclature of the Java banteng. I believe to have been able to clear up the confusion that still exists today, as will be set forth in the present note.\nThe wild ox of Java, the banteng, is known variously as Bos sondaicus or Bos banteng, but neither of these is the earliest available valid name. The species should have been called: Bibos javanicus (d\'Alton) B[os] Javanicus d\'Alton, Skelete der Wiederk\xc3\xa4uer, Bonn, 1823, p. (7), pl. VIII fig. c.\nThe earliest reference to the banteng of Java I have been able to find is in Pennant (1800, p. 35): "Mr. Loten told me that wild oxen, of a reddish brown color, with vast horns, and of a great size, are found in Java".\nRaffles, in his oft quoted "History of Java" refers to the wild Javan ox as "b\xc3\xa1nteng" (Raffles, 1817, p. 49; 1830, p. 56) or "b\xc3\xa1nteng" (Raffles, 1817, p. III; 1830, p. 123), but these are vernacularisms, as are "Bentinger" as used by Boie and Macklot (1827, p. 316) and "Bantinger" (Fischer, 1829, p. 500).\nIn February, 1821, two adult banteng skeletons from Java were sent to Leiden by Reinwardt, one male, and the other female. In the handwritten list of specimens of Reinwardt\'s consignment preserved in the archives of the Rijksmuseum van Natuurlijke Historie at Leiden these skeletons are marked as of the wild Javan ox or Bantinger, Bos javanicus. The skulls of these specimens were figured for the first time by d\'Alton (1823, pl. VIII figs, c and d), who, in the explanation of the plate, indicates the male (his fig. c) as "Schadel des Javanischen zahmen Ochsen (B. Javanicus, Reinwardt)",

Description: In the summer of 1953 and 1954 a detailed 1:25.000 map was made of a part of the central Pyrenees. The mapping ranged from Salardu (Valle d\xe2\x80\x99Aran) to Mongarri, (northeast of Salardu). Thanks to a grant from the Molengraaff fund a special study could be made of the structural geology of this district in the summer of 1954. In the course of this study, particular attention was given to the complicated folding tectonics and numerous \xe2\x80\x9cminor structures\xe2\x80\x9d were measured and examined. This method made it possible in some cases to locate synclines and anticlines without seeing their hinges so that some of the stratigraphy could be reconstructed. The stratigraphical sequence as a whole remains doubtful however, as all the layers in the district are nearly vertical and visible folds remain scarce.

Description: The literature on the recent immigration of the Australian barnacle Elminius modestus to West European coasts is rather exhaustive. The present author has given details on the exact centre of immigration on the Dutch coast. The spreading from this centre has been followed in subsequent years (DEN HARTOG, 1953).\nFrom the French coast only few data are known. The localities where it first established itself are unknown. Speculative though it may be, therefore, it seems useful to try a reconstruction of the immigration of Elminius in France as exact data are still available. In July 1951 the author found Elminius on the Boulonnais coast (Pas de Calais: Le Portel, Boulogne sur Mer, Wimereux, Ambleteuse, Audreselles, Cap Gris Nez). On account of our findings on the Dutch and Belgian coasts, they seemed to us to belong to a population radiating from Holland. BISHOP\xe2\x80\x99S (1954) observation however, in the same region, Wimereux, a year earlier (September 1950) did not exactly fit in with this supposition. Real doubt as to the Dutch descent of these specimens arose after finding Elminius in Brittany.

Description: Between August 18 and September 5, 1950, Dr. C. Beets, geologist Royal Dutch Shell Oil Company, explored the aquatic fauna and flora of the Great Bitter Lake. In the course of this exploration dredge hauls were made at 47 stations, distributed all over the lake. An account of this work and a description of the stations were given by Dr. Beets in a previous volume of the present journal (1953).\nThe Decapod Crustacea collected by Dr. Beets belong to twelve species, three of which have not been reported from the Suez Canal before. Apart from these additions to our knowledge of the fauna of the Suez Canal, the present collection is of great interest because of the extensive data provided by Dr. Beets on the ecology of the localities from which the material originates. Decapoda were collected at the following stations: Station 1. Depth 1 to 2.7 m, bottom muddy/sandy though fairly firm, thickly covered with Halophila stipulacea (Forsk.) Aschers., also yielding some Sargassum prob. crispum (Forsk.) Ag. and Spirulina subsalsa Oerst.\nFauna rich. Decapoda: Metapenaeus stebbingi, Periclimenes calmani, Diogenes pugilator, Ebalia granulata, Pilumnopeus vauquelini.\nStation 4. A shoal in a small embayment, 0.2 to 0.75 m deep, with patches of eel-grass and mussels, bottom consisting of somewhat muddy and sandy gravel deposits. Here and there a boulder beset with small sea anemones.\nDecapoda: Paguristes jousseaumei, Ebalia granulata, Pilumnopeus vauquelini.\nStation 5. Depth 9 m, bottom on the whole muddy but with a good deal of coarse sand and gravel, covered thickly by Sargassum. Decapoda: Metapenaeus stebbingi, Trachypenaeus curvirostris, Periclimenes calmani, Dio-

Description: Pendant les \xc3\xa9t\xc3\xa9s de 1953, 1954 et 1955 j\xe2\x80\x99ai effectu\xc3\xa9 des travaux de terrain dans le Massif des Trois Seigneurs, Pyr\xc3\xa9n\xc3\xa9es orientales, sous la direction du Professeur L.U. de Sitter. Ces travaux de terrain comprennent entre autres le lev\xc3\xa9 d\xe2\x80\x99une carte g\xc3\xa9ologique de la partie centrale et Sud-Ouest de ce massif.\nLe Massif des Trois Seigneurs est un des massifs primaires Nord-pyr\xc3\xa9n\xc3\xa9ens, situ\xc3\xa9 au Nord de la \xe2\x80\x9eZone axiale\xe2\x80\x9d et entour\xc3\xa9 de s\xc3\xa9diments m\xc3\xa9sozo\xc3\xafques. Le massif est constitu\xc3\xa9 enti\xc3\xa8rement de roches pal\xc3\xa9ozoiques. Il doit son nom au Pic des Trois Seigneurs (2199 m) le plus haut sommet de la r\xc3\xa9gion.

Description: In het noordwestelijk deel van de provincie Palencia vormt de Sierra del Brezo een onderdeel van de Cordillera Cant\xc3\xa1brica. Het resultaat van een geologische kaartering van het oostelijk gedeelte der Sierra del Brezo met zijn aangrenzend gebied is weergegeven in de hier bijgevoegde geologische kaart (schaal 1:25.000).\nZowel een onderzoek der stratigrafie, als van de tektoniek leidde tot nieuwe gezichtspunten omtrent dit Palaeozo\xc3\xafsch gebied. Verder wordt in dit werk de petrografie van tien waargenomen gangen besproken en werd aandacht besteed aan het voorkomen van ertsen, t. w. ijzer en koper, en van steenkolen.\nDit gebied, dat bijna geheel uit Devonische en Carbonische afzettingen bestaat, is zeer rijk aan fossielen. Vooral het Devoon tussen Ventanilla en San Martin heeft een rijke fauna, in het bijzonder van brachiopoden en koralen. Door middel van fossielen kon worden aangetoond, dat hier een ononderbroken afzetting voorkomt vanaf Emsien (of ouder?) tot Frasnien, met mogelijk een gedeelte van het Famenien.\nAls bewijs voor de invloed van de Bretonse fase kan het stratigrafisch hiaat gelden (van een gedeelte?) van het Famenien, Tournesien en het Onder-Vis\xc3\xa9en. Waarnemingen in het veld maakten waarschijnlijk, dat het hier meer een epirogenetische beweging betreft.\nHowel de fauna van het Carboon hier armer is dan die van het Devoon, kan de stratigrafie door plantenvondsten worden aangevuld. Hierdoor bleek het mogelijk te zijn het Carboon in zijn diverse etages onder te verdelen.\nInteressant is de oudste Carbonische afzetting, een roodbruin radiolariahoudend gesteente, dat een grote laterale verspreiding heeft. Dit gesteente gaat over in griotte, die plaatselijk knollen van het radiolaria-houdend gesteente bevat. Stratigrafisch volgt de Caliza de Monta\xc3\xb1a-serie, een neritische kalkafzetting met inschakelingen van schalies. Deze serie heeft een dikte van ongeveer 300 m en komt samen met het Devoon voor in grote, isoclinale plooien, die in zuidelijke richting overhellen.\nDe jongere Namurien en Westfalien A afzettingen, ontwikkeld als een Culm-facies, bevatten geen steenkolenlagen en zijn bovendien arm aan fossielen.\nBelangrijk bleken de plantenvondsten in het Curavacas-conglomeraat te zijn, die duidelijk een Westfalien B of C ouderdom te zien gaven. Dit enige honderden meters dikke conglomeraat rust met een hoek-discordantie op oudere afzettingen. Hiermee werd een nieuwe orognetische fase, de Curavacas-fase, aangetoond, die ongetwijfeld in deze gebieden een sterke tektonische invloed moet hebben uitgeoefend, gezien de honderden vierkante kilometers grote uitgestrektheid van dit post-orogene conglomeraat.\nAfzettingen van Westfalien D ouderdom werden in het gebied niet waargenomen.\nAan de voet van de zuidelijke hellingen van de Sierra del Brezo bevindt zich \xe2\x80\x94 hiervan gescheiden door een overschuivingsbreuk \xe2\x80\x94 het steenkolenvoerende Carri\xc3\xb3n-bekken. De gevonden planten wezen uit, dat dit paralisch bekken een Stefanien ouderdom heeft. Dit zijn de jongste Carbonische gesteenten, die in het bestudeerde gebied voorkomen.\nDe orogenetische Asturische fase, die aangetoond kon worden in een aangrenzend gebied, blijkt tijdens het Boven-Stefanien een sterke tektonische invloed te hebben uitgeoefend. Hieraan zal ook ongetwijfeld het gebied van de Sierra del Brezo onderhevig geweest zijn.\nHet gekaarteerde Palaeozoicum vindt zijn zuidelijke begrenzing in een discordante bedekking van Mesozo\xc3\xafsche afzettingen, die bijna geheel tot het Krijt behoren, maar ten zuidoosten van Cervera de Pisuerga nog gedeeltelijk tot de Trias en Jura gerekend moeten worden. Mesozo\xc3\xafsche structuren tonen aan, dat Alpine fasen hun invloed in dit gebied hebben doen gelden.

Description: On the basis of the morphology and stratigraphic positions, the bauxite deposits in Suriname and Demerara (British Guiana) were divided into four main groups, namely: 1. Plateau type bauxite, 2. High-level type bauxite, 3. Medium-level type bauxite, 4. Low-level type bauxite.\nThe age of these deposits is as follows: Plateau type bauxite .................................... Pre-Tertiary Low-level type bauxite ................................ Middle- to Lower-Tertiary High-level and Medium-level type bauxite .... Pleistocene These three main periods of bauxitization have led to the formation of fossil bauxite. After these main periods the bauxitization process, however, has not come to a standstill. It continues even at the present time, although less intensively, so that young, sub-recent to recent bauxite is also found.\nIn all bauxite deposits a layer of kaolin underlies the bauxite. In the case of the Plateau type and the Low-level type this kaolin has been derived from solid rock. The kaolin situated below the bauxite of High-level and Medium-level type, is a sedimentary kaolin.\nIn the transition zone between the kaolin and the bauxite, resorption of kaolinite and crystallization of gibbsite is observed.\nThe growth of the bauxite, at the expense of the soil cover clays has been well observed at Onverdacht, where Coropina clay and sub-recent to recent swamp clays (which clays mainly consists of illite) are subject to recent bauxitization after a preceding kaolinization. One can observe the same bauxitization in the transition zone of the bauxite and the soil cover at Mackenzie (Demerara), where this process also takes place in the kaolin clay of the Zandery formation.\nThe chief mineral of the bauxite is gibbsite. Boehmite is also found but in small quantities varying with the age of the type of deposit.\nThe main constituent of the ferrite is hematite, which is an alteration product of goethite. Goethite is found to a much smaller extent.\nIt is not probable that unknown bauxite deposits of the Plateau type and High-level type still exists in Suriname. This is in contrast to the Mediu-level type deposits. All of these deposits have most probably not yet been found. Low-level type bauxite is only seen in Demerara. There are indications, in the form of large and small boulders of bauxite and ferrite in the Zanderij formation, which leads us to believe that this type also occurs in Suriname.

Description: Lichomolgus longicauda (CLAUS, 1860), is recorded from the gills of Sepia officinalis, captured on 5 different occasions in the North Sea and the Dutch Waddensea. This means a northward extension of the range of this species of more than 8 degrees of latitude. Figures of the parasite have been provided, and the literature bearing on the species has been reviewed.

Description: Scientific research into the occurrence and population density of the Harbour Seal ( Phoca vitulina L.) in the coastal regions of the Netherlands, necessary for any efficacious nature conservancy programme, was started in September 1953 by the author.\nA reliable calculation of the total number of Harbour Seals in the coastal regions of the Netherlands soon proved to be extremely difficult. Estimations of the number of Harbour Seals occurring in these regions had been made several times before. BROUWER (1927) took the total number of seals in the Netherlands part of the Waddenzee at 1500 and the total number of seals in the estuaries of the provinces of Zuid-Holland and Zeeland at 800. The first number had been arrived at by means of countings in the field, the latter had been computed from the number of dead animals brought in on account of a bounty system existing for more than twenty years. HAVINGA (1931, 1933) also based his most ingenious calculations on the number of animals killed for bounties. He found that, should the total number of seals stay at the same level, the total population should amount to at least 4000 animals, the bounty killings amounting to 1100 animals annually. At the moment HAVINGA published his report, there was no direct evidence of a decrease in the number of seals, but even so HAVINGA obviously felt a slight doubt in this respect. ERNA MOJHR (1952) compared HAVINGA\xe2\x80\x99S calculations with Russian calculations concerning the Harp Seal (Phoca groentandica FABR.). Her conclusions are that only a total number of 8500 animals was sufficient to endure an annual killing of 1100 animals without decreasing. To my opinion ERNA MOHR was mistaken in using these calculations, concerning a species with quite another biology and a shorter span of life than the Harbour Seal. So, taking into account the Harbour Seal only, the various authors came to different estimations in the coastal regions of the Netherlands. Therefore it seemed worthwhile to attempt a more exact census of this species.

Description: MATERIAL: Eritrea: Gula (15\xc2\xb0 36\xe2\x80\x99 N., 38\xc2\xb0 21\xe2\x80\x99 E.), 500 m., 19 July 1953, Coll. W. J. STOWER, 1 \xe2\x99\x82 (holotype).\nCOLOUR : Head, except the lower portion of the clypeus and a sharply demarcated spot at the medio-posterior side of the antennal sockets which are yellowish, very dark brown. Antennae and legs similarly dark, with only the 8th joint of the first and the tarsal tip of the second whitish. Collum and subsequent segments brown, the posterior half of the keels yellow.

Description: In dieser Fortsetzung werden die schweizer und italienischen subspecies von Parnassius apollo L. behandelt.\nBevor ich mich der Behandlung des schweizer Rassenkreises im einzelnen zuwende, m\xc3\xb6chte ich etwas tiefer auf ein Problem eingehen, das ich schon kurz gestreift habe, und das auch andere Parnassiologen/Entomologen wiederholt besch\xc3\xa4ftigt hat. Was ist die Ursache der \xc3\xbcberaus grossen Variabilit\xc3\xa4t der Parnassier und welche Einfl\xc3\xbcsse bestimmen das Aussehen der einzelnen Individuen und der Unterarten? Es gibt zweifellos in ihrer Erscheinungsform gefestigte Rassen, die bei aller individuellen Variabilit\xc3\xa4tsbreite im Rahmen der betreffenden species eine sichere Bestimmung der einzelnen Individuen hinsichtlich ihrer Rassenzugeh\xc3\xb6rigkeit auch ohne Fundortsangabe gestatten. Als einige Beispiele seien genannt: P. mnemosyne L. subsp. korbi Bryk, P. eversmanni M\xc3\xa9n\xc3\xa9tr. subsp. felderi Bremer, P. nordmanni M\xc3\xa9n\xc3\xa9tr. subsp. minimus Honr., P. Orleans Ch. Oberth. subsp. bourboni O. Bang-Haas, P. honrathi Staud. & A. Bang-Haas, subsp. alburnus Stich., P. bremeri Bremer subsp. graeseri Honr., P. phoebus F. subsp. corybas Fisch.-Waldh., P. actius Eversm. subsp. actinoboloides O. BangHaas, P. jacquemontii Boisd. subsp. kangraensis Bryk & Eisner und subsp. tibetanus F. R\xc3\xbchl, P. nomion Hb. subsp. richthofeni O. Bang-Haas, P. apollo L. subsp. pumilus Stich.; ich k\xc3\xb6nnte diese Aufz\xc3\xa4hlung beliebig fortsetzen, begn\xc3\xbcge mich aber mit den wenigen Beispielen. Die Tatsache, dass der Habitus vieler anderer Rassen demgegen\xc3\xbcber so ver\xc3\xa4nderlich ist, f\xc3\xbchren manche Entomologen darauf zur\xc3\xbcck, dass die Fluggebiete einzelner Unterarten aneinander grenzen \xe2\x80\x94 das gilt insbesondere f\xc3\xbcr das Gebiet der europ\xc3\xa4ischen Alpen \xe2\x80\x94, und demzufolge eine dauernde Mischung von Erb-

Description: During the zoological exploration of Netherlands New Guinea sponsored by the Rijksmuseum van Natuurlijke Historie, Leiden, in 1954-1955, four specimens of Clausiliidae were found. There are no previous records of the occurrence of Clausiliidae in New Guinea; the most eastern locality in the Indo-Australian region from which this family of snails was known is the island of Halmahera, in the Moluccas (Loosjes, 1953, p. 209).\nParaphaedusa minahassae (P. & F. Sarasin, 1899) Sarasin, 1899, p. 218, pl. 26 figs. 267-268.\nEhrmann in Zilch, 1949, p. 77, pl. 4 fig. 10.\nLoosjes, 1953. P. 137, fig. 38.\nThe specimens show the characters as they are typical of the species, but the aperture of some of the shells is somewhat narrower than usual, and the right upper angle of the peristome is a little less distinct in some specimens. The inner structure, examined in one of the shells, shows no differences from that of Celebes shells.\nDr. L. Forcart of the "Naturhistorisches Museum", Basel, Switzerland, kindly sent to me four specimens (paratypes) from Klabat Volcano for comparison, for which I am greatly indebted to him.\nThe species is known from the northern peninsula of the island of Celebes, from the localities: Klabat Volcano at 1500 m altitude under mosses on tree trunks (type-locality), on Soputan Volcano at 1150 m altitude, and on Mount Lokon.\nThe localities in Central Netherlands New Guinea are (fig. 1) : 1. near River Dimija, between Lake Paniai and Lake Tage (Wissel Lakes), 3-I-1955, 1 specimen, leg. Dr. L. B. Holthuis.

Description: In June 1954, during an ecological study of the mangroves near the Research Station of the S\xc3\xa3o Paulo University Oceanographic Institute at Cananeia, about 200 km south of Santos, southern Brazil, Dr. S. Gerlach of the Zoological Institute and Museum of the University of Kiel, Germany, collected some Crustacea representing three species of Decapoda Macrura; two of these belong to the family Alpheidae and one to the Callianassidae.\nI am most grateful to Dr. Gerlach for the privilege to study this small but interesting collection, which now is the property of the Kiel Museum; duplicate specimens are inserted in the collection of the Rijksmuseum van Natuurlijke Historie at Leiden.\nFamily\nALPHEIDAE\nThe two species of Alpheidae were collected near Cananeia, partly under stones, wooden boards, etc., in the tidal zone of a sandy mud beach, and partly in the mud of the edges of mangrove pools. As all the specimens were combined to one lot it is not possible to find out whether the two species occurred at both localities, or that in one or both habitats only one of the species was found.\nAlpheus armillatus H. Milne Edwards The material consists of 13 specimens, the body length of which varies between 12 and 32 mm, the two ovigerous females being 24 and 32 mm long.\nThe specimens agree quite well with the descriptions given in the literature and especially with that by Zimmer (1913, p. 401, figs. K1\xe2\x80\x94T1). Like in Zimmer\'s material, my specimens show the external demarcation of the grooves on either side of the rostrum far less sharply than in Couti\xc3\xa8re\'s (1899) figs. 66 and 67, though the grooves themselves are quite distinct.

Description: For a study in progress on the fossil Bovidae collected in Java by Eug.\nDubois the necessity was felt to create a new genus for the inclusion of the species described as Leptobos groeneveldtii by Dubois (1908, p. 1261). The diagnosis is presented in this place in order that the name may be made available.\nEpileptobos gen. nov.\nDiagnosis: Large Bovinae with relatively broad and low skull. Horns in both sexes. Parietal extremely short, forming a sagittal crest that begins opposite the centre of the horn cores, and passes backward into a strong triangular parieto-occipital eminence, much raised above the fronto-parietal suture and overhanging the occipital. Temporal crests prominent. Occiput triangular in back view, the top of the triangle being formed by the parietooccipital eminence. Hinder ends of temporal fossae approximating to one another to a distance about two-thirds the width of the brain case. Horn cores long, circular in cross section, placed well behind the orbits, curved backward and outward, then upward and forward. There is a slight anticlockwise torsion (right horn core). Molars hypsodont, palate not united to vomer.\nGenotype: Leptobos groeneveldtii Dubois. The diagnosis of this, the only known species, is that of the genus.\nHorizon: Djetis beds of Java, early post-Villafranchian, Middle Pleistocene (Hooijer, 1952, p. 439; 1955, p. 5).\nThe holotype of Epileptobos groeneveldtii (Dubois) is the back part of a skull from Wadegan (Coll. Dub. no. 2766), with both horn cores entire.\nIn his brief description of two skulls of "Leptobos" groeneveldtii in the

Description: The islands of Aruba, Bonaire and Cura\xc3\xa7ao form part of a row of small islands off the north coast of Venezuela.\nAruba lies 27 km north of the peninsula of Paraguan\xc3\xa1 and 76 km west of Cura\xc3\xa7ao; it is separated from the former by a stretch of sea with a maximum depth of 180 m, and from the latter by a channel 1,300 m deep. Bonaire lies 40 km east of Cura\xc3\xa7ao and 87 km from the South American continent; it is separated from the former by a stretch of sea with a maximum depth of 1,500 m, and from the latter by a stretch of sea with a maximum depth of 1,700 m. Cura\xc3\xa7ao lies 64 km from the peninsula of Paraguan\xc3\xa1 and is separated from it by a stretch of sea with a maximum depth of 1,400 m.

Description: Explanation of the geological map (Northwestern part) of the province of La Coru\xc3\xb1a, Galicia, N.W. Spain Main rock groups We distinguish five main groups of rocks which probably differ in age. Whether this age difference applies only to the time of their intrusion or metamorphism or also to their sedimentary origin remains obscure.\nThese five groups are from top to bottom in the time scale: \xe2\x80\x94 (1) Younger rocks, mostly not tectonized, post tectonic. To this group belong: (a) a red sandstone patch west of Malpica on the coast, unconformable on the underlying schists, age unknown; (b) the Traba granite pluton and some other plutonic rocks south of it; (c) rhyolitic or syenitic dykes south of the Traba granite; (d) a swarm of WNW striking basic dykes, mostly dolerites which are probably older than the Traba granite; (2) A group of intrusive rocks which are partly tectonized and partly not, and often have a porphyritic texture. (a) A group which we call the trondjemetic differentiation series, in the north mostly diorites, in the south gradually losing their content of dark minerals. The rocks often contain very large calcic felspar crystals. (b) A group called the Coru\xc3\xb1a granite, mostly biotite granite but with pegmatites containing muscovite. (3) A group of basic rocks, covering a large territory forming an arc with liameter of \xc2\xb1 60 km and consisting of gabbros, pyroxenites, serpentines and amphibolites. The coarse gabbros in the centre of its western branch are not tectonized but the omphibolites on its outer margin are often strongly tectonized. (4) A group of rocks containing migmatites, white granites, gneisses, mica schists and even less metamorphic rocks, which we call the Lage group. The muscovite granite of Lage is certainly a syntectonic granite, and is associated with migmatites and micaschists on the one hand and with much less disturbed granites on the other hand. (5) A group of rocks, showing locally a very high degree of metamorphism, which we call the \xe2\x80\x9cancient complex\xe2\x80\x9d. It contains hornblende gneisses, amphibolites eclogites, muscovite gneisses, granite gneisses and micaschists, and occupies a long NS trending band. It differs from the Lage complex by the frequent occurence of concordant amphibolites.\nThe relation of these groups of rocks is very doubtful in many cases but we believe that the youngest rocks are Paleozoic and the oldest Pre-Cambrian. The doleritic dykes, striking WNW are often regarded as Mesozoic or even Tertiary (Torre de Assun\xc3\xa7ao, 1950, 1951) it follows that Traba granite might also be Tertiary and could perhaps be compared to the Cintra granite of Portugal (Torre de Assun\xc3\xa7ao and Brak-Lamy, 1952) The Lage complex could be compared perhaps with the pre-Ordovician schists which have been called by Teixeira (1954, 1955) the \xe2\x80\x9cante-Ordovician schistograywackes\xe2\x80\x9d and are perhaps Pre-Cambrian.\nProbably our \xe2\x80\x9cancient complex\xe2\x80\x9d represents then an even older Pre-Cambrian orogenic cycle.\nOn the other hand the analyses of the Rb/Sr relation (Hoja de Tuy, 1953) indicate that the pegmatites of the Lage granite are either Caledonian or Hercynian in age, as they imply ages vary between a 270 and 350 million years. The analyses are not isotopic however and one perhaps ought not attach too much value to their result.\nAccording to the field relation of the Coru\xc3\xb1a granites and the Lage migmatites or schists there can be little doubt that the Coru\xc3\xb1a granite is younger. The Coru\xc3\xb1a granite should then be Hercynian because a Caledonian orogeny is almost unknown in the Iberian Peninsula (Carrington da Costa, 1952).\nThe intrusion of gabbro\xc3\xafc rocks is still more difficult to date. On the one hand it has partly been tectonized on its margin whereas the rocks of the centre are perfectly fresh, but on the other hand they are younger than the schists in which they intruded and the Lage orogeny itself. Provisionally we regard their intrusion as late-Hercynian.\nIn general the structures of this western region of Galicia shows a dominant NS trend, bent in an arc convex towards the west. This convexity has been increased by a set of younger faults striking WNW. The schistosity of the rocks is generally parallel to the trend of their boundaries but exact measurements are mostly lacking. Discordant with the prevailing structures are the abovementioned faults, the doleritic dykes which accompany them and the intrusions of younger granites of the Traba group.\nPetrology 1. The Traba granite and associated rocks. \xe2\x80\x94 This group of rocks occurs only in the eastern coastal section of the province of La Coru\xc3\xb1a. They form either great batholiths like the Traba and the Pindo masses, or small outcrops closely related to the big batholiths as near Mug\xc3\xada, Leis and Caneli\xc3\xb1as.\nThe reddish granite generally contains biotits and Na-K felspar, and has sometimes a porphyritic texture. It never shows any preferred orientation of its minerals.\nIts direct thermal metamorphic zone is restricted to some tens of meters, but its influence is felt in a much larger region. Everywhere on the sheets 67 and 92 and the western half of the sheets 68 and 93 one finds numerous small stocks and dykes. These dykes consist either of hornblende syenites, fine grained dacites and quartz porphyries. A semicircular dyke system of these rocks suggests a circular zone of subsidence.\nAnother dyke system, which also traverses the fundamental structure of the Galician system, has an approximately E\xe2\x80\x94W trend. These dykes consist either of basic rocks (lamprophyres, diabase porphyries or dolerites), or of light coloured acid, aphanitic rocks. Their age is certainly younger than the Lage granite, which they traverse, and older than the Traba granite which in its turn appears to cut off the dykes.\nThe Traba granite mass contains zones full of thin mineralized quartz veins containing cassiterite, wolframite, molybdenite and monazite. Some large quartz dykes traverse the granite from north to south. 2. The non orientated, homogeneous and porphyritic, late tectonic granites. \xe2\x80\x94 This group contains all those granitic masses which appear as rounded hills, which in Galicia are called \xe2\x80\x9cpenedos\xe2\x80\x9d, or occupy large flat surfaces.\nIn general they form large batholiths with well defined boundaries and cause thermal metamorphism in the adjacent rocks, but others are clearly granitizised masses. At the contacts of the latter masses one sees a gradual absorption of the rocks of the \xe2\x80\x9cancient complex\xe2\x80\x9d accompanied by a complete reorganization of the elements. The marginal zones coutain numerous xenoliths, distributed without regular orientation, as for instance south of Mugia. When this process of absorption continues the rock becomes homogeneous and a palingenetic granite, sometimes of porphyritic texture like that of la Ru\xc3\xb1a or Monte Pedrouso, or of homogeneous grain like that of Muros, is the result.\nThe different types are: (a) The biotite-granodiorite of Bayo, (b) The biotite-granite of La Coru\xc3\xb1a, (c) Porphyritic muscovite granite of La Ru\xc3\xb1a, (d) Homogeneous muscovite granite of Muros. a. The biotite-granodiorites of Bayo, or rocks of the trondjemitic differentiation series. \xe2\x80\x94 These granodiorites form elongated masses concordant with the trend of the \xe2\x80\x9cancient complex\xe2\x80\x9d or Lage group. Apparently they have assimilated large tracts of the surrounding rocks. The most basic types contain much pyroxene and hornblende, all of them contain biotite and plagioclase, and in the most acid types the plagioclase predominates.\nThe Bayo mass is some 50 km long and has a width varying between 1 and 5 km. The masses of Santa Comba-Negreira are also elongated in a N\xe2\x80\x94S direction. b. Biotite granite of La Coru\xc3\xb1a. \xe2\x80\x94 In eastern Galicia there are several batholithic granite masses which resemble in many respects those of the Bayo type but cannot be included in the same group because their mineralogy and emplacement is different. They form large plutons which are not concordant with the general trend and find their greatest development in the Cambrian and Ordovician of western Galicia, for instance the Lugo granite described by Barrois in 1881.\nIn our region the Coru\xc3\xb1a granite belongs to this group, further east we find the batholith east of Betanzos and Curtis and the large batholith of Vivero-Mondo\xc3\xb1edo. c. The porphyric muscovite granite of la Ru\xc3\xb1a. \xe2\x80\x94 The Ru\xc3\xb1a mountain, 640 m altitude, gives typical exposures of these muscovite-biotite granites. The granite consists of large idiomorphic Na-K felspars up to 7 cm with quartz, muscovite and biotite, it does not show any preferred orientation beyond a faint parallel arrangement of the phenocrysts probably due to the intrusion.\nThe mass is clearly discordant with its surrounding rocks and contains large blocks of the augen gneiss of Lage. We suppose that it constitutes a granitization product of the Lage granite, a palingenic granite in situ. Several similar masses occur in west Galicia for instance, in the Pontevedra province and south of Vigo, and also near Friol near Lugo in eastern Galicia. d. The homogeneous muscovite granite of Muros. \xe2\x80\x94 This type of granite is very frequent in western Galicia. The name is derived from the occurrence near the district of that name north-west of the r\xc3\xada de Noya. We consider it for the present as closely related to the Ru\xc3\xb1a type, more homogeneous, but of the same origin. 3. The basic rocks belonging to the \xe2\x80\x9cLopolith\xe2\x80\x9d. \xe2\x80\x94 The map shows that these rocks form a discontinuous arcuate outcrop some 100 km long in the N\xe2\x80\x94S direction and some 60 km wide. They dip everywhere inwards and are covered by the Ordenes schists, so that the shape of the mass resembles a dish.\nThe petrography of the rocks is very variable, in general we can recognize: 1. Basic diorites with andesine, pyroxene and hornblende. These we find intercalated between the schists of Barra\xc3\xb1\xc3\xa1n (Carballo sheet). 2. An extensive outcrop north of Carballo of ilmenite-rich gabbro rich in alternating with amphibolites. 3. A large mass of fresh looking olivine-gabbro, also with amphibolites, which extends from Mte Castelo to Carballo in an area of some 200 km2. This mass has on its western margin a band of pyroxenites. 4. A large mass of amphibolites east of Santiago de Compostela which contains important mineralizations of pyrrhotite and cupriferous pyrite. 5. A series of outcrops of peridotites, pyroxenites and serpentines on the southern border of the r\xc3\xado Ulla, near Bandeira, Las Cruces and Berredo. This outcrop of basic rocks narrows north of the r\xc3\xado Ulla and continues to the east of Mellid where it broadens again on the hills of Corno do Boy and reaches the R\xc3\xadas near Sobrado. North of Sobrado it broadens again and the ultra-basic rock reaches Teijeiro. After an interruption of some km the serpentines reappear near Irijoa east of Betanzos and in a small outcrop north of Puentedeume. 6. Finally we find a major outcrop of the basic rocks in the extreme north of the province from Moeche to the Cape of Ortegal, occupying the hills of the Sierra de la Capelada. The cupriferous pyrite mines of Cerdido are situated on their eastern border.\nWe do not know yet the age of these intrusions, which might be older than we suppose now. Neither do we know much about the rocks or their structural circumstances. 4. The migmatitic granite of Lage. \xe2\x80\x94 This gneissic granite with two micas occupies a large area in eastern Galicia. The most typical rocks are exposed between the isles of Sisargas and Lage (Schulz, 1835). The texture of the rock is very variable (Expl. sheet Lage no. 43, Tuy no. 261, Oya no. 260), and can perhaps be regarded as an antexitic granite. In the gneissgranite we find parallel zones of migmatized schists and micaschists. Their orientation is roughly N15\xc2\xb0E.\nAlong the western margin of the outcrop of the polymetamorphic \xe2\x80\x9cancient complex\xe2\x80\x9d these gneisses get an augen structure by the development of large felspatic \xe2\x80\x9ceyes\xe2\x80\x9d up to 10 cm long, surrounded by biotite perhaps indicating a kind of mylonitization. These gneisses seem to possess two planar structures at an angle of 15\xc2\xb0 to 20\xc2\xb0, one due to the mica orientation, the other to the felspar eyes. The Lage gneisses differ from the \xe2\x80\x9cancient complex\xe2\x80\x9d gneisses by the absence of parallel basic bands. 5. The \xe2\x80\x9cancient complex\xe2\x80\x9d. \xe2\x80\x94 A narrow zone of highly metamorphic rocks extends from Malpica (sheet 44) in the north to the ria de Arosa (sheet 152) in the south. This zone of 80 km length and roughly 6 km wide is slightly convex to the west. The most typical rock is a glandular biotite-felspar gneiss, but we find also gneissic mica schists and other varieties. In the centre, between Bai\xc3\xb1as and Mazaricos the gneisses contain riebeckite. The whole complex contains numerous parallel narrow zones or dykes of very much tectonized basic rocks, amphibolites, pyroxenites and eclogites.\nThe fact that these rocks show a higher grade of metamorphism and often are polymetamorphic as compared to the Lage group induses us to believe them to be older.\nMineralogically these rocks are characterized by the instability of their micas, biotite and muscovite, and hornblendes. The first group is often found as much deformed relics. Only in the perhaps younger riebeckite gneiss intrusions the hornblende is more stable and uniformly developed.\nNear Malpica biotite gneisses with some muscovite predominate, near Puenteceso and Zas biotite-hornblende gneiss and near Bai\xc3\xb1as and Mazaricos riebeckite gneiss. Near Noya the biotite gneisses deappear. The basic rocks have their greatest development between Zas and Mazaricos.\nInside the complex we can suspect many faults bringing zones of different grades of metamorphism in contact.\nIt seems quite probable that similar zones of highly metamorphic character exist also elsewhere in Galicia. We suppose for instance that the riebeckite granite an dgranite-gneiss east of the Monte del Carrio and those of Silleda in Central Galicia belong to the same group. Perhaps the Ordenes schists of a much lower metamorphic grade above the basic rocks described before, belong to the same group.\nConclusion Perhaps the complicated skeleton which we have presented here as an explanation of our map, and which is the result of numerous excursions in Galicia during recent years can be summarized in the following table: Age of orogeny Mock groups Deformation; genesis Petrographical type Alpine Traba none intrusion Traba granite Bardullas syenite Rhyolitcs Hercynian Muros weak granitization Bayo diorite Coruna granite Runa granite Maros granite t Lopolith .\' Basic rocks Huronian \xe2\x80\x94 800 m.y. Lage intense migmatization Granite-gneiss of Lage Augen granite of Cabrai Archean \xe2\x80\x94 1200 m.y. Malpica (ancient complex) very intense migmatization Penedo granite Borneiro gneiss Bai\xc3\xb1as gneiss Metamorphic basic rocks The correlation of the rock-groups with known orogenic periods is of course very doubtful. The reader must realize that we give this outline only in order to stimulate further research.

Description: On the suggestion of Prof. Dr L.U. de Sitter I undertook in the summer of 1955 the detailed mapping of some particular intricate folding combined with some intrusive rocks of different kinds in the vicinity of the village of Las Bordas in the Valle de Ar\xc3\xa1n.\nA grant from the Molengraaff Fund gave me financial assistance, for which I want to express my grateful thanks.

Description: THE GOLD DEPOSITS IN SURINAM AND THE DISTRIBUTION OF CONCESSIONS THROUGH THE COUNTRY\nThe fieldwork on the occurrence of primary and secondary gold deposits in Surinam on which this thesis is based was carried out by order of the Welfare Fund Surinam (Welvaarts Fonds Suriname) during the periods December 1950\xe2\x80\x94September 1952 and September 1953\xe2\x80\x94January 1954. The regions investigated form part of Surinam (formerly Dutch Guiana), South America. These regions are indicated by heavy lines on the enclosed geological survey map of Surinam, after Schols and Cohen (1953) and IJzerman (1931). As participant of a medical scientific expedition to the southern borderlands of Surinam, I made investigations on the occurrence of gold in this part of Surinam. The trail of the expedition is indicated on the survey map of Surinam (enclosed map).\nAs was stated by statistical (figure 4) and by field evidence, the goldfields of Surinam occur in the northern and eastern part of the country, south of the coastal plain. The goldfields are geo-topografically connected with an area of metamorphic sedimentary schists (Orapu-Formation and Bonnidoroseries) and, mainly epimetamorphic, basic to intermediate volcanic rocks (Balling-Formation without Bonnidoro-series). Two belts of relative concentration of goldconcessions can be constructed from the distribution of the goldconcessions through the area where the goldfields are found. Most of the workable deposits are alluvial or colluvial placer deposits, but in some places in Surinam, primary deposits of hypogene origin are worked. Here the gold is found in gold-bearing quartz veins, -veinlets and -lenses, and in gold-bearing pyrite, which is limonitised as a result of weathering, and which occur in the metasomatically altered wall rock along, as well as in, some of the goldand pyrite-bearing quartz veins and -lenses. These primary deposits, being the result of hypogene processes which are genetically related to intrusive quartzdiorites and granites, occur in the invaded bedrock of the Balling-Formation (Headley-Reef, Km 124,3 L. S., figures 21 and 22) and the Orapu-Formation (Mindrinetti goldfields, Km 93\xe2\x80\x94106 L. S., figures 22 and 25). The placer gold in the alluvial and colluvial deposits of the mentioned areas must be considered to be the concentrated debris of the gold-bearing quartz veins and -lenses, as a result of mechanical transport from chemically weathered, enclosing bedrock. This is in contradistinction with earlier theories of Middelberg (1908), who thinks the placer deposits a result of mainly chemical transport by the help of supergene solutions. Transport of gold by supergene solutions as a result of weathering under most favourable conditions (Bateman, 1949) in the presence of limonitising pyrite, has occurred in some cases over short distances only, from the pyrite to the surrounding matrix. Mostly however the limonitised gold-bearing pyrites are still gold-bearing (table 9). As a process of concentration of placer gold those supergeneous processes are very unimportant. As was stated earlier by Gruttebink and de Haan (1940, 1950, 1952) and as could be reascertained during our fieldwork in the concessions of the Sarakreek Goudvelden N.V. on the upper course of the Lawa river, the placer gold is also the concentrated debris of quartz veins and -veinlets. The same holds good for most of the other investigated areas, i. c. the concession Ettenberg opposite Stoelmanseiland (survey map) and probably the concession Doorson on the southern slope of the Nassau mountains (figure 12). On the other hand in the investigated area of the Kabalebo river near Stone creek (figure 35) the conglomerates of the Orapu-Formation must be regarded as the possible sourcerock of the scarcely scattered gold in the gravels, mostly formed by quartz pebbles from the conglomerate outcrop, at a distance of some tens of metres upstream the creek. This gold shows signs of long-distance transport, because of its roundness (figure 67 e). Workable deposits of this type are not known in Surinam.\nThe gold from the workable placer deposits was not transported over long distances from its source deposit. Therefore the geology of the underlying bedrock of the placer deposits is an important source of information with respect to the genetic relationship between the occurrence of gold and the processes of primary mineralisation, even if the primary gold deposits are not known or hidden by the result of chemical decay of the deposits and their enclosing bedrock. The genetic relation between gold in placer deposits and gold bearing quartz veins is proved by the occurrence of gold-bearing quartz pebbles in the gravels, whereas the geological processes that caused the mineralisation arc detected by the coincidence of the distribution of the placer deposits and contactzones between the Balling-Orapu-Formations and younger intrusive granites and quartzdiorites. The primary deposits have already been found or must be sought for in the invaded bedrock of the Balling- and Orapu-Formation, in the direct contact aureoles of the quartzdiorites and granites (figure 12) or at a certain distance from the outcrops of the contacts, but seldom further than 2000 m (figure 16). In the case of the Mindrinetti-goldfields (figure 25), the placer and primary deposits are concentrated on both sides of a savannah area. This savannah area consists of the weathered products of contact metasomatieally altered schists and conglomerates of the Orapu-Pormation (Grosgroup). The contact metasomatieally altered schists and -conglomerates are here considered as the contact aureole of a hidden granitic intrusion, comparable to the granite of Km 109 L. S. (figure 26).\nThe gold-bearing hypogene deposits don\'t occur in the direct contactzone, but at a short distance from there, not exceeding 2000 m, along shear planes and minor faults. Study was made of the type of granites and quartzdiorites that caused mineralisation, because igneous rocks of the same mineralogical composition are found in the southern and western part of Surinam, where as far as known, workable gold deposits are not found. The granites and quartzdiorites in this part of Surinam are formed as large migmatite-granite complexes of an inhomogeneous mineralogical composition over short distances (de Munck 1953, IJzerman 1931). Because most of the Surinam granites belong to this type, the chemical analyses of the granites represent mostly granites of this migmatite-granite type. In the QLM-diagram (P. Niggli 1945) it can be seen that they belong to the pacific province (calc-alkali magma), but they are very irregularly distributed in this diagram (figure 44). There is a shifting of the plotted analyses to the side of sedimentary rocks, probably meaning that the analyses represent igneous rocks which assimilated a lot of material from the invaded rocks of a different chemical composition. These granites are interpreted as being formed by granitisation. The granitic and quartzdioritic magmas which caused gold mineralisation are characterised by their homogenity, chemically as well as mineralogically, over short and long distances. Their contacts are well marked, either by xenolith\'s (figure 12) or by zones of marked contact-metasomatism (Grosgroup, figures 22 and 26). Four chemical analyses of quartzdiorites which are genetically related to gold mineralisation were made. The result of the analyses are published in table 2. The analyses are plotted against the analyses of other quartzdiorites (figure 45). The same has been done for the granites. The granite of Km 109 L. S. represents an extremely acid granite (granitaplite).\nThese granites and quartzdiorites are interpreted as real intrusive granites. As the quartzdiorites from the concessions on the upper course of the Lawa river are porfiritic, they have a double sequence of crystallisation. The gold deposits of the SE\xe2\x80\x94NW goldbelt of Surinam (figure 4) and those of the concessions Ettenberg (survey map) and Doorson (figure 12) are genetically related to the intrusive quartzdiorites.\nThe same quartzdioritic complex that causes mineralisation on the concession Doorson has been found discordantly covered by the Orapu-Formation (Schols and Cohen 1953). The conglomerates and schists of the Orapu-Formation were never seen to have been intruded by quartzdiorites. The granites of Km 109 L. S. are intrusive into the Orapu-Formation. This proves that granites and quartzdiorites of different age do occur and makes it probable, that both can have caused gold mineralisation. The quartzdiorites (granites no. 1) are supposed to be older than the granite of Km 109 L. S. (granites no. 2).\nThe SE\xe2\x80\x94NW goldbelt of Surinam is genetically related to the granite no. 1 (quartzdiorites); the B\xe2\x80\x94W goldbelt of Surinam to the granite no. 2 (granite of Km 109 L.S.).\nFor both goldbelts we can give the same sequence of events causing workable gold deposits. Only in the Mindrinetti-goldfields and near Km 124,3 L. S. (Headley-Reef) workable primary deposits, as a result of hypogene processes, are known and here have been studied especially, whereas the placer deposits on the upper course of the Lawa river and in the alluvial deposits of this river and the Marowyne have been studied especially there.\nAs a result of the fieldwork and laboratory investigations we can subdivide the different types of gold-bearing deposits into the following groups.\nA. Secondary deposits 1. Deposits formed as a result of mainly mechanical transport a. Alluvial deposits. b. Colluvial deposits. 2. Deposits formed as a result of mainly chemical transport a. Residual deposits. b. Gold-bearing, deeply weathered bedrock.\nB. Primary deposits as a result of hypogene processes 1. Gold-bearing quartz veins, -veinlets and -lenses. a. Gold- and pyrite-bearing quartz veins. b. Gold-bearing blue quartz veins. c. genetically related, not gold-bearing turmaline-quartz veins. d. Gold- and ferberite-bearing quartz veins. e. genetically related, not gold-bearing white quartz veins. 2. Gold-bearing bedrock. a. Gold-bearing pyrite in metasomatically altered wall rock of the gold- and pyrite-bearing quartz veins. b. Gold-bearing bedrock. a. dolerites. p. granites. y. conglomerates.\nThe workable gold deposits in Surinam must be considered to be the result of a genetic sequence of events from intrusive granites or quartzdiorites which intruded older rocks of the Balling- or Orapu-Pormation, causing goldbearing quartz veins and gold-hearing pyrites in the wall rock, which has often been altered contact-metasomatically. The placer deposits are formed from the debris of these primary deposits, mainly as a result of mechanical transport.\nA.\nSECONDARY DEPOSITS\n1. Deposits formed as a result of mainly mechanical transport Most of the workable gold deposits in Surinam are of this type. The gold occurs in these placer deposits as flour gold (up to 0,1 mm), dust gold (0,1\xe2\x80\x940,5 mm) and coarse gold (more than 0,5 mm). Nuggets too occur and are called \xe2\x80\x9cpepieten\xe2\x80\x9d.\nThe gold is marked by irregular forms, flakes and fine specks.\nGrutterink (1940) described some large nuggets from the concession area on the upper course of the Lawa river and states a hypogene origin of these nuggets, because chalcopyrite was found as inclusions in the gold. Morphologically the gold from the placer deposits is sharp-angular to subrounded (figure 67). Gold-bearing quartz pebbles often occur in this type of deposits.\nThese pebbles are also sharp-angular to subrounded. More seldom fully rounded quartz pebbles occur. This proves that the transport of the gold and the gold-bearing quartz did not occur over long distances. a. Alluvial deposits The alluvial deposits can be subdivided into a. recent alluvial deposits; \xc3\x9f. terrace deposits. a. Recent alluvial deposits are the most common type of workable gold deposits in Surinam. The gold occurs in one or more layers of the deposits, mostly concentrated in the gravel-bottomlayer, on a kaolinitic-weathered bedrock. Examples of this type of deposits are illustrated by the figures 15, 17, 18, 23.\nFigure 15 represents an alluvial deposit of the Lawa river, opposite Stoelmanseiland. The deposit consists of gold-bearing sands and gravel on a kaolinitic-weathered quartzdioritic bedrock. Fine and coarse gold occurs in the gravel layer. The gold has irregular subrounded forms. Nuggets do not occur in this place. Gold-bearing quartz pebbles are found in the gravel layer. Some 1500 m upstream the river, the contact between quartzdiorite and the Balling-Formation is hidden by swampy lands and the Lawa river. In the Balling-Formation many quartz veins occur. According to the concessional, nuggets (0,5\xe2\x80\x9410 grams) have been found in the area of the Balling-Formation, which is marked by more accidentated lands and ferritic weathering.\nSo the primary deposits must be sought in this area of the Balling-Formation.\nFigures 17 and 18 illustrate the morphology of the gravel-covered bedrock and the distribution of goldconcentrations in the Bas Rufin (figure 16). Here the gold occurs in a gravel-layer of an average of 70 cm, resting on a kaolinitic-weathered bedrock and covered by layers of sands and clays of 2\xe2\x80\x943 m. The workable deposits are found in the bottom layer of the gravel and the first 2 or 3 cm of the weathered bedrock. Here the gold is found as fine and coarse gold, together with gold-bearing quartz pebbles and irregularly formed nuggets with rounded and subrounded forms and platy sharpangular nuggets weighing up to several tens of grams and not showing any results of transportation. In the weathered bedrock under these gravel layers, gold-bearing quartz veins occur. This proves that the gold from these deposits has partly been transported over short distances, whereas soms of the gold has to be considered as eluvial.\nFigure 23 shows a section, situated on the borderline of the savannah area and the hills of the gold bearing zone of De Jong Zuid and Gros Placer (figure 25). Here the gold-bearing deposits consist mostly of material of the gold-bearing zone, whereas the colluvial deposits of the savannah area prove to be barren of gold. The morphology of the gold, found in these deposits, is subrounded. \xc3\x9f. Terrace deposits, in Surinam prospection, is the name given to all gravel deposits above creek- or river level. Deposits of this type are illustrated by figures 5, 6, 7, 17, 18.\nFigures 5, 6, 7 reproduce a type of terrace deposit found in the Marowijne river. At main waterlevel, in the river and along the banks of the river we find cemented riverconglomerates, which rise up to 2 meters above waterlevel. The quartz pebbles of the conglomerates (2\xe2\x80\x9420 cm) are perfectly rounded. Along the banks they are covered by sands and clays. Some of the islands (tabbetjes) in the river are the remains of older riverbank terraces (Nason).\nThe conglomerates proved to bear a small amount of gold.\nThe fine gold has irregular rounded forms. Deposits of this type are not worked in Surinam. Another type of terraces is found in the valleys along the creeks on the upper course of the Lawa river. This type is illustrated by figures 17 and 18. The gold in these terraces has the same morphology as the gold in the recent alluvial deposits. The terraces represent an earlier stage of the creek, which carved a valley in preexisting rocks. The terrace deposits are characterised by their topographical height above creek level and by their more ferritic appearance as a result of weathering processes above water level.\nSometimes the gold in this type of deposits occurs together with limonite. b. Colluvial deposits The colluvial deposits link together the alluvial deposits of the type A. 1. a and the primary deposits of the type B. They are characterised by yellow and redbrown sandy granular clays with angular gold and quartz fragments and often ferritic iron stones. The deposits represent the slightly transported debris which resulted after the lateritic weathering of the underlying bedrock. They are transported as a result of creep and of the removal of large volumes of peliticweathered bedrock by erosion. The occurrence of quartz fragments and free gold with angular morphology in this type of deposits proves that in most instances the chemical weathering did not affect the gold to an important degree. In some cases gold-bearing limonitised pyrite is found in this type of deposits.\nSometimes the colluvial deposits form a foothill plain. The colluvial deposits are affected by chemical weathering, resulting in the formation of so called \xe2\x80\x9ckraskouw\xe2\x80\x9d layers. This kraskouw, being a stage of ferritic weathering of transported material above water level, occurs in the clays of the terrace deposits too. Kraskouw is characterised by its irregular reticulated ferritic enrichment and pore-space filling by clay matter.\nFigures 19 a. b. c. illustrate some types of colluvial deposits.\nFigure 19 a represents the most common type of colluvial deposit.\nThe clay matrix of the upper layer is washed out by erosion, by which the layer has undergone enrichment in quartz fragments and iron stones. The lower layer has more pelitic contents but also belongs to the colluvial deposit transported by creep, because quartz-fragments and gold occur, whereas the underlying bedrock does not show quartz veins.\nFigure 19 b illustrates colluvial deposits which cover an older terrace deposit. Kraskouw has been formed in the colluvial layers.\nFigure 19 c represents a deposit that has been considered as a result of filling of a creek valley with residual quartz boulders, by mainly colluvial deposits. The quartz boulders, measuring up to several cubic feet, are subrounded to angular. In this type of deposit, nuggets have been found with sharp-angular platy forms, which prove that the nuggets were formed as a result of fissure filling from gold-bearing solutions of hypogene origin (Grutterink 1940). 2. Deposits formed as a result of mainly chemical supergene processes Deposits of this type have not yet been carefully studied in Surinam. Some random observations prove the existence of this type of deposits but nowadays no workable deposits of this type are known in Surinam. These deposits seem to be a consequence of the weathering processes in primary and secondary gold deposits. They result into: a. Residual deposits. b. Gold-bearing, deeply weathered bedrock. a. Residual deposits Residual concentration of gold in the ferritic final members of the lateritic weathering of gold-bearing deposits in the form of gold-bearing quartz fragments and free gold, belongs to the type already discussed as colluvial deposits.\nBeside this type of residual concentration there is also another type which probably is a result of the above mentioned processes. Here the ferrites themselves are gold-bearing as was proved by van Kooten (1953). Assays of ferrites above the gold-bearing deposit of Pakira Hill (De Jong Zuid) showed a grade of 2,5 g Au/ton. b. Gold-bearing, deeply weathered bedrock Probably a piece of gold-bearing clay, which was found in the kaoliniticweathered bedrock under the gravel layers of the Rufin (figure 82), belongs to this type. The morphology of the gold and the distribution through the clay prove it perfectly impassible that this gold is placer gold, which penetrated mechanically into the clay. There is always a possibility that the gold was already formed in the unweathered bedrock by hypogene processes but this doesn\'t explain the clayey-weathered bedrock that is enclosed in the gold. To a certain degree some results of the limonitic weathering of gold-bearing pyrites in the quartz veins and in the contact-metasomatically altered wall rock along these veins also belong to this type, which will be treated together with B. 1. a., because the deposits formed in this way are mainly formed by hypogene processes.\nB. PRIMARY DEPOSITS,\nAS A RESULT OF HYPOGENE PROCESSES\nPrimary deposits are only worked in the environment of the country railroad between Km 93 and Km 133.\nThese deposits were studied especially, although here too, placer deposits of the same types which have already been discussed, are more important as contributors to the gold production of Surinam than the primary deposits.\nTwo types of primary deposits can be distinguished.\nThe first type is that of the Mindrinetti-goldfields and can be found in several zones on both sides of the savannah area of figure 25, between Km 99,5 and Km 105,5 L. S. (country railroad).\nThe second type occurs near the contact of the Kabeltonalite (figure 22). The primary deposits of the Mindrinetti-goldfields lie in deeply-weathered, contact-metasomatically altered wall rock which consists of (sandy-) kaolinitesericite-quartz-bearing clays (figure 31). Often limonitised pyrite occurs in the contact zones along gold-bearing quartz veins.\nThe kaolinitic-weathered contact-metasomatically altered wall rock is distinguished from the normal regional-epimetamorphic schists and conglomerates of the Orapu-Formation, by its colour, which is often white or a pastel shade of rose, violet, yellowbrown and redbrown; by its often high kaolinite percentage (table 5, column VI); by its unconsolidated pelitic character (table 6 and figure 50), conglomeratic relicstructure and its topographic position along goldbearing quartz veins. The normal epimetamorphic conglomerates and schists of the Orapu-Formation are weathered to a smaller degree and are still consolidated rocks. Lateritic weathering of these rocks results in the formation of ferrites which occur in the colluvial deposits on the tops and the slopes of the bills.\nThe weathering products of the Grosgroup (figure 22) are characterised by the same weathering features as the contact-metasomatically altered rocks along the gold- and pyrite-bearing quartz veins, but here limonitised pyrite, nor gold occur.\nThe unconsolidated sandy kaolinite-sericite-quartz clays change into the consolidated conglomerates and schists of the Orapu-Formation, loosing their pelitic character and later on their non-ferritic weathering. As was proved by two drillings into the unweathered parts of this contact-metasomatically altered bedrock, which were located by reason of the results of the laboratory investigations on the weathering products, the contact-metasomatism resulted in important changes of the mineralogy and chemistry with respect to the epimetamorphic schists and conglomerates of the Orapu-Formation.\nMineralogically the contact-metasomatically altered rocks of the Grosgroup (figure 25, WFI) consist of chlorite- and calcite-bearing epidote-sericite-albitequartz schists, whereas the regional-metamorphic schists of the Orapu-Formation consist only of (chlorite-, chlorito\xc3\xafd- and plagioclase-bearing) sericite-quartz schists and -conglomerates.\nThe contact-metasomatically altered wallrock of the gold-bearing zone of Pakira Hill (De Jong Zuid, LB 65) consists of a biotite-bearing quartz-sericiteepidote-albite rock. Table 4 shows the estimated mineralogical changes caused by the contact-metasomatism. The process of contact-metasomatism mineralogically results in the formation of albite and epidote mainly and also of calcite in the rocks of the Grosgroup and of biotite in the rock of the Pakira Hill.\nChemically the contact-metasomatism is characterised by the supply of soda and lime into the schists and conglomerates of the Orapu-Formation, which form albite and epidote in a first stage, synchronous with desilicification of the pre-existing conglomerates and schists; whereas in a later stage carbonatisation and silicification occurred. This stage of silicification was found in the drilling WF I. Here small quartz and calcite veins cut through the newly formed albite (figure 46). In the drilling LB 65 only the first stage was found. Possibly the equivalent of the second stage of the contact-processes here can be found in the gold-bearing quartz veins. It seems very probable that the processes, which caused contact-metasomatism and those which caused gold mineralisation and quartz veins, are genetically related and that both result from the intrusion of a hidden granitic intrusion which exists under the savannah-area (figure 26). It is probable that the residual solutions which escaped from the intruding magma, reacted with the invaded bedrock. As a result of the reactions with the invaded bedrock an exchange of elements occurred, whereby the residual solution became more concentrated with Si02, whereas the invaded rock became enriched in sodium and calcium. The contactmetasomatism of the Grosgroup is here interpreted as a result of diffuse processes, whereas the gold-bearing quartz zones are the results of more concentrated solutions, which acted along shear planes and minor faults.\nThe figures 51 and 52 illustrate the relative supply and removal of the elements, joined into groups si, al, fm, c and alk after P. Niggli (1945). In figure 51 the removal and relative concentration of elements from contactmetasomatically altered rocks to their weathering products is shown and in figure 52 the relative supply and removal from the epimetamorphic subgraywacke (WB III) to the contact-metasomatically altered rocks of the drillings WF I and LB 65 and then to the weathering product of LB 65 is shown.\nFigure 53 illustrates the same supply and removal of the elements on the supposition that Al2O3 was supplied nor carried off during the processes. The analyses are compared by the same calculated atom equivalent of 282 for \xc2\xbd(Al2O3). 1. Gold-bearing quartz veins, veinlets and lenses Figures 25 and 26 show the relations between granites, zones of contactmetasomatism and the gold-bearing and related quartz veins, as they were interpreted by field evidence and laboratory studies.\nAlong the northern boundary of the savannah-area (De Jong Noord) five zones of gold-bearing and genetically related quartz veins are found. Each zone is characterised by its own paragenesis of the quartz veins which usually strike in a similar direction and occupy a certain area. The gold-bearing deposits occur as separated groups of quartz veins and -lenses, called reefs (figures 27, 28, 29 and 30). Thus a zone has several reefs, characterised by the same paragenesis. Every reef consists of several quartz veins and -lenses either with the same paragenesis (De Jong Noord) or of more types of quartz veins and -lenses each with their own paragenesis (De Jong Zuid).\nFive types of paragenesis are distinguished, being: a. Gold- and pyrite-bearing quartz veins. b. Gold-bearing blue quartz veins. e. genetically related, non-gold-bearing turmaline-quartz veins. d. Gold- and ferberite-bearing quartz veins. e. genetically related, non-gold-bearing white quartz veins.\nThis subdivision is made of the quartz veins in the Mindrinetti-goldfields but holds good for the other concession areas too, i. c. the concessions on the upper course of the Lawa, the concession Ettenberg opposite Stoelmanseiland, Headley-Reef near Km 124,3 L. S. and Concession Doorson on the southern slope of the Nassau mountains. Some other types of paragenesis are found on these concessions but they are of secondary importance with respect to the gold-bearing primary deposits. Not all types occur on the same concession. Type d was found only at one place in Surinam (Pakira Hill, De Jong Zuid). a. Gold- an pyrite-bearing quartz veins The gold- and pyrite-bearing quartz veins are the most common and most easily discovered type of primary gold deposit of the Mindrinetti-goldfields. Here they are characterised by contact zones of metasomatically altered wall rock, as was described before. This wall rock has been altered by weathering into kaolinitic-clay and often shows schistose- or conglomeratic relicstructures. Gold-bearing, limonitised pyrite often occurs in this wall rock. Figures 27, 30 and 31 show sections through the gold-bearing primary deposits of this type, whereas figure 25 shows the distribution of the zones where reefs of this type occur (reefs marked P.).\nAssays of the quartz are given in table 8. Table 9 shows assays of goldbearing, limonitised pyrite from the wall rock of the quartz veins of this type.\nThe gold occurs scattered through the quartz between the boundaries of grains and in cracks of the quartz. Gold also occurs in the surrounding matrix of the limonitised pyrite, which has been impregnated by iron oxides and hydroxides (figures 57 and 58). Here it appears as fine specks or sometimes as flaky gold in the crystal-negatives of completely-weathered pyrite. Figures 59 and 60 show the stages of weathering of the pyrite. The white parts of figure 60 are the non-weathered pyrite, surrounded by low reflecting material (limonite I). The dark grey parts further away from the pyrite also consist of limonite (limonite II). The light-grey parts represent the final stage of the weathering of the pyrite. They consist of hematite.\nMacroscopically visible gold is seldom encountered in these gold-bearing limonitised pyrites. One sample of the last mentioned type was presented to me by the Sarakreek Goudvelden N.V. for laboratory investigations. The figures 61 and 62 show the morphology of the gold (white) in the limonitised pyrite (grey). This morphology is considered to originate from the weathering processes of the limonite and as a result of transportation of the gold by supergene solutions.\nBeside gold-bearing, limonitised pyrites and gold-bearing quartzes which result from the weathering of the pyrites, primary gold of hypogene origin occurs in the gold-bearing quartz veins of this type of deposits. Figure 64 shows the outlines of primary gold from these quartz veins. As a result of limonitic-weathering of gold-bearing pyrites in the wall rock of these quartz veins, limonite and hematite walls occur which enclose the veins. Secondary enrichment has occurred on the boundary between the limonite-hematite and the quartz. Here the gold has been concentrated as a result of supergene processes. These gold-bearing limonite-hematite walls along the quartz veins are known as """"tjaps"""" in Surinam. The supergene processes however didn\'t contribute to the amount of gold of the gold-bearing deposits as a whole. Only slight transport and concentration over a distance measurable in cm\'s, resulted from these supergene processes. Of course it is possible that relative concentration occurred by carrying off of other formerly existing minerals. b. Gold-bearing blue quartz veins Gold-bearing greyblue, blue and blueblack quartz veins occur in the goldfields of Surinam. They were studied especially on De Jong Noord (figure 25), De Jong Zuid and on the concessions on the upper course of the Lawa river. One specimen of an extremely deep blueblack colour proved to enclose millions of semi-opaque inclusions. The walls of the inclusions are coated by particles of solid matter, whereas the content of the inclusions consists of liquid- and gaseous CO2. By concentrating the solid matter from the inclusions, through treatment of the quartz with HF, and by X-ray analyses of the thus obtained concentrate, the solid matter which causes the colour of the blue quartz was proved to be graphite.\nPrimary gold of hypogene origin was studied in a specimen of bluegrey quartz from the concessions on the upper course of the Lawa river. The gold is irregularly distributed through the quartz (figure 65) and contains inclusions of three different minerals beside quartz, which is replaced by the gold (figure 66).\nOne of the included minerals is probably chalcopyrite, which possibly encloses valleriite.\nThe blue quartz veins on De Jong Noord are not characterised by contactzones of kaolinitic-weathered, metasomatically altered wall rock. On De Jong Zuid this type of quartz vein occurs together with the gold- and pyrite-bearing type of quartz veins in a zone of strongly contact-metasomatically altered and later weathered wall rock. Here they are probably younger than the gold- and pyrite-bearing quartz veins because they change into turmaline-bearing blue quartz veins as a transition between the gold-bearing blue quartz veins and the non-gold-bearing turmaline-bearing white quartz veins. e. Genetically related, turmaline-bearing white quartz veins On De Jong Zuid the quartz veins of this type are certainly younger than the gold- and pyrite-bearing quartz veins, because they cut through these veins. On De Jong Noord two zones of non-gold-bearing turmaline-quartz veins border the zones of gold-bearing quartz veins. d. Gold- and ferberite-bearing quartz veins Ferberite was found at only one place on De Jong Zuid. The deposit occurs on Pakira Hill in a zone of contact-metasomatically altered wall rock

Description: Several cases of deformities in the spinal column were described in fishes, viz. lordosis in the bitterling Rhodeus amarus) by ROTH (1922), in the minnow (Phoxinus phoxinus) by ROTH (1922), in the pike (Esox lucius) by ROTH (1922) and PLEHN (1924); kyphosis in the toothcarps (Cyprinodontidae) by ROTH (1922); scoliosis in the carp Cyprinus carpio) by HOFER (1904), ROTH (1922) and PLEHN (1924); kyphoscoliosis in the toothcarps by ROTH (1922); kypholordosis in the highly arched Aischgr\xc3\xbcnder race of the carp by SPICZAKOW (1935) and in the carp by SCH\xc3\xa4PERCLAUS (1941, 1954); plecospondylic spinal column in the eel (Anguilla anguilla) by SCH\xc3\xa4PERCLAUS (1941, 1954) and in the guppy or millionfish (Lebistes reticulatus) by STOLK (1955 a). SCHR\xc3\xa4DER (1930) described curvatures of the spinal column in fishes of about 55 species and families.\nIn this paper we briefly describe a case of plecospondylic spinal column, observed in an adult eel (Anguilla anguilla) (fig. 1). The fish was fixed in formalin and embedded in paraffin. The sections (4\xe2\x80\x946 \xc2\xb5) were cut frontally and transversally and stained with hematoxylin and eosin, hematoxylin and phloxin as also according to the VAN GIESON method and the azan method.

Description: The results of a complete census of the breeding population of the White Stork (Ciconia ciconia) in the Netherlands, carried out in the year 1950 by the State Forestry Service, have been published by M\xc3\x96RZER BRUIJNS and BRAAKSMA in Beaufortia 5, Nr. 45, April 15, 1955, p. 23\xe2\x80\x9442.\nA new census was performed during the year 1955 ; it is the intention to repeat the census from now on every year.\nThe results of the last census are even more alarming than those from 1950 (see table, p. 113). The number of occupied nests decreased from 83 nests in 1950 to 58 nests in 1955. The number of fledged young decreased from 195 in 1950 to 96 in 1955. Many nests, still occupied in 1950, were either in a state that they could no longer be used or they had vanished altogether in 1955. On the other hand some new nests have been erected in recent time, some of them yielding good breeding results. The data have been arranged in tables according to the provinces. Every nest is numbered. The numbers of the 1950 census are given in parentheses. Nests marked + means that the nest was occupied by a pair of birds, but that no young were fledged. Nests marked \xe2\x80\x94 means that the nest was not inhabited, or that it was visited irregularly or else occupied by one solitary bird. The number of young fledged is marked by a figure. A gale in the spring of 1955 destroyed 4 nests ; 12 eggs got lost.\nFighting was reported frequently, the unfortunate result being that 3 young storks and at least 37 eggs got lost. These figures probably indicate that at present an insufficient number of nesting sites is avaible in the Netherlands. Therefore it seems worth while to try to erect new nests in localities where fighting has been frequently reported, and to repair those nests that have been visited, but remained unoccupied, owing to the poor state of the nest. In this connection Mr. W. DRIESSEN got most remarkable results with a newly erected nest, made according to a special method. This method should be used for the nests which we hope can be erected or repaired before the new breeding season. Surely the alarming decrease of the White Stork in the Netherlands is not primarily caused by housing problems, but a more appropriate condition and a greater number of nesting sites probably helps to prevent the yearly destruction of perhaps ten or twenty eggs or chicks.\nPhotomechanical reproduction

Description: Mr. C. Hoogerheide, who was stationed at the Netherlands Naval Air Base at Biak Island between July 1953 and December 1954, brought together a small collection of birds, which was sent to the Leiden Museum. It is worth while to put on record those species, which have not been collected before on this island and to give remarks on a few other species. An excellent review of the avifauna of Biak Island is given by Mayr and De Schauensee (1939).\nFregata ariel ariel (Gray) A \xe2\x99\x82 imm. and a \xe2\x99\x80 imm. have been collected by Mr. F. Heuberger at sea near the south coast of Soepiori between Korrido and the kampong So\xc3\xabk on July 26, 1952. Through the intermediary of Dr. L. D. Brongersma the specimens were presented to the Leiden Museum.\nNear this island the species has been collected before only by Beccari on May 8, 1875. Mayr and De Schauensee (1939, p. 14) already pointed out that the specimen must have belonged to ariel and not to minor as Salvadori (1882, p. 405) stated. It may be added that in the Leiden Museum there are no specimens of minor from the New Guinea region. The measurements of the 2 specimens are: wing 530, 553; middle tail feathers 190, 185; outer tail feathers 308, 330; culmen 88, 88; bill from gape 107, 106; tarsus 25, 22 mm.\nAviceda subcristata obscura nov. subspec.\nMr. Hoogerheide collected 5 specimens on the south coast of Biak. Moreover the Leiden Museum possesses a specimen collected by Von Rosenberg at Biak on March 25, 1869. Particulars of the specimens follow here: Sex Date Wing Tail Culmen from cere Tarsus \xe2\x99\x82 22- 8-1953 289 168 20 32

Description: Lardoglyphus zacheri Oudemans and L. (= H oshikadania) konoi (Sasa and Asanuma) were sent to me by Mr. D. A. Griffiths of the Infestation Control Division of the Ministry of Agriculture. They were found in butcher\'s offal ("gut greaves"), used in the manufacture of fertiliser, on premises near Chesterfield. In this particular case the offal was obtained locally, though it can also be imported from the Argentine; possibly the mites were orginally introduced into this country on empty uncleaned sacks obtained from other manufacturers.\nThe purpose of this paper is to provide a more complete description of L. zacheri Oudemans, and also to clear up some confusion in nomenclature.\nLardoglyphus zacheri Oudemans, 1927 (figs. 1-5) Female (fig. 1). Length of idiosoma of six individuals: 450-600 /JI. The body is spindle-shaped, widest between the second and third pairs of legs and tapering towards either end; the posterior edge is concave. The body cuticle is smooth and cream-coloured, the legs, apodemes, and chelicerae are of a darker shade; the propodosoma lacks a dorsal shield and is clearly separated by a transverse groove from the hysterosoma.\nThe setae of the idiosoma are smooth and slightly pectinate. The vertical internals (v. i) arise close together and project forward over the gnathosoma without reaching its extremity; the vertical externals (v. e) orginate from the same level, they are pectinate and curve towards the base of the chelicerae; behind them are the pseudostigmatic organs \xe2\x80\x94 small, curved and serrated \xe2\x80\x94 which lie in a depression above the base of leg I and are encircled by a lateral sclerite; at the anterior end of this sclerite is Grandjeans organ, a triangular fold of cuticle.

Description: Parnassius clodius hel subsp. nova Schon die erste Sendung einer gr\xc3\xb6sseren Anzahl von P. clodius M\xc3\xa9n\xc3\xa9tr., die ich von D. Frechin empfing, enthielt Exemplare, die in den Mts. Cascade, Washington, gefangen waren und ein von dem \xc3\xbcbrigen clodius-Material, das vom Gorst Creek, Bremerton, Bear Creek, Tahuyah Creek, Mission Creek, alle Washington-State, stammte, verschiedenes Aussehen zeigte. Eine zweite gr\xc3\xb6ssere Ausbeute aus den Mts. Cascade best\xc3\xa4tigte meine Vermutung, dass es sich bei den Tieren vom Stevens Pass 4500\' und Berne 3500\' um eine distincte H\xc3\xb6henrasse handelt, die sich zu subsp. claudianus Stich. wie subsp. baldur W. H. Edw. zu der Stammform verh\xc3\xa4lt. Allerdings zeigt die neue Unterart eine subsp. baldur W. H. Edw. entgegengesetzte Entwicklungstendenz, subsp. baldur W. H. Edw. zur Reduktion der Zeichnungselemente, subsp. hel (m.) zu deren Verst\xc3\xa4rkung und zur Verdunkelung, weshalb ich die Rasse nach der G\xc3\xb6ttin der Unterwelt in der nordischen Mythologie \xe2\x80\x9eHel" benannt habe. Mit subsp. baldur W. H. Edw. hat meine hel die auffallend starke Verkleinerung der Ozellen gemeinsam, von denen das Medianauge bei 14 von mir insgesamt vorliegenden 102 \xe2\x99\x82 schwarz ausgef\xc3\xbcllt ist. Eine Erscheinung, die ich bei P. clodius M\xc3\xa9n\xc3\xa9tr. erstmalig festgestellt habe, ist die f. grundi n.c. = zus\xc3\xa4tzlicher schwarzer Fleck zwischen den beiden Zellflecken, der 4 \xe2\x99\x82 und 3 \xe2\x99\x80 angeh\xc3\xb6ren (1 \xe2\x99\x82 Holotypus, 1 \xe2\x99\x80 Allotypus, 3 \xe2\x99\x82 2 \xe2\x99\x80 Paratypen in c. m.). Von subsp. claudianus Stich. unterscheidet sich die neue Unterart vor allem auch in der Gr\xc3\xb6sse, \xe2\x99\x82 31-35 mm, \xe2\x99\x80 30-34 mm gegen\xc3\xbcber der Vergleichsrasse \xe2\x99\x82 34-39 mm, \xe2\x99\x80 32-39 mm, wobei noch darauf hingewiesen werden muss, dass die Mehrzahl von subsp. hel sich der unteren, die von subsp. claudianus Stich. der oberen

Description: In 1953, Mr. E. C. Stol, naturalist at Leiden, kindly placed at my disposal a small collection of Surinam freshwater aquarium fishes. A second collection, consisting of freshwater and marine specimens from Surinam, mainly collected by Dr. D. C. Geijskes and Mr. H. W. Lijding (Fishery Department), was received during 1954. As the two collections proved to contain several interesting specimens belonging to species not yet reported from Surinam, the following enumeration is given.\nTo the measurements of specimens with damaged caudal fins the mark is added.\nDasyatis guttata (Bl.; Schn.) 1 ex., near lightship Surinam River, 5-8 miles E., 12 January 1954, H. W. Lijding, 412 mm, \xe2\x99\x82.\nFurther data: length of disc (to anus) 97 mm; length of tail (from anus) 315 mm; width of disc 106 mm; snout (to orbit) 26 mm; floor of mouth with three distinct papillae; skin completely smooth; yolk sac well developed. A well known species from the Surinam coastal area.\nGymnura micrura (Bl.; Schn.) 1 ex., Surinam River (8-10 miles above outlet?), 11 February 1954, H. W. Lijding, 165 mm, \xe2\x99\x82.\nA common Caribbean species; the type came from Surinam.\nNarcine brasiliensis (Olfers) 1 ex., near lightship Surinam River, 5-8 miles E., 13 July 1953, H. W. Lijding, 123 mm, 9.\nThere are distinct dark circular markings on the back. This species is quite common in the Caribbean waters but apparently had not yet been

Description: In the collection of the Haifa Sea Fisheries Research Station, among material trawled in Mersin Bay, S. E. Turkey, two Brachyuran crabs were found which prove to be of great interest. One, Actaea rufopunctata (H. Milne Edwards), has a rather wide distribution in both the Atlantic and the Indo-West Pacific regions, but only very few records from the Mediterranean are known as yet. The other, Ixa monodi, a species of IndoWest Pacific origin, is new to science, while the genus to which it belongs is now reported for the first time from the Mediterranean.\nActaea rufopunctata rufopunctata (H. Milne Edwards, 1834) (pl. IV fig. 1) An ovigerous female (cb. 20 mm) 1) was trawled in Mersin Bay in August 1954. The specimen fully agrees with the published accounts of this species.\nOdhner (1925, p. 60) in his revision of the genus Actaea distinguished two forms of Actaea rufopunctata, viz., the typical form and a variety retusa Nobili, 1905. Actaea nodosa Stimpson, 1860, was considered by Odhner as a full synonym of A. rufopunctata, but was later made by Rathbun (1930, p. 257) a subspecies of the latter species. Thus at present three forms of Actaea rufopunctata are recognized: A. r. rufopunctata (H.\nMilne Edwards, 1834), A. rufopunctata nodosa Stimpson, 1860, and A. rufopunctata retusa Nobili, 1905.\nOur Turkish specimen proves to belong to A. r. rufopunctata. The narrow tip of the carapace region 3M 1) reaches beyond 2M as in the typical form, while in A. r. nodosa the tip of 3M reaches about to the middle of 2M. The frontal and lateral lobes of the carapace of our specimen are

Description: The present paper contains the results of studies on the tribe Greenideini of the subfamily Greenideinae Takahashi, 1931, a primitive group of Aphididae mainly restricted to East Asia. Material could be studied of twentyseven species described by previous authors, while seven species had to be described as new. Some changes had to be effected in the systematic arrangement, so that at present six genera (old and new) are recognised in the group, together including five subgenera. In spite of repeated attempts not all the species so far described could be examined, accordingly in a final chapter notes are added on the species that were not available.\nThe project for carrying out research work on Aphididae could be realised through the kind help of Mr. D. Hille Ris Lambers at Bennekom, who not only selected a suitable subject for these studies (the genus Greenidia and its allies), but also placed the valuable material from his private collections at my disposal together with the literature of the group from his library, and, moreover, arranged for the loan of specimens from other institutions.\nAfter having discussed at Bennekom the plans for the investigations, the work was carried out in the Rijksmuseum van Natuurlijke Historie at Leiden, whilst the results were supervised by Mr. Hille Ris Lambers during my repeated visits to Bennekom; I am greatly indebted to him for assiduous guidance and for hospitality received at his home.\nIn the Rijksmuseum van Natuurlijke Historie help and encouragement was received from Professor H. Boschma in various ways, while manyfold help was obtained from Dr. L. B. Holthuis, curator of Crustacea. Thanks are due to Dr. W. Vervoort, Zoological Laboratory, Leiden, for the micro-

Description: During my studies of the Surinam specimens belonging to this genus my attention was drawn to the often wrong interpretation of several old species. To avoid future misidentifications it seems useful to give a short review of the American species that are known up till now. It is emphasized, however, that this paper does not have the pretension to be a monograph of the American species. For the greater part my study of the species was confined to the type material and the variability therefore is not known. However, this contribution may serve as a base for a future monograph of this interesting group.\nAttention is drawn to the fact that only older leaves of the plants should be studied, because the leaf apex of the younger leaves is in all species acute and the lamina may not have reached its definite form.

Description: Une \xc3\xa9valuation des plantes d\xe2\x80\x99apr\xc3\xa8s leur pouvoir \xc3\xa9dificateur de dunes doit \xc3\xaatre pr\xc3\xa9c\xc3\xa9d\xc3\xa9e d\xe2\x80\x99une description de leur structure a c\xc3\xb4t\xc3\xa9 de l\xe2\x80\x99\xc3\xa9tendue et de la densit\xc3\xa9 des organes a\xc3\xa9riens il faut consid\xc3\xa9rer d\xe2\x80\x99importance capitale et d\xc3\xa9cisive la structure des organes souterrains, tel que K\xc3\x9cHNHOLTZLORDAT (1923) et VAN DIEREN (1934) l\xe2\x80\x99ont sugger\xc3\xa9.\nLes organes souterrains peuvent \xc3\xaatre: des rhizomes, des racines, ou des tiges ensevelies par le sable meuble. Une comparaison des diff\xc3\xa9rentes qualit\xc3\xa9s m\xc3\xa8ne \xc3\xa0 la distinction de groupements et \xc3\xa0 la cr\xc3\xa9ation d\xe2\x80\x99un syst\xc3\xa8me.

Description: In the course of preparing a treatment of the Bromeliaceae for the \xe2\x80\x9cFlora of Suriname\xe2\x80\x9d four new species have been encountered and are here recorded for the first time.

Description: The list of Marantaceae published by PULLE (1906) comprises 20 species belonging to 6 genera, the largest genus being Calathea with 8 species. It was found, however, that one of the species does not belong to the family: investigation of the type of Calathea strobilifera (Miq.) Koern., viz. Kegel 1469 [GOET], showed that it pertains to Renealmia strobilifera Poepp. et Endl. (Zingiberaceae). The record of another species, Calathea allouia (Aubl.) Lindl. appeared to be based on a misidentification: the collection Focke 893 cited under this name by PULLE (1906) belongs to C. grandis O. G. Peters. Later on PULLE (1909) recorded the occurrence of one species more of this family in Suriname, viz. Myrosma polystachya Pulle, a new species. Since then no further additions to the list of Suriname species have been published.\nOur investigation of the Suriname material showed the occurrence of 33 species belonging to 8 genera. In the following pages a few taxonomic and phytogeographical remarks are made on some of these genera and species; they also contain the description of a new genus.

Description: It can hardly be denied that the expression \xe2\x80\x9cGeneral Plant Morphology\xe2\x80\x9d, which is so often met with in botanical textbooks, has little or no meaning. A general morphology of the Plant Kingdom would have to occupy itself with those morphological features that are common to all groups of plants, which means that it would have to confine itself to the common features of the cell structure and eventually to such peculiarities as are independent of the uni- or pluricellular structure of the plant body, e.g. its enclosure within a rigid envelop. However, when we realize that there is in this respect no fundamental difference between the common features of plants and animals or, at least, of some groups of animals it will be clear that the use of the expression \xe2\x80\x9cGeneral Plant Morphology\xe2\x80\x9d is misleading and should be avoided.\nWhat in most botanical textbooks is understood by \xe2\x80\x9cGeneral Morphology\xe2\x80\x9d is not a morphology of the whole Plant Kingdom but only of a part of it; however, the delimitation of this part, and this is a most astounding feature, is but seldom explicitly indicated, and, moreover, proves to vary, sometimes even in different chapters of the same work. Most textbook-writers seem to agree that Algae and Fungi have a morphology of their own, and that the latter should be left to specialists in these fields; they accordingly restrict their attention either to the Embryophyta, i.e. the group which comprises the Bryophyta and the Vascular Plants, or to the Vascular Plants alone.

Description: In the course of examination of specimens in the fern collection of the Botanisch Museum en Herbarium, Utrecht, the senior author discovered a specimen of Doryopteris that seemed to be different from any species treated in the junior author\xe2\x80\x99s revision of the genus. Further examination has proved this to be the case and it is here described as new.\nDORYOPTERIS conformis, spec. nov.

Description: A varietate typica differt foliis submersis in lacinias 20-60 (plerumque 20-40) 1\xe2\x80\x941,8 mm latas divisis.\nTypus in herb. Utrecht, cultivated in aquaria.

Description: Sedert 1948 hebben J. van Dijk Jr. en ondergetekende in het moerasgebied van N.W.-Overijsel jaarlijks op verscheidene plaatsen een merkwaardige vorm van Carex diandra Schrank aangetroffen, die zowel in groeiwijze als in standplaats van de normale vorm verschilt. Dit valt daarom op, omdat Carex diandra overigens een nauwelijks variabele soort is, met een uitgesproken, beperkt milieu. Do soort komt in N.W.-Overijsel nog tamelijk veel voor, en wel, evenals bv. in het Vechtplassengebied, in do zgn. mesotrofe trilvenen, die ontstaan door verlanding van stilstaand, niet door de wind bewogen water in smalle, vaak lange petgaten (dit zijn vroeger uitgeveende gaten). Het kenmerk van oen trilveen is: 1. dat het met de waterstand op en neer gaat (dus niet vatbaar is voor inundatie), 2. dat men er bij betreding niet doorheenzakt (zoals door een drijftil), doch met vegetatie en al langzaam omlaag zakt, m.a.w. in een steeds dieper wordende plas komt te staan. Carex diandra, kenmerkend voor deze mesotrofe trilvenen, groeit er nietzodevormend.\nNu komt een afwijkende, dicht zodevormende vorm van Carex diandra voor aan de oever van brede sloten en smalle kanalen, o.a. bij Wanneperveen en in de Bollemaat bij Giethoorn. Habitueel doet zij hier op een afstand aan kleine planten van Carex paniculata denken. De groeiplaats is geen verlandingszone, maar een steile, bijna loodrechte, enkele dm hoge kant, die door het jaarlijks schoonhouden van de sloten in stand blijft en waar land- en watervegetatie dus scherp aan elkaar grenzen. Aan de voet van deze kanten groeien slechts weinig soorten die daar t.o.v. de land- en waterzone een relatief optimum hebben, en dan nog met geringe frequenties dit zijn vooral Iris pseudacorus, Sium latifolium, Carex paniculata, Carex pseudocyperus, en dan hier en daar pollen van Carex diandra.

Description: In het Onderbos ten Westen van Apeldoorn, dat thans door de gemeente Apeldoorn omgezet wordt in een sportpark, en dat tot dusver over het algemeen uit een arm Querceto-Betuleturn bestond, bevinden zich belangrijke overblijfselen van de middeleeuwse ijzerindustrie, die op de Veluwe gebloeid heeft van de 8ste tot . de 12de eeuw. Hiertoe behoren de twee grootste ijzerslakkenhopen van Europa, voorzover bekend, Haar aanleiding van een bericht, dat ook deze zouden verdwijnen, heeft de heer S. van der Werf, verbonden aan het Laboratorium voor Plantensystematiek en -geografie der Landbouwhogeschool, in de zomer van 1956 deze slakkenhopen botanisch onderzocht. Zij bleken een rijke en interessante flora en vegetatie te bezitten, groeiende op een in de loop van de eeuwen ontstane dunne ijzerslakkenverweringslaag, De grootste bijzonderheid was Selinum carvifolia L., die op beide hopen werd aangetroffen. Op een van beide groeide tevens Lathyrus montanus L. Deze combinatie was eveneens bekend van eikenberkenbosjes langs de Puntbeek in N.O.-Twente en van de Zevendaalse Baan bij Mook (zie: V. Westhoff, Beken en beekdalen in Twente, ins In het Voetspoor van Thijsse, Wageningen 1947), in beide gevallen in een rijk bostype van het Queroion roboris-petraeae, dat overeenkomt met het bostype van de ijzerslakkenhopen van het Orderbos, en dat ir. H. Doing Kraft voorlopig als Violeto-Quercetum aanduidt.\nDe heer S. van der Werf zal t.z.t. de flora en vegetatie van de ijzerslakkenhopen nader beschrijven in \xe2\x80\x9cDe Lovende Natuur\xe2\x80\x9d.

Description: Het Instituut voor het Vegetatie-onderzoek van Nederland (I.V.O.N.) werd opgericht in 1930 en is thans gevestigd in het Rijksherbarium, Nonnensteeg 1 , Leiden, Het stelt zich o.a. ten doel om door stelselmatige inventarisatie een overzicht te verkrijgen van de verspreiding der in Nederland voorkomende Pteridophyta en Spermatophyta. Reeds in 1902 werd door de heren Dr. J.W.C. Goethart en W. J. Jongmans, destijds resp. conservator en assistent aan het Rijksherbarium, een aanvang gemaakt motdit biogoo grafische onderzoek. In de jaren daarna werd het met medewerking van een aantal Nederlandse floristen voortgezet, waarna men wegens de toenemende betekenis van het werk en met medewerking van de heren Goethart en Jongmans in 1930 kwam tot de oprichting van het I.V.O.N.\nBij de inventarisatie werd tot voor enige jaren \xe2\x80\x93 het oorspronkelijke werk werd nl. in 1949 afgesloten \xe2\x80\x93 gebruik gemaakt van de Topografische kaart van Nederland, schaal 1 : 50.000, welke ten behoeve van het onderzoek door verticale en horizontale lijnen in vakken was verdeeld van 1045 bij 1250 m. Deze vakken, kwartierhokken genaamd, vormden de eenheden van de inventarisatie. Per kwartierhok werd nl. genoteerd welke planten daarin werden waargenomen, hetgeen gebeurde op excursies in verschillende jaargetijden, waardoor een zo volledig mogelijk overzicht der voorkomende soorten werd bereikt. De zo verkregen gegevens werden vervolgens soort voor soort in albums overgebracht, waarbij ieder album betrekking heeft op een der 62 bladen van de Topografische kaart 1 : 50.000. Tenslotte was het mogelijk om de in de albums vervatte gegevens op een kaart van Nederland te noteren, zodat een overzicht werd verkregen van de verspreiding van de betreffende soorten over het gehele land. Als resultaat werd een serie z.g. Plantenkaartjes van Nederland uitgegeven. Deze kaartjes geven, dank zij de grote volledigheid, die bij de inventarisatie bereikt werd, een betrouwbaar beeld van de verspreiding der plantensoorten. Het ligt in de bedoeling om de publicatie van deze serie Plantenkaartjes zo lang voort te zetten tot een beeld van de verspreiding van alle Nederlandse Pteridophyta en Spermatophyta verkregen zal zijn. In de nog te verschijnen kaartjes zullen daarbij alle gegevens tot en met 1949 verwerkt worden.

Description: He in het vooruitzicht gestelde literatuur-rubriek zal in het volgende nummer worden geopend.

Description: Orchis simia Lamk. Bij het doorzien van het onderwijs-herbarium van de R.M. Landbouwschool te Dordrecht werd door mij het enige uit Nederland bekende exemplaar van deze soort teruggevonden. Dit exemplaar was indertijd afgebeeld in de Flora Batava, doch in tegenstelling met de meeste daar afgebeelde planten, niet aanwezig in de collecties van het Rijksherbarium of de K.N.B.V. Hoe de plant in Dordrecht is terechtgekomen, is onbekend. Zij werd verzameld in de duinen bij \xe2\x80\x99s-Gravenhage door R.H. Haverman op 28 Mei 1905 en werd onlangs door de heer J. Guittart, leraar aan genoemde school, aan het Rijksherbarium geschonken, -v.O.\nEen merkwaardige van Carex brizoides L. De twee bekende vind \xe2\x80\x93 plaatsen van Carex brizoides in ons land zijns Wolfhaag (Z.L.) en Weert. Op 22 Mei 1956 vond E.E. van der Voo deze soort in groot aantal in de Krimpenerwaard tij Stolwijks op zandig-venige grond. De zandgrond is daar opgebracht bij de aanleg van een nu opgeheven tramlijn van Gouda naar Schoonhoven. Vermoedelijk is de Carex met het zand meegekomen, De heer van der Voo is nog bezig een onderzoek in te stellen naar de herkomst van het zand; dit zou ons mogelijk op het spoor van nog een andere, tot nu toe onbekende vindplaats van C. brizoides kunnen brengen.

Description: The rapid accumulation of data necessitated the issue of a new bulletin. It was with deep gratitude that I remembered, in the Xmas holidays during which I was compiling this text, the many letters received from various sides expressing appreciation for our enterprise. Editor\xe2\x80\x99s hearts need sometimes a little warming; ours remains distinctly encouraged.\nParticular encouragement I got from the British Colonial Office which, stimulated by the Government of Malaya, has given a grant to our Foundation to cover part of the travel and accomodation expenses of Dutch collaborators in the United Kingdom, provisionally for two years. This manifest sign of appreciation from the British and Malayan Governments for our work is significant and most gratefully remembered here.

Description: Bryophyta. The new collections built up during the last years under the supervision of Prof. R. van der Wijk, Groningen, have now all been arranged and provisionally been identified by him and his collaborator Mr Margadant. Revisional work has started.\nPteridophyta. A most important collaboration, anticipated for years, is that of doctors Holttum, Kew, and Alston, London, who have now definitely agreed in compiling the series II of the Flora Malesiana containing the account of the Pteridophyta. Dr Alston spent a year (Oct. 1955-Oct. 1954) in Indonesia on the invitation of the Indonesian Government. Dr Holttum has finished his large work on the ferns of Malaya; he is now finishing off an account of the bamboos of Malaya and will then set definitely to the study of Malaysian Pteridophytes. Some limited families will be worked out by both specialists as a sample.

Description: The preparation of a new account of the pteridophytes of the whole Malayan region is a very large undertaking, and when one is at the beginning of it, one cannot foresee what may happen during the course of its execution. It is in part a voyage of discovery.\nThe work will have to be done in stages, and published in parts. To wait until it is all completed, and then to coordinate and re-arrange it before publication, would mean an unreasonably long delay. But to publish it in parts will inevitably mean that one will have new ideas about the early parts as one works on the later ones. My hope is that, when the work is finished, it will be possible to have a new and better conception of the inter-relations of the parts. Present schemes for definition of families for the great majority of ferns are no more than tentative, and that is one reason why I see no need to carry out the work in any pre-arranged sequence.

Description: The genus Stenandriopsis was created by S. Moore in Journ. of Bot. 44: 153. 1906 for a plant collected first by Vaughan Thompson and afterwards by Baron in an unspecified part of Madagascar. As the plate by which the description is accompanied depicts the specimen collected by Baron (n. 6708), the latter is to be regarded as the type.\nStenandriopsis was referred by its author to the Justicieae, but this tribe is apparently accepted by him in the delimitation it received in BENTHAM and HOOKER\xe2\x80\x99s \xe2\x80\x9cGenera Plantarum\xe2\x80\x9d, and as it is in this sense a most heterogeneous mixture, this does not greatly enlighten us. Of more importance is that Moore compares it with Crossandra Salisb. and Stenandrium Nees, i.e. with genera belonging to my subfamily Acanthoideae and referred by me respectively to the Acantheae and the Aphelandreae. However, in my paper on \xe2\x80\x9cThe Acantheae of the Malesian Area. I. General Considerations\xe2\x80\x9d in Proc. Kon. Ned. Akad. v. Wetensch., Ser. c. 58: 166. 1955, I pointed out that it can not belong to the Acantheae as the corolla throat lacks the incision in the adaxial side which is characteristic for that tribe. It can not belong to the Aphelandreae either as the corolla limb is subactinomorphous instead of distinctly bilabiate. As I had to rely at that time entirely on Moore\xe2\x80\x99s description and on the plate by which the latter is accompanied, I was unable to arrive at a conclusion, but I suggested that the genus might represent a new tribe of my Acanthoideae. Since then I have had the opportunity to inspect in the herbarium of the British Museum of Natural History the material on which the genus was based, for which I tender my best thanks to the Keeper, and now I am able to express a more definite opinion.

Description: This vegetation survey is the outcome of an investigation of the islands of the Netherlands Antilles carried out under the auspices of the Foundation for Scientific Research in Surinam and the Netherlands Antilles. The data on which the present study is based were obtained during a trip which lasted from September 1952 until October 1953. During this trip the following islands were visited: Cura\xcf\x82ao, Bonaire, Aruba, St. Martin, Saba, and St. Eustatius. A short visit was also paid to the island of St. Kitts (B.W.I.).\nThe present work gives an account of the actual vegetation of the Netherlands Antilles. Other studies, comprising the systematic results and conclusions of the survey, are being prepared, and will possibly be published in 1958.