ALBERT

Description: The following account of the non-marine Mollusca of the Island of Sumatra, the second largest of the Greater Sunda Islands (surface 440.000 km2) is based on the following collections: 1. Zoological Museum, Amsterdam, including the material collected by Prof. Max Weber, Dr. L. P. de Bussy, Jhr. Dr. F. C. van Heurn, Prof. J. C. van der Meer Mohr, Dr. E. Jacobson, and many others. 2. Rijksmuseum van Natuurlijke Historie, Leiden. 3. Museum Zoologicum Bogoriense, Bogor (Java). 4. Naturhistorisches Museum, Basle (Switzerland). 5. Zoologisches Museum, Z\xc3\xbcrich (Switzerland). 6. Mus\xc3\xa9um d\xe2\x80\x99Histoire Naturelle, Geneva (Switzerland). 7. Naturmuseum Senckenberg, Frankfurt am Main (Germany). 8. Mr. J. P. van Niel, who lived in Sumatra from 1951 to 1956 and made great efforts to collect molluscs in his leisure time. This material has been presented to the Zoological Museum, Amsterdam. 9. Various private cabinet owners in the Netherlands and one in Switzerland who received their material from relations overseas.\nIn the list of localities these collections will be referred to by the following symbols: ZMA Zoological Museum, Amsterdam RMNH Rijksmuseum van Natuurlijke Historie, Leiden MBo Museum Zoologicum Bogoriense, Bogor MBa Naturhistorisches Museum, Basel MZh Zoologisches Museum, Z\xc3\xbcrich MGv Museum d\xe2\x80\x99Histoire Naturelle, Geneva SMF Senckenberg Museum, Frankfurt Nl Mr. J. P. van Niel Br Mr. A. C. van Bruggen, Leiden Bt Mr. L. J. M. Butot, Haarlem By Dr. P. Bohny, Basle Dr Mr. J. Drijver, Wageningen Ls Dr. F. E. Loosjes, Wageningen Nb Mr. W. H. Neuteboom, Heemskerk Sl Mr. L. van der Slik, Rotterdam Vm Mr. L. A. W. C. Venmans, Moergestel

Description: Am 5. August 1956 traf von Dr. H. Kern auf dem Schiffswege aus Djakarta eine erwachsene Netzschlange, Python reticulatus Schn., von 6.40 m L\xc3\xa4nge im Tierpark Berlin ein. In ihre Kiste hatte man f\xc3\xbcr den etwa vier Wochen dauernden Schiffstransport ein lebendes Huhn (gro\xc3\x9fer Malaiischer K\xc3\xa4mpfer) hineingesetzt, das unterwegs gefressen wurde. Reste davon \xe2\x80\x94 darunter ein Fu\xc3\x9f \xe2\x80\x94 wurden dann unvollkommen verdaut wieder erbrochen. Nach der Ankunft in Berlin brachten wir die Riesenschlange zun\xc3\xa4chst provisorisch in einem kleinen Terrarium unter. Dort nahm sie zwei mittelgro\xc3\x9fe Meerschweinchen zu sich. Mittlerweile war ein gr\xc3\xb6\xc3\x9ferer Beh\xc3\xa4lter f\xc3\xbcr das Tier fertiggestellt worden, in den die inzwischen durch die W\xc3\xa4rme der Schlangenfarm munterer gewordene Schlange umgesetzt wurde. Hier verweigerte die Schlange in der Folge jede weitere Nahrung. Es zeigte sich nunmehr \xe2\x80\x94 4 m distal von der Schnauzenspitze \xe2\x80\x94 eine abgetreppte Verschiebung (Abb. 1) der Wirbels\xc3\xa4ule, die auf einen Bruch des R\xc3\xbcckgrates schlie\xc3\x9fen lie\xc3\x9f. Die Schlange magerte in den folgenden Wochen erheblich ab, und der Bruch trat endlich so stark in Erscheinung, da\xc3\x9f der Python nicht mehr ausgestellt werden konnte. W\xc3\xa4hrend die Schlange in der ersten Zeit noch sehr aggressiv war und der vor dem Bruch liegende K\xc3\xb6rperteil immer noch hoch aufgerichtet wurde, ergriff in zunehmendem Ma\xc3\x9fe immer gr\xc3\xb6\xc3\x9fere Apathie das Tier, bis es schlie\xc3\x9flich v\xc3\xb6llig teilnahmslos herumlag. Innerhalb von vier Monaten erfolgten drei H\xc3\xa4utungen. Hinter dem Bruch schwoll der v\xc3\xb6llig gel\xc3\xa4hmte K\xc3\xb6rperabschnitt bis zum After stark an (Abb. 2). Der Schwanz blieb von der Schwellung unber\xc3\xbchrt. Der K\xc3\xb6rperumfang vor dem Bruch betrug 35 cm, hinter ihm 56 cm. Die Haut des aufgetriebenen K\xc3\xb6rperteiles war sehr m\xc3\xbcrbe und n\xc3\xa4\xc3\x9fte an verschiedenen Stellen. Am 30. November 1956 starb die Netzschlange. Der angeschwollene Teil ging nach dem Tode der Schlange sofort in F\xc3\xa4ulnis \xc3\xbcber. Im Enddarm fand sich eine riesige Menge von Harns\xc3\xa4urekristallen gespeichert, obwohl w\xc3\xa4hrend der Krankheit des Tieres wiederholt gro\xc3\x9fe Portionen von Kot manuell aus der Kloake geholt worden waren.\nDr. G. BEUTEL (Berlin-Lichtenberg) \xc3\xbcbernahm freundlicherweise das R\xc3\xb6ntgen und die entsprechende Deutung. Es stellte sich \xe2\x80\x94 wie vermutet \xe2\x80\x94 tats\xc3\xa4chlich ein Wirbels\xc3\xa4ulenbruch heraus. Der betreffende Wirbel ist stark destruiert. Hier macht die Wirbels\xc3\xa4ule einen nach rechts gerichteten Knick (Abb. 4), und beim Seitenbild erkennt man au\xc3\x9ferdem eine Versetzung der beiden Wirbels\xc3\xa4ulenabschnitte in dorsoventraler Richtung um fast die volle Wirbels\xc3\xa4ulendicke (Abb. 5). Wolkige Schattenbildungen an diesem Abschnitt d\xc3\xbcrften Callus sein. Auf der Seitenaufnahme sieht man weiterhin multiple alte und frische Rippenfrakturen, von denen die letzteren durch kr\xc3\xa4ftigen Callus bereits \xc3\xbcberbr\xc3\xbcckt werden. In H\xc3\xb6he des destruierten Wirbels sind links mehrere Rippen zu sehen, die z.T. etwas aufgetrieben sind und zentrale Aufhellungen mit exzentrischer Verd\xc3\xbcnnung der Compacta aufweisen. Hierbei d\xc3\xbcrfte es sich um Enchondrome handeln. Soweit die Tatsachen und die Befunde.

Description: At the Royal Zoological Gardens \xe2\x80\x9cBlijdorp\xe2\x80\x9d at Rotterdam May 6th 1958 a Father David\xe2\x80\x99s Deer gave birth to a female calf. It was the first young of this three year old doe.\nDuring the days before the day of birth the doe was seen several times leaping upon the buck. Experience with other Ungulates has taught that such behaviour may be regarded as an indication that the time of delivery is approaching. On the day of birth the doe refused her food as has been observed in many other mammals. She lay down very often, gnashed her molar teeth and made movements with her head towards the belly and the udder, the ears flattened to the neck, as if she was suffering from cramps. One had the impression, however, that the expulsion of the young was kept back until the keeper went home and the door of the stable was closed. Apparently a great number of mammals prefer to give birth to their young in the quietest part of the space of 24 hours. For most mammals this is the evening or the night, but bats very frequently give birth during the day which is their time of rest (SLIJPER, 1959). A postponement of birth until all is quiet has frequently been observed in zoological gardens. In natural surroundings the Ringed Seal (Phoca hispida Schreb.) and other Seals are said to be able to postpone birth as long as 10 days if the weather is very bad (KRUMBIEGEL, 1947).

Description: 1. Extensors and flexors trochanteris of the second thoracic leg of Periplaneta americana were investigated physiologically and toxicologically. 2. The movements of the separate muscles were recorded with the aid of a special myographic technique. 3. Nerve muscle preparations of a completely fast and a nearly completely slow function type could be studied in this way. Some muscles represent a form in which both function types occur, probably mixed. When analysed, ryanodine appeared to be a valuable expedient. In some types of nerve muscle preparations inhibition could be demonstrated. 4. Linking up with what is known, it is reasonably certain that the action of high dosages of DDT actually takes place on motor axons or myoneural junctions and not on the muscle fibre itself. Not all of the different nerve muscle preparations seemed to be of the same sensitivity to this poison. 5. \xce\xb3-HCH appears to have a very slight influence on the function of the different types of isolated nerve muscle preparations. However, because of the intense motor activity the muscles become greatly fatigued.

Description: CONTENTS\nA. Introduction.................. 1\nB. History of Suriname Carcinology............ 4\nI. Popular literature............... 4\nII. Scientific literature............... 11\nIII. Economic literature............... 17\nIV. Collectors................. 17\nV. Expeditions................. 34\nC. Occurrence of Decapoda in Suriname.......... 41\nD. Economic Importance of Suriname Decapoda......... 43\nE. Enemies of Suriname Decapoda............. 44\nF. Vernacular Names................ 47\nG. Notes on the Species............... 49\na. Macrura.................. 49\nb. Anomura.................. 130\nc. Brachyura.................. 162\nH. Literature cited................. 277\nA.\nINTRODUCTION\nThe decapod fauna of the three Guianas (British, Dutch, and French) is very poorly known. A few scattered notes exist which deal with the crabs and shrimps of the region, but no comprehensive account of the Decapoda of any of the three countries has ever been published apart from Young\'s (1900) "The stalk-eyed Crustacea of British Guiana, West Indies and Bermuda", which, however, also covers the West Indian Islands and Bermuda (including the deep-water species), and furthermore is incomplete.

Description: A new species of Septobasidium is described, in relation with which the position of the genus Uredinella is discussed.

Description: A revision is given of the genera Auriscalpium, Hericium, Hydnum, and Sistotrema.\nHydnum heimii is described as a new species.

Description: Description et figures de Hydnellum auratile, combinaison nouvelle pour une esp\xc3\xa8ce longtemps oubli\xc3\xa9e, comparaison avec deux autres esp\xc3\xa8ces du m\xc3\xaame groupe et cl\xc3\xa9 de d\xc3\xa9termination.

Description: The author regards the Cyphellaceae as an artificial family. He redefines it for practical purposes, suggesting the gradual removal of those elements that show relationship with other groups; several elements are referable to the Corticiaceae or the agarics. A list of the \xe2\x80\x98cyphellaceous\xe2\x80\x99 generic names tentatively included is given. The genera to be excluded from the family as defined are briefly discussed. The same applies to a long series of specific names that had or have been included. A historic chapter reviews some important developments in regard with some of the older genera, Solenia, Cyphella, Aleurodiscus, as well as the rise of the family. Some species are transferred to Aleurodiscus Rab. ex J. Schroet.; Cytidia Qu\xc3\xa9l. is redefined and Auriculariopsis Maire excluded from it. Other genera reviewed and redefined are Stromatoscypha Donk [Porotheleum (Fr. per Fr.) Fr.], Chromocyphella De Toni & Levi Phaeocyphella Pat.], and Lachnella Fr. Two new monotypic genera are introduced, Cellypha Donk and Pellidiscus Donk. One or more species of the redefined and new genera are discussed. The name Mycena sect. Hirsutae (K\xc3\xbchner) ex Donk is validly published. Several specific names are reduced to the synonymy of other species for the first time. Several types of names published by Persoon and by von Albertini & von Schweinitz were studied. New combinations are made under Hymenochaete L\xc3\xa9v. (1), Favolaschia (Pat.) Pat. (1), Aleurodiscus (2), Cellypha (1), Pellidiscus (1), Chromocyphella (1).

Description: Lichenology in Great Britain nowadays rejoices in increased activity and interest. This is evidenced by the foundation of the British Lichen Society which came into being some time ago, and now runs its own journal, The Lichenologist. The present book is another example, and it certainly appears at an appropriate time.\nThe book which is written in clear and simple language contains a few introductory chapters (on the structure of lichens, the use of reagents and apparatus, and on the ecology), keys to orders and families, a descriptive part, a bibliography, a glossary, and an index, followed by the plates.

Description: Sediments in the foreland of a mountain chain are sometimes suited to reconstitute the conditions in these mountains at the time of deposition of the sediments. The present study gives the results of a sedimentological investigation of the Tertiary and Quaternary deposits in a part of the Duero basin, situated south of the Cordillera Cantabrica, which supplied the sediments. The aim was to determine both the conditions in the source area, and the environments in the area of deposition.\nThe investigated area is situated in the province of Palencia, between the rivers Pisuerga and Carri\xc3\xb3n. The area being a part of the so-called Meseta, has a simple relief. Two levels at different heights can be distinguished. The higher level, p\xc3\xa1ramo, is strikingly flat, the lower, campi\xc3\xb1a, is more undulating.\nThe Tertiary basin sediments are of various types, and can have six different facies.\nAlong the mountain foot the sediments are chiefly conglomerates with some sandstones, united into the Cuevas facies. The pebbles consist of limestones derived from the Cretaceous limestones, which in the E occupy extensive areas but in the W are only exposed in a narrow strip along the southern border of the mountain chain. At that time they must have formed the southern flank of the Cantabrian Mountains. Pebble roundness and flatness indicate for the greater part a deposition as river fans in a warm and rather dry climate. These conglomerates have been brought into an overturned position in the W of the investigated area, and were strongly tilted in the E. This tectonic deformation is thought by several authors to have occurred during the Savian orogenic phase. The younger beds, having the Cuevas facies, are nearly horizontal, and were deposited during and after this folding as appears from the presence of sandstone pebbles derived from the sandstone layers within the folded conglomerates.\nSouth of the limestone conglomerate belt a wide zone with red beds occurs. These sediments, consisting of an alternation of quartzite conglomerates and sandy layers, represent the Vega de Riacos facies. The change of deposit from a limestone conglomerate into a quartzite conglomerate may be due to changes in the supply area, the Mesozoic limestones having been eroded and having become covered with soils, and the Palaeozoic quartzites and conglomerates becoming largely exposed. A typical feature is the absence in all basin sediments of pebbles derived from the Carboniferous limestone, the so-called Brezo-limestone, which at present froms a great part of the southern flank of the Cantabrian Mountains. The sediments presenting the Vega de Riacos facies were deposited in a warm and humid monsoon climate, as appears from (1) the red colour, (2) the shape of the quartz sand grains, and (3) the clay mineral associations.\nThe remainder of the investigated area is characterized in the N by yellow sandy and clayey deposits, covered by similar, but yellow and red, sandy and clayey deposits, and in the S by yellow clayey deposits overlain by white and grey gypseous marls, alternating with limestones.\nThe underling yellow sandy and clayey sediments, typical for the Carri\xc3\xb3n de los Condes facies, are dated as Vindobonian on account of the fossils found near Palencia and Salda\xc3\xb1a. The upper yellow and red, sandy and clayey layers found in the N, having the Relea facies, have a Pontian age, based on fossils found near Salda\xc3\xb1a and Relea. In the E of the investigated area this Relea facies shows a local divergent aspect, called Zorita facies, characterized by an alternation of red, sandy deposits and white, marly deposits. The gypseous marls and the limestones in the S, which show the P\xc3\xa1ramos facies, overlying the yellow clayey sediments in Carrion de los Condes facies, have a cover of a very hard, bluish limestone, the P\xc3\xa1ramos-limestone, which provided some freshwater molluscs indicating also a Pontian age.\nThe sediments in the four last-named facies represent chiefly deposits of rivers and shallow temporary lakes (lagunas). A rather regular sedimentation went on from Vindobonian into Pontian times, meanwhile influenced by changes of climate in the basin. After the warm and humid climate in which the red beds were deposited, the climate became more arid, with an increased evaporation.\nFirst the yellow sediments in Carri\xc3\xb3n de los Condes facies were deposited, in the N being still sandy, in the S becoming more clayey. They are clearly deposits of rivers which did not supply very coarse material, but some deposition in temporary lakes must also have occurred.\nAt the end of the Vindobonian evaporation became stronger, as can be concluded from the lime crusts found in the upper layers in the area of the Carri\xc3\xb3n de los Condes facies, and more to the S, in the area of the P\xc3\xa1ramos facies, from the deposition of gypsum bearing marls, when the drainage was more or less restricted.\nThis climate persisted during the first part of the Pontian as can be concluded from lime crusts occurring in the lower beds in Relea facies, the depositional environment, that is rivers and lagunas, remaining the same.\nLater in the Pontian the humidity of the climate increased, as appears from the increasing number of red layers in this Relea facies. In the S this increasing humidity caused the precipitation of gypsum to cease, and at this time the P\xc3\xa1ramos-limestones were formed. The Zorita facies, which laterally replaces the Relea facies, is chiefly determined by a supply from a different source area, namely the Mesozoic calcareous rocks exposed a few kilometres N of the deposits in Zorita facies.\nThe heavy mineral associations (chapter VIII, part 1) are monotonous, practically consisting of resistant minerals. They seem to indicate a supply from NW to SE. Also the pebble supply followed this direction, as may be concluded from their size distribution within the red beds having the Vega de Riacos facies. This NW\xe2\x80\x94SE direction was the main drainage direction in Pre-Rhodanian times.\nThe clay minerals in the sediments presenting the various facies allow to draw some conclusions on the climates at the times of deposition. For instance, the rather righ percentage of kaolinite in the sediments in the Cuevas and Vega de Riacos facies, may indicate a warm and rather humid climate during and after deposition. But later alterations also influenced the clay mineral associations, causing a preponderance of illite (see chapter VIII, part 3).\nAfter the deposition of the P\xc3\xa1ramos-limestones the Duero basin became a non-depositional area. During the Rhodanian orogenic phase the bordering mountains were uplifted, and the basin was tilted towards the W. This caused a switch of the drainage pattern which before was directed towards the Mediterranean, and now became directed towards the Atlantic Ocean. During the whole of the Pliocene strong bevelling occurred, through which the p\xc3\xa1ramolevel in the basin and pediments at the foot of the mountain chains were formed.\nNext, a warm and dry climate characterized by sheetfloods must have prevailed all over the Meseta, causing the deposition of the angular quartzitic ra\xc3\xb1a pebbles, so well exposed in the investigated area on the ra\xc3\xb1a of Guardo. These ra\xc3\xb1as are presumed to be of Villafranchian age.\nSoon the influence of Quaternary changes of climate became evident. Certainly the younger river terraces, found at five various levels, are due to these Pleistocene climatic changes. Pebble analyses could confirm the opinion of various authors who admit only two real glaciations in the Spanish mountains, namely the last and the penultimate. Indeed, the two lower terraces contain pebbles which may have been formed in a periglacial climate, whereas the deposits of the three upper terraces only contain evidences of a humid, temperate climate.\nThe sedimentological data on which the conclusions on the depositional environments, as given above, are based can be found in the following chapters: (a) grain size distribution (chapter V), (b) pebble analyses (chapter VI), (c) morphometrical sand analysis (chapter VII), (d) mineralogy of the sands (chapter VIII, parts 1 and 2), (c) clay minerals (chapter VIII, part 3).\nThe development of the drainage pattern (see chapter IX) was reconstituted with the help of a number of captures, which can be observed in the field. In this way a gradual adjustment of the drainage to the present direction can be demonstrated. In the investigated area this adjustment occurred rather late during the Quaternary. At that time also the campi\xc3\xb1a-level was formed.\nFinally, in the last chapter (X), an attempt is made to establish the palaeoclimates, and the relief in the source area, though there remain many uncertainties.\nThe Cordillera Cantabrica, being a mountain area, must always have had a more humid climate than the basin. Even during the Upper-Vindobonian and Lower-Pontian, while the basin was arid, the climate in the mountains must have been more humid. This appears from the clastic sediments supplied into the basin (Relea facies). Though the drainage was restricted, it will not have been totally interrupted, because only calcite and gypsum were deposited in the basin centre, and no halite.\nThere will have been a certain relief in the source area during the whole time. The sediments give no indications for a fully developed peneplain. During the whole of Vindobonian and Pontian times clastic sediments have been supplied by the Cantabrian Mountains.

Description: In 1958 werden de karteringen in de Centrale Pyrenee\xc3\xabn en in het noorden van de provincie Leon (zuidrand Ast.-Cantabrisch Gebergte) voortgezet, het werk in Galici\xc3\xab niet.\nIn de Centrale Pyrenee\xc3\xabn werd een eerste verkenning in het Ribagorzana dal aangevangen, waarover hier nog niet gerapporteerd wordt. Het werk in het Segre dal werd voortgezet, terwijl de kartering van een klein ingewikkeld gebied in een oostelijk zijdal van de Pallaresa werd begonnen en be\xc3\xabindigd. De karteringen in het noorden van Andorra en over de grens in Frankrijk werden eveneens voortgezet.

Description: This paper deals with the slugs Alderia modesta (Lov\xc3\xa9n) and Limapontia depressa Alder & Hancock, both very common in the intertidal zone of the Dutch salt-marshes.\nVan Benthem Jutting & Engel did not mention them as native species in \xe2\x80\x9eFauna van Nederland\xe2\x80\x9d 8, a monograph on Dutch Opisthobranchia, published in 1936. Alderia and Limapontia do not belong to the order of Nudibranchia, but to a separate order, Saccoglossa (Ascoglossa). They possess an uniseriate radula, the worn teeth of which fall in a pouch (saccus, ascus). Their way of life is different, the Nudibranchs feed mainly on hydroids, sea anemones, bryozoa, sponges, etc.; only a few species e.g. Polycera quadrilineata O. F. M\xc3\xbcller feed on algae, while all west-european Saccoglossa feed exclusively on algae.

Description: Delias benasu Martin ist nicht nur eine der gr\xc3\xb6ssten und auff\xc3\xa4lligsten, sondern auch eine der seltensten Arten ihrer Gattung. Zudem f\xc3\xa4llt ihre Entdeckung reichlich sp\xc3\xa4t, n\xc3\xa4mlich in die erste Oktoberh\xc3\xa4lfte des Jahres 1912, sie fand statt beim Dorfe Boku, ,,wo die drei Landschaften von Mittel-Celebes Kolawi, Benasu und Besoa zusammenstossen". Die Ehre der Entdeckung geb\xc3\xbchrt dem deutschen Milit\xc3\xa4rarzte Dr. Ludwig Martin, im Dienste der fr\xc3\xbcheren Niederl\xc3\xa4ndisch-Indischen Regierung, der sich um die Erforschung der Rhopaloceren von Celebes und von Nord-Ost-Sumatra recht verdienstlich gemacht hat. Er hat die Art zwar nicht selbst gefangen, sondern berichtet bescheiden, dass ,,ein Sanit\xc3\xa4tssoldat mit einer Patrouille von 30 Bajonetten" sie ihm mitgebracht h\xc3\xa4tte, siehe Martin (1) 225. Die ganze Ausbeute bestand nur aus 3 \xe2\x99\x82\xe2\x99\x82, welche Martin 1.c. ausf\xc3\xbchrlich beschreibt. Ein Jahr sp\xc3\xa4ter bildet der Autor den Holotypus ab (2). Im Jahre 1919 f\xc3\xbcgt er noch hinzu (3) 63, ,,dass drei M\xc3\xa4nnchen im Jahre 1912 auf dem feuchen Ufersande eines kleinen Fl\xc3\xbcsschens" gefangen wurden. Diese 3 \xe2\x99\x82 \xe2\x99\x82 waren die einzigen Exemplare dieser merkw\xc3\xbcrdigen Art, die bis heute bekannt waren.\nSie gelangten mit Martens Sammlung, bei dessen Tod (1924), an die Zoologische Staatssammlung M\xc3\xbcnchen, ein \xe2\x99\x82 hiervon wurde an das Hill Museum abgegeben, das von Talbot in seiner Monographie (1) 29, 294 bearbeitet wurde. Der Holotypus, aus der M\xc3\xbcnchner Sammlung, konnte farbig abgebildet werden, Tafel 60, Figur 1. Das \xe2\x99\x82 aus dem Hill Museum befindet sich jetzt im Britischen Museum (Nat. Hist.).\nDem unerm\xc3\xbcdlichen und vortrefflichen Sammler Dr. L. J. Toxopeus kommt das Verdienst zu, die Art auf einer Sammelreise in Mittel-Celebes wieder entdeckt zu haben. Er hat zwar in seinemReiseberichte, siehe Toxopeus

Description: SCAMANDRA UNDULATA n.sp. \xe2\x99\x82, Ocre brun\xc3\xa2tre plus ou moins fonc\xc3\xa9 suivant les exemplaires; pattes brun noir\xc3\xa2tre. Face sup\xc3\xa9rieure de l\'abdomen plus ou moins rouge, avec au milieu une grande tache un peu plus fonc\xc3\xa9e. Les deux tiers ant\xc3\xa9rieurs des \xc3\xa9lytres sont havane, avec d\'assez nombreuses petites taches d\'un rouge fonc\xc3\xa9 et de tr\xc3\xa8s fins points noirs surtout visibles le long des grosses nervures; entre cette partie et la post\xc3\xa9rieure, une bande rouge p\xc3\xa2le, transversale, ondul\xc3\xa9e, pr\xc3\xa9sentant au milieu de la largeur une large convexit\xc3\xa9 vers l\'avant; la partie post\xc3\xa9rieure est un peu plus claire que l\'ant\xc3\xa9rieure; \xc3\xa0 la face sup\xc3\xa9rieure se voit une bande ros\xc3\xa9e, parall\xc3\xa8le au bord apical; \xc3\xa0 l\'inf\xc3\xa9rieure cette bande est blanche, les nervures sont jaunes ou ocre, sur celles-ci des fins poils noirs.\nAiles rouge ponceau, devenant brun\xc3\xa2tres vers l\'apex; une partie des nervures transversales est ocre p\xc3\xa2le; parall\xc3\xa8lement ou un peu en avant du bord apical, ainsi que le long du bord post\xc3\xa9rieur, une assez large bande blanche. \xe2\x99\x80, Les ailes ont la m\xc3\xaame couleur que les \xc3\xa9lytres, mais un peu moins fonc\xc3\xa9es, avec les m\xc3\xaames bandes blanches qui se voient chez les \xe2\x99\x82 \xe2\x99\x82.\nProlongement c\xc3\xa9phalique assez long, s\'\xc3\xa9tendant jusque pr\xc3\xa8s du bord post\xc3\xa9rieur du vertex, en c\xc3\xb4ne aplati, \xc3\xa0 surface stri\xc3\xa9e transversalement. Sur le front trois car\xc3\xa8nes mousses, la m\xc3\xa9diane visible dans la partie sup\xc3\xa9rieure, disparait un peu au-dessus du milieu de la longueur; la partie m\xc3\xa9diane comprise entre les deux car\xc3\xa8nes lat\xc3\xa9rales est plane et celle externe \xc3\xa0 ces car\xc3\xa8nes est en goutti\xc3\xa8re. Une car\xc3\xa8ne sur le clyp\xc3\xa9us. La protub\xc3\xa9rance de la base des tibias post\xc3\xa9rieurs est en c\xc3\xb4ne mousse, assez court; les tibias portent trois \xc3\xa9pines. Longueur du corps: \xe2\x99\x82, 15 mm, \xe2\x99\x80 17 mm; envergure: \xe2\x99\x82, 43 mm, \xe2\x99\x80, 53 mm.\nType: Sumatra: Poeloe Babi Simaloer; paratypes: ibid et Sinabang Sima-

Description: Subgenus Eukoramius Bryk Tibia mit stark zugespitztem, ihr Ende \xc3\xbcberragendem Schienenbl\xc3\xa4ttchen.\nR3 entspringt aus der vorderen Mittelzellrippe vor dem Zellende und verw\xc3\xa4chst in der N\xc3\xa4he des Fl\xc3\xbcgelvorderrands mit R1, trennt sich dann aber wieder und m\xc3\xbcndet im Apex. M1 entspringt direkt hinter dem Gabelstiel von R4 + R5 aus der Mittelquerrippe, ohne mit ihm zu verwachsen. Das VIII. Tergit des \xe2\x99\x82 sehr tief eingebuchtet, die Seitenlappen abgerundet. Uncus zweispitzig, seine H\xc3\xb6rner gegen die Basis nicht verbreitert. Valve mit caudal-dorsalem Fortsatz. Aedoeagus lang und schlank, mit kleinem Orificium. Sphragis braungelb, den Hinterleib ringf\xc3\xb6rmig umschliessend, ventral tief ausgeh\xc3\xb6hlt, die Seitenlappen am Rande von einer flachen Leiste eingefasst, die ventral und dorsal vorspringt und caudalw\xc3\xa4rts eingebuchtet ist.\nTad. (Euk.) imperator Oberth\xc3\xbcr (Bull. Soc. ent. France, serie 6 v. 3 p. 77) Die Art bewohnt Szetschwan, Thibet, Sikkim, Junnan. Amdo, Nanshan (Humboldkette) und Kansu.\nTad. (Euk.) imperator imperator Oberth\xc3\xbcr Tatsienlou 7 \xe2\x99\x82, f. ocelloconjuncta n.c. 5 \xe2\x99\x82, f. fermata n.c. 1 \xe2\x99\x82, f. fermata + analisconjuncta n.c. 1 \xe2\x99\x82, 17 \xe2\x99\x80, f. ocelloconnexa Bryk & Eisner 1 \xe2\x99\x80 Holotype = ocelloconjuncta n.c, 2 \xe2\x99\x80, f. ocello + analisconjuncta n.c. 3 \xe2\x99\x80, f. rubroocellata n.c. 1 \xe2\x99\x80, f. latecincta n.c. 1 \xe2\x99\x80, f. atroguttata n.c. 1 \xe2\x99\x80, f. ampliusocellulata n.c. 5 \xe2\x99\x80, f. minuscula n.c. 3 \xe2\x99\x80, f. ochreoocellata n.c. 1 \xe2\x99\x80, f. flavoocellata n.c. 2 \xe2\x99\x80, f. mediorubrodivisoocellata n.c. 1 \xe2\x99\x80; Watusi-Pass, Setzschwan f. rubroocellata n.c. 1 \xe2\x99\x80.\nGrosse, 36-41 mm, wenig digryphe Unterart, mit grauweissem Fl\xc3\xbcgelfond und weissen Fransen. \xe2\x99\x82 mit gestrecktem Vorderfl\xc3\xbcgel, dessen Vorderrand

Description: A visit paid in June 1956 to the British Museum (Natural History), London, and to the University Museum of Zoology, Cambridge, England, enabled me to study the types of several species of Pontonid and Palaemonid prawns, the identity of which thusfar was not known with certainty. In the present paper some of the results of these reexaminations are given.\nI wish to express here my sincere thanks to Dr. Isabella Gordon of the Crustacea Section of the British Museum, and to Dr. C. B. Goodhart of the University Museum of Zoology at Cambridge for the permission to study this valuable material and for their most cordial assistance.\nPericlimenes (Periclimenes) incertus Borradaile, 1915 Periclimenes (Cristiger) incertus Borradaile, 1915, Ann. Mag. nat. Hist. (8) 15: 210; Borradaile, 1917, Trans. Linn. Soc. Lond. Zool. (2) 17 : 364, pl. 53 fig. 7.\nPericlimenes (Periclimenes) incertus Kemp, 1922, Rec. Indian Mus. 24: 140, 150; Holthuis, 1952, Siboga Exped. 39 (a1o) : 9, 39.\nPericlimenes (Periclimenes) impar Kemp, 1922, Rec. Indian Mus. 24: 140, 147, textfigs. 16, 17, pl. 3 fig. 1; Kemp, 1925, Rec. Indian Mus. 27: 322; Holthuis, 1952, Siboga Exped. 39 (a1o) : 9, 38, fig. 7; Holthuis, 1955, Zool.\nVerhand. Leiden 26: 60, fig. 33a.\nIn his key to the species of the subgenus Periclimenes, Kemp (1922: 140) placed P. incertus in the group with "no teeth of upper rostral series situated on carapace behind orbit". However, in Borradaile\'s (1917) pl. 53 fig. 7, the posterior dorsal rostral tooth is shown as being placed behind the orbit.\nSince Kemp (1922: 150) stated that he had examined the type material of Borradaile\'s species, the possibility existed that the shape of the rostrum

Description: A new species of freshwater Bryozoa has been found at Patua, Sumatra by Dr. A. Holleman-Haye. It belongs to the genus Lophopodella which has an Aethiopean-Indian range.\nThe genus Lophopodella is characterised by its large oval statoblast, large capsule and broad annulus. This annulus possesses one or more spines at the poles. These spines are studded with very small anchor-like hooklets. The genus Lophopodella is closely related to the genus Pectinatella. The statoblasts of the latter genus may bear large spines without hooklets or, on the other hand, a great number of small spines (or hooklets) which are directly placed on and around the entire margin, as e.g. in Pectinatella gelatinosa Oka. Characteristic of the new species of Lophopodella is that the poles are studded with a number of hooklets, directly placed on to the margin. In this respect the species resembles Pectinatella gelatinosa and on this character the name of the new species is based. The species is an "intermediate" form between the genera Lophopodella and Pectinatella.\nThe close relationship is proved by the variability and the teratology of the statoblasts. Sometimes they already show the character of a more evolved species or, conversely, they recall a more primitive stage by their lack of characters.\nZoarium: a gelatinous mass, about 4 mm is diameter, lobate, the lobation originates from the base but also, probably as a result of incisures into the border; in peripheral lobation they do not reach very far into the lumen, they give the impression to be cicatrices of healed fissures.\nPolypides: about 21/2 mm long, tentacles numbering 50-70; about half of the total length; invagination is complete.

Description: In the earliest papers on neotropical Blattidae a fair number of specimens from Surinam were recorded (LINNAEUS, DE GEER \xc2\xb9), DE SAUSSURE, BRUNNER). But in the period from the beginning of this century up to now only a few scattered reports of Blattidae from that region have appeared in the literature of the subject. The present article will be the first to deal exclusively with Surinam species.\nThe material dealt with in this paper was mainly secured by DR. D. C. GEIJSKES between 1938 and 1955. His extensive travels both in the coastal area and far into the interior of Surinam enabled him to collect all over the country.

Description: Most of the material recorded in this paper was collected by the author during his stay in Suriname from 1949 to 1955.\nBy courtesy of Mrs. J. BONNE-WEPSTER, the author was enabled to study the Wyeomyia specimens which were collected by BONNE and BONNE-WEPSTER in Suriname and are at present in the collection of the Department of Tropical Hygiene and Geographical Pathology of the Royal Tropical Institute, Amsterdam. This material includes five holotypes and a number of paratypes.

Description: Two small but interesting collections of octocorals from the northeastern coast of South America have recently come into my hands through the U.S. Fish and Wildlife Service, one of them from a survey conducted by the Government of Surinam, the other from exploratory work of the U.S. Fish and Wildlife Service. The first was obtained off the coast of Surinam by Mr. J. C. HIGMAN, U.S. Fish and Wildlife Service observer aboard the motor vessel \xe2\x80\x9cCoquette\xe2\x80\x9d during the course of exploratory shrimp investigations. The second was obtained between Trinidad and the Amazon River, Brazil, through the efforts of Dr. GILES W. MEAD during the course of cruise 47 of the exploratory vessel \xe2\x80\x9cOregon.\xe2\x80\x9d Because there is so little information available dealing with the fauna of the northeastern coast of South America, it seems desirable to make known the records of Octocorallia taken by the \xe2\x80\x9cCoquette\xe2\x80\x9d and the \xe2\x80\x9cOregon\xe2\x80\x9d along this extensive and little known coast, together with a list of the species already reported in the literature. The four new species contained in the present material are described and figured in full, and figures of the spicules of the known species are given in support of the identifications set forth.

Description: The present paper embodies the results of a study of 362 specimens of the genus Rivulus from Suriname and the other Guyanas.\nSo far, 58 species names (morphological species or subspecies) have been proposed, by a great many authors; these names are listed on pages 52\xe2\x80\x9453. Of the 58, topotypical specimens have been examined in 8 instances. In order to facilitate a future review of the genus, which is in great need of revision, short remarks are made on the morphology and ecology of a number of specimens, from various localities, belonging to distinct species.

Description: In the second half of the nineteenth century an important contribution to our knowledge of the fauna of the Netherlands Antilles, and especially of St. Martin, was made by the medical officer of that island, H. E. VAN RIJGERSMA, whose name, however, has remained almost unknown to Dutch biologists. By assembling important zoological collections VAN RIJGERSMA enabled specialists to study the fauna of St. Martin and the neighbouring islands; as a result, this fauna was for a long time better known than that of many other West Indian islands.\nFrom information kindly placed at my disposal by the Rijksarchief (Netherlands State Archives) and the Record Office of the Ministerie van Zaken Overzee (Netherlands Ministry of Affairs Overseas) it appears that HENDRIK ELING (or ELINGSZ.) VAN RIJGERSMA was born in 1834 or at the beginning of 1835, and was very probably of Frisian origin. It is not known where he studied; but he practised on the island of Marken, in the Netherlands, as doctor, surgeon and obstetrician, until the year 1863. By Royal Decree No. 60, dated 26 June 1863, VAN RIJGERSMA was appointed Government Physician on the Dutch West Indian island of St. Martin, where he went in the autumn of 1863 with his wife and two children. He filled this post on St. Martin until his death on 4 March 1877, only once returning on furlough to the Netherlands, from Spring 1873 till March 1874. He was married to MARIA HENRIETTA GR\xc3\x84FING, probably from Amsterdam. At his death he left seven children. His widow continued to live on St. Martin until 1893, when she went back to the Netherlands with five of her children.

Description: The results of an investigation of the structure and sedimentology of Upper Westphalian and Lower Stephanian strata in the eastern end of the Cantabrian palaeozoic core (NW Spain), are presented.\nThe sediments, shales, sandstones, limestones and coal seams occur in three main associations: the orthoquartzite-carbonate, the turbidite and paralic associations. Two facies are dstinguished: a western, without turbidites, with relatively many coal seams and an eastern, with turbidites and a few coal seams.\nSome evidence for a zone of less subsidence is present. This zone separates the two facies. The western and eastern facies are represented by the rocks in the Sierra Corisa and Redondo synclines respectively. Between the two synclines occurs a zone of long stretched narrow folds, often upthrusted to the west. Fold axes generally plunge SSE. Some of the structural features are explained by disharmonic folding and extrusion tectonics.\nIn the eastern facies a formation occurs, which consists of graded sandstones alternating with mudstones.\nThickness measurements of the individual sandstone and mudstone beds are analysed with non-parametric statistical methods. Several regularities in the succession of lithological types or thicknesses are revealed. Correlations between thickness or position of variates (i. e. sandstone, mudstone, sideritic concretion) are tentatively explained in the light of the turbidity current hypothesis. Especially the successive sandstone thicknesses show an interdependence expressed in \xe2\x80\x9cfluctuations\xe2\x80\x9d. Sandstone-mudstone thickness-correlation leads to the assumption of a very high mud content of the turbidity current in these cases, and considerable erosion by successive currents.\nSedimentary structures, especially those of the turbidite association, are described in detail. A short annotated bibliography on sole markings is given.\nThe palaeocurrent directions measured from sole markings and cross-bedding are discussed. The sequence of sole-marking-directions on successive turbidite layers indicates interdependence of these dirctions, which could also mean the interdependence of the depositing currents.\nA litho-stratigraphic map, three structural sections and twelve stratigraphic sections are given.

Description: Geological and petrographical investigations were carried out in the northern part of the so-called Adula Nappe, one of the deepest Pennine nappes. The area under consideration lies in the SE of Switzerland, near Vals, S of Ilanz. This area is situated north of the Lepontinic gneiss-region, the deepest part of the Alpine orogen.\nThe rocks of the mapped area fall into four groups, viz gneisses; micaschists; amphibolites and allied rocks; and Mesozoic rocks, either of sedimentary or of igneous origin. The first three of these groups presumably represent metamorphic Hercynian or older rocks.\nStructurally three unites were distinguished, viz the Valserschuppen, the Fanellalappen and the Zervreilerlappen. The investigations clearly showed the important role of thrusting, isoclinal folding being of minor importance.\nThe fissure-filling and rock-making minerals, a. o., chloritoid, chloromelanite, ferrian phengite, garnet, crossite, glaucophane and ferrohastingsite, are described in chapter III. They are listed on p. 451.\nA petrographical description of the region is to be found in chapter IV. The four different groups of rocks are treated separately, with a summary at the end of each section.\nThe phengite-gneisses have a blastic structure pointing to a total recrystallization of the original granitoid material. Generally the feldspars do not show alteration. The large orthoclase porphyroclasts in some samples are assumed to represent relics of an older mineral assemblage.\nThe mica-schists show the influence of several different phases of metamorphism as witnessed by, e. g., the chloritization of garnets, the replacement of chloritoid by transverse muscovite, the occurrence of several successive generations of amphibole and the occurrence of biotite fringes around the muscovites.\nThe amphibolites and allied rocks vary in mineralogical composition. The latter comprise, a. o., sodium-pyroxene garnet rocks with occasional glaucophane and rocks rich in albite with subordinate quartz, amphibole and/or garnet. The amphibolites and allied rocks are mainly found between mica-schists and phengite-gneisses. The occurrence of zonal amphiboles and of very narrow veins filled with a different metamorphic mineral assemblage, points to a polyphasic metamorphic history. The mineral assemblage of such a narrow vein is assumed to have originated within a relatively short time and to represent a stable association of approximately contemporaneous minerals.\nThe Mesozoic rocks mainly comprise metamorphic carbonate-bearing sediments and metamorphic ophiolites. These rocks inform us about the age of a large number of metamorphic minerals, since these minerals can only have been produced during metamorphism of Alpine age. A list of such minerals is given on p. 521. The occurrence of zonal amphiboles, the replacement of chloritoid by garnet and that of chloritoid and garnet by chlorite, point to polyphasic metamorphism.\nChapter V treats the chemical composition of the various groups of rocks. If the chemical composition of the rock-making minerals is approximately known, the chemical composition of a sample can be calculated from the mode. In this way a number of chemical compositions of samples was added to those obtained by chemical analysis.\nA theoretical discussion of point counter analysis is given first. The results are summarized on p. 530\xe2\x80\x94531. In order to avoid correlation between the measurements it seems advisable to choose as the distance between the points, the diameter of the largest grains that occur in appreciable quantities, or any larger distance. The theory that the grain size is irrelevant in modal analysis, is disproved.\nIn chapter V 26 chemical analyses and 35 calculated analyses of rocks have been used to study the characteristic differences between the various groups by means of statistical methods. Differences in the chemical composition of both groups of rocks strongly suggest that the amphibolites did not derive from ophiolites. In view of their low potassium content it is highly improbable that the amphibolites represent a basic front of the phengitegneisses at their boundaries with the mica-schists. Hence it is the author\xe2\x80\x99s opinion that the amphibolites, the mica-schists and the phengite-gneisses have no genetical relation whatsoever.\nIn chapter VI the results of the mineralogical, petrographical and chemical investigations are combined in order to arrive at a synthesis. The rocks of the northern Adula region are shown to have been influenced by three successive phases of metamorphism of Alpine age. Some rocks even show traces of pre-Alpine metamorphism. The first Alpine metamorphic phase produced, a. o., glaucophane, crossite, sodium-pyroxene, garnet, epidote and chloritoid. The second phase is characterized by the production of, a. o., blue-green amphibole, ferrohastingsite, garnet, albite, epidote and biotite. The third phase produced, a. o., actinolite, chlorite, green biotite, epidote, zoisite and albite. The existence of these three Alpine phases was proved by making use of the following phenomena: (a) the occurrence of armoured relics; (b) the difference between the mineral assemblages of the host-rock and of narrow veins originated during the metamorphism; (c) the zonal habit of amphiboles; (d) the frequency of occurrence of a number of mineral associations in a group of about 300 samples, a result of a quantitative investigation with the aid of an International Business Machines equipment.\nThe amphibolites and allied rocks seem to be metamorphosed mafic igneous rocks of Hercynian or older age. Scanty evidence suggests that the phengite-gneisses are the products of metamorphism of Hercynian igneous rocks. The fact that the amphibolites are nearly always found between micaschists and phengite-gneisses might be explained by assuming a teetonical cause for this association.\nIn chapter VII some general aspects of the results obtained in the Adula region are discussed, as well as the bearing of these results on the geology and petrology of the southern part of the Swiss Alps. The tentative conclusion is reached that the Alpine glaucophane was produced simultaneously with the chloritoid and stilpnomelane of E. Niggli\xe2\x80\x99s different zones, whereas the blue-green amphibole may be contemporaneous with the kyanite and the coarse-flaky brown biotite of Alpine age. Consequently the typical minerals of Niggli\xe2\x80\x99s zones may be of different age. The distribution pattern of glaucophane in the Penninides and their immediate surroundings shows a conspicuous gap south of the Gotthard Massif, more or less coinciding with the area of brown biotite of Alpine age. This phenomenon may be connected with the occurrence of post-Palaeozoic granitoid rocks in the regions of Bellinzona and Tessin.\nMaps showing the distribution of glaucophane and lawsonite in Europe and in the rest of the world are added, as well as a bibliography giving localities of these minerals.

Description: Im Jahre 1953 setzten Crisp & Southward auseinander, dass hinsichtlich Arten aus dem Gezeitengebiet, Seestrassen bisweilen eine un\xc3\xbcberwindliche Sperre bilden. Crisp & Southward erl\xc3\xa4uterten diese Annahme u.a. mit den Beispielen der Seepocke Balanus perforatum Brugui\xc3\xa8re und der Napfschnecke Patella intermedia Jeffreys, Arten welche an der englischen S\xc3\xbcdk\xc3\xbcste vorkommen, jedoch in Irland fehlen und von welchen angenommen werden kann, dass es sich hier nicht um rezente Einwanderer handelt. Die Seepocke Elminius modestus Darwin, die sich w\xc3\xa4hrend des Krieges in England ansiedelte (Bishop, 1947) und sich dort schnell verbreitete, ist ein interessantes Objekt um diese Annahme zu pr\xc3\xbcfen. Die s\xc3\xbcdliche Nordsee sowohl wie der Kanal zeigten sich als Sperre nicht un\xc3\xbcberwindlich, obwohl f\xc3\xbcr beide F\xc3\xa4lle in Betracht gezogen werden k\xc3\xb6nnte, dass Elminius mittels des Schiffsverkehrs den Weg nach dem Kontinent fand, und nicht mittels eines Uebergangs der Nauplius-Larven (den Hartog, 1953, 1956). Ansiedlung an der irischen K\xc3\xbcste ist bisher ausgeblieben.\nDie Insel Helgoland in der Deutschen Bucht ist ebenfalls von einer Seesperre vom Festland getrennt; sie liegt ungef\xc3\xa4hr 40 km von den ostfriesischen Watteninseln Wangeroog und Scharnhorn entfernt, und ca. 60 km von Cuxhaven. Im Jahre 1953 wurde Elminius modestus zum ersten Male in Cuxhaven gefunden, vermutlich dahingebracht durch den Schiffsverkehr (K\xc3\xbchl, 1954). Bei einem Besuch an Helgoland im August 1955 zeigte es sich dass diese Art da schon vorhanden sei. Die Ansiedlung von Elminius hatte im Sp\xc3\xa4tjahr 1954 statt gefunden. Auf den st\xc3\xa4hlern Spundw\xc3\xa4nde des D\xc3\xbcnenhafens wurden n\xc3\xa4mlich ziemlich viele Exemplare von 3\xe2\x80\x945 mm gefunden, w\xc3\xa4hrend nur eine geringe Menge einer anderen Gr\xc3\xb6sse-Ordnung, 8\xe2\x80\x9411 mm, anwesend war. Der obere Teil dieser grossen Exemplare war stark mit Rost impr\xc3\xa4gniert, w\xc3\xa4hrend darunter ein breiter weisser Rand vorhanden war. Diese Rostimpr\xc3\xa4gnation deutet auf eine Periode von Hemmung im Wachstumsprozess hin: der Winter 1954\xe2\x80\x94\xe2\x80\x9955. Diese Tiere hatten alle gut entwickelte Gonaden. Die kleinen Exemplare ware alle sch\xc3\xb6n weiss und noch unfruchtbar. Obwohl wir Elminius auf fast alle geeigneten Stellen auf der D\xc3\xbcneninsel fanden, beschr\xc3\xa4nkten die Funde der mehrj\xc3\xa4hrigen Individuen sich ganz und gar auf die Spundw\xc3\xa4nde und das Holzwerk des D\xc3\xbcnenhafens und deren unmittelbare Umgebung. Auf der Felseninsel Helgoland war Elminius noch sp\xc3\xa4rlich vorhanden. Dort wurden nur einzige jungen, 3\xe2\x80\x944 mm grossen Individuen in dem Nord-Osthafen auf den Landungsbr\xc3\xbccken der D\xc3\xbcnenf\xc3\xa4hre gefunden; weiter auf einigen Stellen an der Schutzmauer.

Description: Some time ago Mr. G. M. Roding, director of the natural history museum at Enschede, sent me for identification two mandibular fragments with teeth of a large rodent collected in the clay pit at Needse Berg, province of Gelderland, by Mr. Ten Bokkel Huinink, the owner of the pit. The Neede Clay, Needian of Dutch terminology (Van der Vlerk and Florsch\xc3\xbctz, 1950, p. 149), is characterized by the abundance of the freshwater molluscs Viviparus diluvianus (Kunth) and Valvata naticina Menke; the scanty remains of large mammals found in this deposit, representing Elephas antiquus Falconer, Cervus elaphus L., and Dicerorhinus merckii (J\xc3\xa4ger), were described already half a century ago by Rutten (1909).\nThe Neede Clay corresponds to the great Mindel-Riss Interglacial; it is to be correlated with the English interglacial deposits of Clacton-on-Sea, Hoxne, and Swanscombe (Van der Vlerk, 1955, p. 37), and with those of Mauer and the main fauna of Mosbach in Germany (Azzaroli, 1951, p. 169). Both of these two last-mentioned localities yield Trogontherium cuvieri Fischer, an extinct beaver-like rodent, to which the mandibles from Neede should be referred.\nAbundant remains of another species of Trogontherium, T. boisvilletti (Laugel), have been described from the Tegelen Clay, province of Limburg, Netherlands, by Schreuder (1929); this deposit dates either from a G\xc3\xbcnz Interstadial (Schreuder, 1945) or from the G\xc3\xbcnz-Mindel Interglacial (Azzaroli, 1951, p. 169). In her last paper on Trogontherium, Schreuder (1951) refers the Pleistocene remains from the English and continental European localities west of the Rhine to T. boisvilletti, and those from the localities east of the Rhine to T. cuvieri.

Description: In the spring of 1947, during his stay on the Canary Islands, Dr. C. O. van Regteren Altena collected a small number of Opiliones on the Island of Tenerife, which he kindly permitted me to study. Most of these specimens are juveniles that could not be identified. Three species are, however, represented by adult specimens. I identified two of these with Metadasylobus fuscoannulatus (Simon) (localities : Barranco Andura (or Andola), south of Realejo, 17-III-1947, 1 \xe2\x99\x82, 3 \xe2\x99\x80 \xe2\x99\x80; Las Mercedes, about 650 m, 22-III-1947, 1 \xe2\x99\x82), and Bunochelis longipes Roewer (localities: La Paz, near Puerto Orotava, 12-III-1947, 1 \xe2\x99\x82; Icod el Alto, about 500 m, 25-III-1947, 1 \xe2\x99\x82) respectively.\nThe third species appeared, however, to be new to science; it is dedicated to its collector. I classify it with Bunochelis, a genus in which the first joint of the chelicerae of the male has a dorsal protuberance. Bunochelis altenai nov. spec. is described and figured in the present paper, whilst in a key a comparison is made with other species of the genus. I am greatly indebted to Prof. Dr. C. F. Roewer for his kind assistance in the study of the new species. The material is preserved in the Rijksmuseum van Natuurlijke Historie, Leiden.\nBunochelis altenai nov. spec. (fig. 1a, b, c) Material. Barranco Andura (or Andola), south of Realejo Alto, Tenerife, Canary Islands, 17-III 1947, 1 \xe2\x99\x82 (holotype); 1 subadult \xe2\x99\x82 (paratype).\nDescription. Length of the male (without chelicerae) : 4.2 mm.\nCephalothorax whitish with a pattern of light and dark brown spots: it bears a number of denticles (fig. 1a). Supracheliceral laminae each with one denticle. Ocularium brown with two longitudinal rows of 5-7 denticles.\nAbdomen dorsally whitish, with 5 transverse rows of denticles, of which

Description: In the keys to the palaearctic Saldidae, which will be published before long in Dr. W. Stichels: "Illustrierte Bestimmungstabellen der Wanzen Europas", I shall use systematic conceptions, deviating from those which were up till now generally used. The character of the work mentioned does not permit a motivation. The following notes serve as an introduction to the system, as proposed in Stichel.\n\nCONTENTS\nI. Major classification. A. Relation to other families B. Subfamilies C. Tribes II. The problem of generic divisions.\nIII. On the status of some palaearctic forms.\nIV. Saldula heijningeni spec. nov.\nI.\nMAJOR CLASSIFICATION\nA. Relation to other families A study of the egg development (position of germband, blastokinesis and eclosion) of Saldidae and other families (not published) has shown that the hypothesis of China (1950) that the saldids should belong to the Amphibicorisae, is justified. Of old they have been treated as representatives of the Geocorisae.\nB. Subfamilies Up till now the division in Saldinae Van Duzee 1917 and Saldoidinae Reuter 1912 has always been in use. To the latter belongs only the genus Saldoida Osborn 1901, while under the former all remaining (momently 15) genera are grouped. The three species of Saldoida have always attracted

Description: SYNOPSIS\nThe type slide of the species Fedrizzia helleri briefly described by Oudemans 1929 from Paramaribo, Dutch Guiana, but never figured, has been re-examined. The species is now shown to belong not to the genus Fedrizzia Canest. (fam. Fedrizziidae) but to the genus Klinckowstroemiella Turk 1951 (fam. Klinckowstroemiidae).\nThe species Fedrizzia helleri was briefly described by Oudemans 1929 as follows: "Fedrizzia helleri nov. sp. Er is geen scherp begrensd sikkelvormig scutum verticale; wel is dit gedeelte naar den voorrand membraneus; die voorrand is niet zuiver rond, maar iets golvend; er zijn 4 stralende vertikaalhaartjes op geplaatst, die op gelijke afstanden van elkander staan. Verder is de rug haarloos. \xe2\x99\x80 genitaalopening trapezoidaal, v\xc3\xb3\xc3\xb3r bijna even breed als de rechte achterrand van het sternale, en breeder dan achteren; zij wordt door 4 driehoekige schildjes gedekt (teeken in gedachte de diagonalen in het trapezium). \xe2\x99\x82 genitaalopening als bij Fedrizzia laevis Can. 1884, maar precies tusschen de coxae III (bij laevis nog iets meer naar achteren) \xe2\x80\x94 Op Passalus sp., Paramaribo; Juli; C. Heller legit".\nIn her Catalogue of 1945 of the Acari in the Oudemans collection in the Leiden Museum, Dr. A. M. Buitendijk indicates that drawings of this species have been published but I am informed by Dr. L. van der Hammen of the Leiden Museum that this is an error and that no figures exist.\nExcept for the reference by Sellnick 1938 in which he suggests that on the structure of the genital shields in the female, helleri belongs to his genus Eufedrizzia which he erected for the species Trachyuropoda tricuspis Banks 1914 from a Passalid from Brazil, no references appear to have been

Description: The genus Staurophlebia was established by BRAUER (1865, 1866) from his species magnifica from Brazil, a name which later proved to be a synonym of reticulata (Burmeister 1839), (see under this species). In his notes on St. magnifica, HAGEN (1867) said that SELYS (MS) has proposed the genus name Megalaeschna for Aeschna reticulata Burm., Ae. gigas Rbr. (= reticulata), and Ae. gigantula Selys, a closely related new species which was subsequently described by MARTIN. However, Megalaeschna is a synonym of the earlier name Staurophlebia, as already pointed out by COWLEY (1935). In his classification of the aeschnines, SELYS (1883) includes the two subgenera Neuraeschna and Staurophlebia in his genus Staurophlebia s.l., while KIRBY (1890), CALVERT (1905), and MARTIN (1909) give Staurophlebia s.str. generic rank, with St. reticulata Burm. as the genotype.\nThe characters of this genus are as follows: Wing venation: subcosta prolonged beyond the nodus to the first or second postnodal cross vein. Median space free. Triangle long, with 6\xe2\x80\x948 cells. M2 curved upward proximal to stigma. Rs forked proximal to stigma, enclosing in its fork 3\xe2\x80\x944 rows of cells; Rspl curved, between Rs and Rspl 5\xe2\x80\x946 rows of cells at maximum. Anal loop with 12\xe2\x80\x9418 cells. Anal triangle in male 3-celled. Pterostigma small, longer in fore wing than in hind wing. Large (75 mm) to very large (96 mm), stoutly built species, green, brown and blue-coloured. In general, head and thorax light-green, abdomen (except the first two segments) red-brown, bluish green, or dull blue. Frons prominent, marked with T-spot. Eyes connected for a long distance, occipital triangle small. Abdomen long-cylindrical, male with auriculae on segm. 2 and moderately narrowed at segm. 3. Male appendices superiores long, leaf-like, with a hooked middle process on upper side half-way down their length, and an erect denticulate crest at the distal end, along the inner margin. Inferior appendage long-triangular, reaching to 1/3, mostly to 2/3, the length of the superiores. There is a basal prominence of the inferior appendage just between the bases of the app. sup. in the male. App. sup. of the female lanceolate, entire. Abd. segm. 10 of female with a long, two-pronged, ventral process.

Description: The present report is based in the first place on material collected by the trawler \xe2\x80\x9cCoquette\xe2\x80\x9d, which, from April to August 1957, explored the offshore waters of Suriname and French Guiana from the mouth of the Nickerie River in the west to the Iles de Salut in the east. Most of the hauls were made at a distance of 20 to 30 miles from the coast. The paper also considers the Stomatopoda collected off the Suriname coast by the Suriname Fisheries Service.\nTo date, only one species of stomatopod has been reported from Suriname, viz. \xe2\x80\x9cGonodactylus chiragra Fabr.\xe2\x80\x9d, so named by NEUMANN (1878, p. 39), who reported on a specimen which is preserved in the collection of the Heidelberg Museum and was said to have originated from Suriname. As has been shown by HOLTHUIS (1959, p. 14) NEUMANN\xe2\x80\x99S so-called Suriname material is very likely incorrectly labelled, and was more probably collected in the West Indian Islands. Accordingly, this record had better be ignored.

Description: This contribution may be considered as an Appendix to my paper on \xe2\x80\x9cTenebrionid Beetles of Cura\xc3\xa7ao, Aruba, Bonaire, and the Venezuelan Islands\xe2\x80\x9d, which was published in the fifth volume of this series (1954).\nThe addition has proved to be justified after study of: 1. a collection of Tenebrionids gathered by Dr. H. J. MAC GILLAVRY, Professor of Geology at Amsterdam University, as a student member of an excursion that took place in 1930 under the direction of the late Prof. L. M. R. RUTTEN; 2. some additional material collected by Dr. P. WAGENAAR HUMMELINCK; 3. specimens from the collection of Ir. R. H. COBBEN, entomologist and agriculturist of Wageningen, in 1957; 4. material collected by B. DE JONG, biologist at Cura\xc3\xa7ao, and other sources.

Description: J\xe2\x80\x99ai r\xc3\xa9cemment re\xc3\xa7u du Dr. P. WAGENAAR HUMMELINCK de Utrecht environ 230 exemplaires (larves, nymphes et fourreaux vides) d\xe2\x80\x99un Helicopsyche, recueillis par lui-m\xc3\xaame en 1936 en quelques localit\xc3\xa9s de l\xe2\x80\x99\xc3\xaele de Margarita (Venezuela). Gr\xc3\xa2ce au fait que les armatures g\xc3\xa9nitales du \xe2\x99\x82 et de la \xe2\x99\x80 purent \xc3\xaatre trouv\xc3\xa9es chez une paire de nymphes, le probl\xc3\xa8me de l\xe2\x80\x99appartenance sp\xc3\xa9cifique de cet insecte p\xc3\xbbt \xc3\xaatre \xc3\xa9lucid\xc3\xa9; il s\xe2\x80\x99agit d\xe2\x80\x99une nouvelle esp\xc3\xa8ce. Nous remercions vivement le Dr. P. WAGENAAR HUMMELINCK pour le mat\xc3\xa9riel et pour les indications \xc3\xa9cologiques, ainsi que le Dr. D. E. KIMMINS du British Museum pour les pr\xc3\xa9cieuses indications qu\'il nous a aimablement donn\xc3\xa9 sur la forme que nous d\xc3\xa9crivons, apr\xc3\xa8s avoir consult\xc3\xa9 nos dessins.

Description: In this article the results of a study on boulder-clay in the neighbourhood of Winschoten (N.E. Netherlands) are communicated (Chapter I).\nThe underlying sediments of the boulder-clay in this area consist of fine preglacial sands and black clay. In the nuclei of the many drumlins a strongly ice-pushed boulder-clay may be encountered (Chapter II).\nPalynological analysis showed the pollen content of the boulder-clay to be very small. In a few samples more pollen was found (Plates I and II), but in these cases there appeared to be an admixture of black clay, obviously picked up by the land-ice. This black clay (the so-called potklei or pottery clay) is very humic and resembles the Lauenburg clay from Germany, but is younger.\nUsing pollen analysis only one would date this clay as Miocene or even older (Plates II and III). This is impossible however, for in borings in this area Pleistocene sediments underneath the potklei are encountered.\nThe solution of the problem is that we are dealing bere with secondary pollen material, originating from the Miocene in N.W. Germany; this pollen was transported by rivers before the land-ice came (Chapter III).\nGranulometric analysis proved the boulder-clay of Winschoten to be the normal Dutch type. As far as we know this boulder-clay was deposited during the Saale glacial (Chapter IV).\nThe erratics in two samples were carefully examined. To this purpose the erratics from 6 mm \xe2\x80\x94 5 cm were counted (according- to the Madsenmethod 1897); the results were arranged in such way that a comparison with the countings from De Waard (1947) in the N.O. Polder could be made. Therefore the percentages of the various groups of erratics taken from the total content of erratics were compared with each other (Chapter V).\nFig. 4 shows the countings. It will be seen that the number of crystalline erratics in the boulder-clay from Bovenburen is considerably smaller, the sandstone and quartzite content far greater than that found in the boulder-clay from the N.O. Polder. In the field too, this was striking. We might speak of a local association of erratics in the grey boulder-clay at Bovenburen.\nThe analysis of the light fraction (Chapter VI) gave the following data: the composition of the samples, the roundness and dullness of the quartz grains correspond with the data from the normal grey boulder-clay (Table VI).\nThis agrees with the fact that the microfossils mentioned in this article were only found in grey boulder-clay. A small admixture of red boulder-clay is possible however, on account of an occasional find of some brown bryozoa and ostracoda characteristic for the red boulder-clay. Moreover the identification of the bryozoa indicated that fine components of the boulder-clay we examined originated from an area (Denmark and S. Sweden) with Danian and Upper Senonian outcrops (Table V).

Description: Cap\xc3\xadtulo 1. Introducci\xc3\xb3n Se han ejecutado investigaciones geomorfol\xc3\xb3gicas en la parte meridional de la Cordillera Cant\xc3\xa1brica (dib. 1), en el terreno drenado por el tramo superior del R\xc3\xado Pisuerga, por el R\xc3\xado Camesa, afluente del mismo, y por el R\xc3\xado Rubag\xc3\xb3n, afluente del R\xc3\xado Camesa. Se encuentra la regi\xc3\xb3n investigada en la zona donde se halla el l\xc3\xadmite entre las rocas Paleozoicas y las Mesozoicas de la Cordillera (mapa 2). M\xc3\xa1s hacia el Sureste, desde Cervera de Pisuerga se extiende una zona de rocas Mesozoicas plegadas, llamada por Ciry (1939) : \xe2\x80\x9dLe Pays Pliss\xc3\xa9\xe2\x80\x9d (mapa 1). Es una zona de relieve intermedio, ni tan alto como la Cordillera Cant\xc3\xa1brica, ni tan llano como la Meseta, que se encuentra m\xc3\xa1s hacia el Sur de dicha zona.\nExiste una gran diferencia geomorfol\xc3\xb3gica entre las vertientes septentrional y meridional de la Cordillera Cant\xc3\xa1brica, como resultado de la situaci\xc3\xb3n alta de la Meseta. Los r\xc3\xados de la vertiente norte en una recorrida de cerca de 50 kil\xc3\xb3metros llegan el Mar Cant\xc3\xa1brico y as\xc3\xad pasan un desnivel de m\xc3\xa1s de 1300 metros; los r\xc3\xados de la vertiente sur se dirigen a la Meseta que aqu\xc3\xad, en su parte norte, tiene una altura de 1000 metros. Es decir, poco m\xc3\xa1s o menos, en la misma recorrida, los r\xc3\xados pasan un desnivel que es 1000 metros menor que el de los r\xc3\xados de la vertiente norte. Como resultado, los valles de la parte norte est\xc3\xa1n profundamente agrietados, con considerables pendientes, caracteriz\xc3\xa1ndose la parte sur por amplios valles, con suaves pendientes; es la misma altura topogr\xc3\xa1fica, pero el fondo de los valles se encuentra a unos 1000 metros m\xc3\xa1s alto que en la parte norte (dib. 2).\nMenos pronunciado, pero tambi\xc3\xa9n claramente visible es el contraste en relieve con la regi\xc3\xb3n de la cuenca del R\xc3\xado Ebro, que limita la cuenca del Camesa en el norte y noreste.\nEl clima de la regi\xc3\xb3n considerada forma la transici\xc3\xb3n entre el clima de tipo atl\xc3\xa1ntico de la costa cant\xc3\xa1brica, y el clima semi-\xc3\xa1rido del interior de la Meseta. En dib. 3, el clima de Cervera de Pisuerga y de Reinosa est\xc3\xa1 ilustrado gr\xc3\xa1ficamente (seg\xc3\xban F. Hern\xc3\xa1ndez Pacheco, 1944).\nLa cartograf\xc3\xada de las unidades morfol\xc3\xb3gicas ha sido realizada a base del Mapa de Espa\xc3\xb1a, escala 1:50.000. Las hojas utilizadas se presentan en dib. 1. La naturaleza litol\xc3\xb3gica de los cantos de terrazas fluviales fu\xc3\xa9 determinada en los cantos mayores de 2 cms de di\xc3\xa1metro; el \xc3\xadndice de desgaste fu\xc3\xa9 determinado en los cantos mayores de 4 cms de di\xc3\xa1metro. Es para eliminar la influencia de las pudingas tri\xc3\xa1sicas que no hemos considerado los menores de 4 cms (ve\xc3\xa1se Cap\xc3\xadtulo 3).\nSe calcula el desgaste mediante la f\xc3\xb3rmula de Cailleux: Ie = 2re . 1000/L La granulometr\xc3\xada de arenas y arcillos fu\xc3\xa9 realizada por el m\xc3\xa9todo de \xe2\x80\x9ccriba-pipeta\xe2\x80\x9d; los resultados son representados por curvas logar\xc3\xadtmicocumulativas.\nEl desgaste de los granos de cuarzo se obtuvo de la misma manera que el desgaste de los cantos rodados; el examen de las muestras se ejecut\xc3\xb3 bajo el micr\xc3\xb3scopo binocular.\nLa determinaci\xc3\xb3n de los minerales densos se hizo de la manera acostumbrada.\nCap\xc3\xadtulo 2: Geolog\xc3\xada Las m\xc3\xa1s importantes caracter\xc3\xadsticas geol\xc3\xb3gicas de la regi\xc3\xb3n investigada se describen en este cap\xc3\xadtulo, seg\xc3\xban las investigaciones de los autores Karrenberg (1934), Ciry (1939), Quiring (1939), De Sitter (1955 y 1957) y Kanis (1956).\nRocas cristalinas apenas si se encuentran. El Dev\xc3\xb3nico se halla en la parte NO de la cuenca del R\xc3\xado Pisuerga y se compone de areniscas cuarcitosas y cuarcita, alternando con calizas. En el Carbon\xc3\xadfero tres unidades litol\xc3\xb3gicas pueden distinguirse : calizas masivas y cristalinas, conglomerados de gran espesor (el llamado conglomerado Curavacas) y una alternaci\xc3\xb3n de pizarras, areniscas y conglomerados, a veces tambi\xc3\xa9n de calizas. Se compone el Permo-Tri\xc3\xa1sico de conglomerados m\xc3\xa1s finos y claramente distintos de los Carbon\xc3\xadferos, y de areniscas gruesas, de color rojizo. El Keuper principalmente se compone de margas y arcillas; el Jur\xc3\xa1sico de calizas bien estratificadas y de margas. El Wealden tiene una litolog\xc3\xada muy caracter\xc3\xadstica, componi\xc3\xa9ndose de conglomerados finos de cuarzo y cuarcitas, calizas lacustrinas, y areniscas bastante gruesas. Est\xc3\xa1 mal cementado, de modo que por la alteraci\xc3\xb3n se forman f\xc3\xa1cilmente arenas y cascajos. El Cretaceico superior s\xc3\xb3lo se encuentra en unos lugares, como al Sur de Cervera de Pisuerga. Se compone, generalmente, de calizas.\nLas estructuras de la fase Sud\xc3\xa9tica (llamada la fase Curavacas por De Sitter) tienen una direcci\xc3\xb3n E\xe2\x80\x94O, las de la fase Asturiana (fase Pe\xc3\xb1a Cilda) una direcci\xc3\xb3n NNO\xe2\x80\x94SSE. Las deformaciones Terciarias son visibles en la regi\xc3\xb3n del Valdecebollas, pero quedan sin datar.\nCap\xc3\xadtulo 3: Alteraci\xc3\xb3n, denudaci\xc3\xb3n y formaci\xc3\xb3n de pendientes en diversos tipos de rocas La Caliza de Monta\xc3\xb1a forma el relieve en toda la Sierra del Brezo. En ning\xc3\xban lugar hemos hallado sedimentos con derrubios derivados de esta Caliza, salvo en una brecha situada al pie de su vertiente meridional. Las pendientes de denudaci\xc3\xb3n (\xe2\x80\x9cRichter-slopes\xe2\x80\x9d, cot\xc3\xa9jese Bakker, 1952) de esta Caliza son muy caracter\xc3\xadsticas, con \xc3\xa1ngulos de inclinaci\xc3\xb3n de 25\xe2\x80\x9430\xc2\xb0 (dib. 5). Otras calizas Paleozoicas, por encontrarse m\xc3\xa1s aisladas, tienen menos importancia en relaci\xc3\xb3n con la formaci\xc3\xb3n o deformaci\xc3\xb3n de pendientes.\nEn el conglomerado Curavacas, que se encuentra en una regi\xc3\xb3n extendida, las pendientes de denudaci\xc3\xb3n pueden tener los \xc3\xa1ngulos m\xc3\xa1s variados, pero las transiciones son siempre suaves. Los conglomerados Tri\xc3\xa1sicos son m\xc3\xa1s finos y m\xc3\xa1s compactos, de suerte que reaccionan de manera completamente diferente en la eflorescencia. En el conglomerado Curavacas la \xe2\x80\x9cmatriz\xe2\x80\x9d de los cantos se pulveriza, de manera que los cantos individuales son librados, los conglomerados Tri\xc3\xa1sicos, al contrario, reaccionan a lo largo de diaclasas, de tal manera que se forman cantos compuestos de conglomerado Tri\xc3\xa1sico. Las pendientes de denudaci\xc3\xb3n en las rocas Tri\xc3\xa1sicas son de perfil sencillo, rectilinear o suavemente curvado (dib. 5).\nLas esquistas Paleozoicas no tienen gran resistencia contra la alteraci\xc3\xb3n; r\xc3\xa1pidamente se descomponen en arcillas, pero por la fuerte erosi\xc3\xb3n generalmente desaparece la arcilla formada, dejando la roca expuesta a nueva alteraci\xc3\xb3n. Por eso, la mayor\xc3\xada de las pendientes de esquistas es muy compleja, no existe un tipo general. Las areniscas forman en muchos sitios interrupciones de las pendientes, a causa de su mayor resistencia. La composici\xc3\xb3n de los minerales densos de unos productos de alteraci\xc3\xb3n se presenta en dib. 7.\nCap\xc3\xadtulo 4: Fen\xc3\xb3menos glaciarios y periglaciarios Los fen\xc3\xb3menos glaciarios de la regi\xc3\xb3n investigada han sido estudiados ampliamente por F. Hern\xc3\xa1ndez Pacheco (1944), junto con los del valle de Campo de Suso. Por eso, no nos hemos ocupado intensivamente de tales fen\xc3\xb3menos.\nFen\xc3\xb3menos periglaciarios se observan en toda la regi\xc3\xb3n. Hay bloques de dimensiones impresionantes (dib. 10), que se han deslizado suavemente hacia abajo sobre un suelo permanentemente helado, bloques que se encuentran, sobre todo, en las regiones m\xc3\xa1s elevadas. Luego hay \xe2\x80\x9cdellen\xe2\x80\x9d, valles secos de perfil transversal de forma concava (Schmitthenner, 1925), entre los cuales pueden distinguirse dos tipos: el tipo \xe2\x80\x9chamaca\xe2\x80\x9d y el tipo de \xe2\x80\x9csuelo llano\xe2\x80\x9d (dibs 11 y 12, respectivamente). El suelo de estos \xc3\xbaltimos es m\xc3\xa1s llano que el de los primeros, pero tambi\xc3\xa9n concavo. Finalmente, la soliflucci\xc3\xb3n ha sido muy activa en toda la comarca. Es dif\xc3\xadcil observar, d\xc3\xb3nde s\xc3\xb3lo ha sido activa bajo el clima periglaciario, y d\xc3\xb3nde todav\xc3\xada sigue activa como \xe2\x80\x9csoil creep\xe2\x80\x9d, el que hemos encontrado en muchos sitios.\nCap\xc3\xadtulo 5: Descripci\xc3\xb3n de las terrazas del R\xc3\xado Pisuerga El R\xc3\xado Pisuerga se caracteriza por la presencia de numerosos restos de terrazas fluviales. Pueden agruparse en los niveles siguientes: La terraza HP altura relativa 120\xe2\x80\x94150 m \xe2\x80\x9e \xe2\x80\x9e LH \xe2\x80\x9e \xe2\x80\x9e 80-100 \xe2\x80\x9e \xe2\x80\x9e \xe2\x80\x9e HM \xe2\x80\x9e \xe2\x80\x9e 50\xe2\x80\x9455 \xe2\x80\x9e \xe2\x80\x9e \xe2\x80\x9e MM \xe2\x80\x9e \xe2\x80\x9e cerca de 40 \xe2\x80\x9e \xe2\x80\x9e \xe2\x80\x9e LM \xe2\x80\x9e \xe2\x80\x9e 20\xe2\x80\x9430 \xe2\x80\x9e \xe2\x80\x9e \xe2\x80\x9e HL \xe2\x80\x9e \xe2\x80\x9e 5\xe2\x80\x9410 \xe2\x80\x9e \xe2\x80\x9e \xe2\x80\x9e Baja \xe2\x80\x9e \xe2\x80\x9e hasta 5 \xe2\x80\x9e Dibujo 13 representa un perfil longitudinal del R\xc3\xado Pisuerga, con la proyecci\xc3\xb3n de las terrazas. El n\xc3\xbamero de cada una de las partes individuales corresponde con el n\xc3\xbamero de la descripci\xc3\xb3n en Cap\xc3\xadtulo 5.\nTerraza HP. Las partes de Herreruela (1) y San Felices (2) son casi libres de sedimentos. Al NO del Pantano de Va\xc3\xb1es se encuentran las partes de Polentinos (3) que est\xc3\xa1n cubiertas de un mezclado de cantos cuarcitosos, Tri\xc3\xa1sicos y areniscos. Al NO de Cervera de Pisuerga se encuentra la parte de Cervera (5) (dibs. 14 y 15), formada de una llanura alta, de dimensiones impresionantes, cubierta de una capa de gravas fluviales, principalmente cuarcitosas, de un espesor de 12\xe2\x80\x9414 metros. Al otro lado del valle del Pisuerga se halla la parte de Rabanal (6) que resulta la continuaci\xc3\xb3n de la parte de la Cervera. Al Sur del valle del R\xc3\xado Rivera se hallan las partes de Vado y de Dehesa (7) (dib. 16), que claramente son del mismo nivel. La altura relativa es la misma que la de la parte de Cervera, igualmente existe la cobertura sedimentaria de cantos cuarcitosos, encontr\xc3\xa1ndose en ella cantos del conglomerado Tri\xc3\xa1sico en una proporci\xc3\xb3n de menos de 1 %. Es importante esta presencia, porque indica que anteriormente el llamado Pisuerga Alto (el r\xc3\xado tal como exist\xc3\xada en la \xc3\xa9poca de sedimentaci\xc3\xb3n de la terraza HP) desde Cervera continuaba en direcci\xc3\xb3n sur, pasando por el Puerto del Brezo, que es la depresi\xc3\xb3n marcada entre las rocas Mesozoicas del Mariserrana, y las calizas Carbon\xc3\xadferas de la Sierra del Brezo. M\xc3\xa1s hacia el Sur se ensancha la terraza y queda menos claramente visible. Esta parte ha sido estudiada por Mabesoone (1959).\nLa terraza LH s\xc3\xb3lo se halla cerca de Cervera (4), a una altura relativa de 80\xe2\x80\x94100 metros; se caracteriza por la ausencia de cantos, estando la superficie formada en un sedimento arenisco que tambi\xc3\xa9n se encuentra bajo la terraza HP. Parece que este sedimento es de m\xc3\xa1s edad que la terraza HP. Cerca de Lig\xc3\xbcerzana, se halla una parte de la terraza LH a una altura de cerca de 80 metros sobre el nivel del r\xc3\xado; aqu\xc3\xad los cantos cuarcitosos tienen un espesor de cerca de 2 metros. Al Sureste de Salinas, se hallan restos de la terraza LH en las partes de Barrio (13) y de Hum\xc3\xadn (15). En las dos, los cantos son escasos; sin embargo, la cobertura sedimentaria alcanza un espesor de 3\xe2\x80\x944 metros.\nLas terrazas intermedias. El nivel HM se encuentra en las partes de San Mames (14) y de Frontada (16). Hay una cobertura de sedimentos fluviales, de un espesor de 2 a 3 metros. El nivel MM se halla en las partes de Barcenilla (11) y Salinas (12). Aqu\xc3\xad tambi\xc3\xa9n el sedimento tiene un espesor de 2\xe2\x80\x943 metros. El nivel MM se ha conservado en sitios aislados (8, 9, 17).\nLa terraza Baja. El nivel HL s\xc3\xb3lo se encuentra al NE de Aguilar; la terraza propiamente dicha se presenta casi en todas las partes del tramo del R\xc3\xado Pisuerga, salvo en el tramo superior (cot\xc3\xa9jese mapa 1).\nCap\xc3\xadtulo 6: Petrograf\xc3\xada sedimentaria de las terrazas del Rio Pisuerga El estudio de los sedimentos fluviales conduce a las conclusiones siguientes. Los cantos de todas las terrazas de cualquier altura relativa se componen en su mayor\xc3\xada de cuarcitas, procedentes del conglomerado Curavacas. Los cantos de la terraza HP se caracterizan por \xc3\xadndices de desgaste bastante altos, que excluyen una influencia de clima periglaciario en la \xc3\xa9poca del Pisuerga Alto. Los cantos de las terrazas intermedias y bajas est\xc3\xa1n mucho menos rodados, lo que indica la influencia del clima periglaciario en aquellos tiempos. El an\xc3\xa1lisis de los sedimentos nos demuestra que el sedimento ha sido depositado bajo condiciones de \xe2\x80\x9cbraiding rivers\xe2\x80\x9d, es decir que hubo m\xc3\xa1s derrubios de los que el r\xc3\xado pudo transportar.\nLos dep\xc3\xb3sitos de las terrazas intermedias tambi\xc3\xa9n han sido sedimentados bajo importantes alternaciones en el r\xc3\xa9gimen fluvial. Como son menos espesos y tampoco tienen la gran distribuci\xc3\xb3n horizontal de los sedimentos de HP, las \xc3\xa9pocas en las cuales fueron depositados habr\xc3\xa1n sido bastante m\xc3\xa1s breves.\nLos granos de cuarzo de 500\xe2\x80\x941050 \xc2\xb5 de di\xc3\xa1metro son generalmente angulares, como se ve del dib. 27. Unos porcientos tienen altos \xc3\xadndices de desgaste, lo que puede indicar que localmente ha habido influencia e\xc3\xb3lica.\nLos an\xc3\xa1lisis de los minerales densos se presentan en el cuadro 10 y en el dib. 28, en los cuales se observa una predominancia de los minerales circ\xc3\xb3n, turmalina y r\xc3\xbatilo. La estaurolita procede del Tri\xc3\xa1sico, pero esto no quiere decir que todo el Tri\xc3\xa1sico se caracterice por la presencia de estaurolita.\nDe las observaciones hechas se concluye que en la \xc3\xa9poca del Pisuerga Alto, el r\xc3\xado ten\xc3\xada dos importantes arterias superiores, una de ellas procedente de la zona del conglomerado Curavacas, bajando la otra del escarpamiento del Tri\xc3\xa1sico. Desde Cervera continuaba al Sur, pasando por el Puerto del Brezo. De la continuaci\xc3\xb3n de la terraza HP con respecto a la ra\xc3\xb1a de Guardo, se deduce que la terraza es m\xc3\xa1s reciente, es decir que probablemente es de edad Villafranquiense superior. Despu\xc3\xa9s, el Pisuerga Alto fu\xc3\xa9 capturado por un afluente del Camesa Alto, que en un tramo subsecuente en rocas de poca resistencia pod\xc3\xada agrietarse r\xc3\xa1pidamente por erosi\xc3\xb3n regresiva. Despu\xc3\xa9s de la captura, el R\xc3\xado Pisuerga se desvi\xc3\xb3 desde Cervera hacia el Este; el nuevo suelo del valle, tras una fase de incisi\xc3\xb3n, form\xc3\xb3 la terraza LH.\nLas terrazas intermedias (HM, MM y LM) fueron depositadas bajo un clima periglaciario; los niveles MM y LM se atribuyen a la glaciaci\xc3\xb3n Rissiense, no siendo segura a\xc3\xban la edad del nivel HM. La terraza baja, adem\xc3\xa1s del car\xc3\xa1cter periglaciario de sus sedimentos, se caracteriza por la desembocadura de diversos \xe2\x80\x9cdellen\xe2\x80\x9d, que tambi\xc3\xa9n ofrece un argumento para atribuir su origen a la glaciaci\xc3\xb3n W\xc3\xbcrmiense.\nCap\xc3\xadtulo 7: Descripci\xc3\xb3n de las terrazas del R\xc3\xado Rubag\xc3\xb3n Existen diferencias considerables entre el Pisuerga y el Rubag\xc3\xb3n : la cuenca de \xc3\xa9ste es mucho menos extensa; las terrazas fluviales son, por consiguiente, menos grandes y se encuentran, adem\xc3\xa1s, en niveles m\xc3\xa1s bajos, tanto en sentido relativo como absoluto. Pueden distinguirse cuatro niveles: La terraza HR Altura relativa 55\xe2\x80\x9470 m \xe2\x80\x9e \xe2\x80\x9e MR \xe2\x80\x9e \xe2\x80\x9e 40\xe2\x80\x9450 \xe2\x80\x9e \xe2\x80\x9e \xe2\x80\x9e LMR \xe2\x80\x9e \xe2\x80\x9e 15\xe2\x80\x9420 \xe2\x80\x9e \xe2\x80\x9e \xe2\x80\x9e Baja \xe2\x80\x9e \xe2\x80\x9e 0\xe2\x80\x945 \xe2\x80\x9e Est\xc3\xa1n representadas en dib. 29, con el perfil longitudinal del R\xc3\xado Rubag\xc3\xb3n hasta su desembocadura en el R\xc3\xado Camesa. Los n\xc3\xbameros de las terrazas en el texto corresponden con los en el perfil.\nLa terraza HR se halla en las partes 4, 6 y 7. El espesor de la cobertura sedimentaria var\xc3\xada de unos 2 metros a seis o siete metros. Se compone el dep\xc3\xb3sito fluvial de cantos de conglomerado y de arenisca gruesa Tri\xc3\xa1sicos y cantos cuarcitosos; el di\xc3\xa1metro de los mayores cantos excede los 70 cms.\nAqu\xc3\xad, lo mismo que en la cuenca del Pisuerga, se observan en muchos sitios pendientes de denudaci\xc3\xb3n con \xc3\xa1ngulos peque\xc3\xb1os que se levantan suavemente sobre el nivel de la terraza alta.\nM\xc3\xa1s hacia el Sur en la comarca de Matalbaniega y Nestar, se presentan tres restos de una terraza alta, con alturas de 1000\xe2\x80\x94980 metros. Como veremos m\xc3\xa1s adelante, forman parte de la terraza alta del Camesa.\nLa terraza MR se halla en las partes 3, 8, y probablemente, 1. Salvo \xc3\xa9ste \xc3\xbaltimo, estas partes est\xc3\xa1n cubiertas de una capa sedimentaria de cantos, de un espesor de 2\xe2\x80\x943 metros. La terraza LMR se encuentra en las partes 2 y 9. Tambi\xc3\xa9n est\xc3\xa1n cubiertas de una cobertura de cantos.\nLa Terraza Baja se extiende desde Barruelo de Santull\xc3\xa1n r\xc3\xado abajo, y localmente alcanza una anchura de m\xc3\xa1s de 500 metros. La cobertura de cantos tiene un espesor de unos 2\xe2\x80\x944 metros.\nCap\xc3\xadtulo 8: Petrograf\xc3\xada sedimentaria de las terrazas del R\xc3\xado Rubag\xc3\xb3n La naturaleza litol\xc3\xb3gica de los cantos est\xc3\xa1 representada gr\xc3\xa1ficamente en dib. 33, en el cual se ve que domina la cuarcita, mezcl\xc3\xa1ndose con los cantos del Tri\xc3\xa1sico. Los \xc3\xadndices de desgaste se dan en el dib. 34. Por la ausencia de conglomerados espesos que suministren cantos cuarcitosos ya rodados, son distintos los diagramas de dibs. 21 y 34. Sin embargo, puede concluirse que los cantos del sedimento HR demuestran un transporte fluvial de corta distancia, en el cual no hubo influenca glaciaria ni periglaciaria. La terraza LMR, al contrario, claramente indica una influencia periglaciaria. En la Terraza Baja tambi\xc3\xa9n puede ser observada una influencia periglaciaria, pero ha sido menos importante que en el caso LMR.\nLa granulometr\xc3\xada de las muestras indica deposici\xc3\xb3n bajo un r\xc3\xa9gimen fluvial con grandes variaciones de caudalosidad. V\xc3\xa9ase dib. 35. El contenido algo mayor de la fracci\xc3\xb3n \xe2\x80\x9csilt\xe2\x80\x9d (2\xe2\x80\x9450 micr\xc3\xb3n) en las terrazas LMR y Baja puede atribuirse a la acci\xc3\xb3n del viento.\nLos granos de cuarzo son generalmente angulares (dib. 36), con una excepci\xc3\xb3n importante: la terraza MR, cuyo sedimento est\xc3\xa1 bien rodado y como tal refleja el car\xc3\xa1cter periglaciario de su cobertura sedimentaria.\nLos minerales densos (dib. 37, cuadro 13) ense\xc3\xb1an la predominancia de los minerales turmalina, circ\xc3\xb3n y r\xc3\xbatilo. El contenido de topacio de una parte de la terraza Baja fu\xc3\xa9 causado por acarreo desde el Oeste, de la r\xc3\xa9gion Wealdense.\nCap\xc3\xadtulo 9: Descripci\xc3\xb3n de las terrazas del R\xc3\xado Camesa S\xc3\xb3lo hay dos niveles de terrazas del Camesa: la terraza HC, de altura relativa, media de 60\xe2\x80\x9475 metros, y la terraza baja.\nLa terraza HC se halla, extendi\xc3\xa9ndose desde Mataporquera (dib. 38), en las partes 2, 4 y 5, con una afluente en el valle del Arroyo de la Canal (3), y en las partes de Matalbaniega. Est\xc3\xa1 cubierta esta terraza de un sedimento de unos 10\xe2\x80\x9412 metros de espesor; s\xc3\xb3lo en las partes superiores (Mataporquera y Arroyo de la Canal) no alcanza m\xc3\xa1s de 6\xe2\x80\x948 metros.\nNo hay terrazas intermedias.\nLa Terraza Baja del R\xc3\xado Camesa es distinta de las de los R\xc3\xados Pisuerga y Rubag\xc3\xb3n, por no tener cantos en su superficie. Por el perfil longitudinal de la pendiente extremadamente baja, la potencia de erosi\xc3\xb3n y transporte es casi nula. Los cantos, si los hay, se pierden en los dep\xc3\xb3sitos turbosos del agua estancada.\nCap\xc3\xadtulo 10: Petrograf\xc3\xada sedimentaria de las terrazas del R\xc3\xado Camesa Por ausencia de afloramientos, no hemos podido tomar muestras de la Terraza Baja, y tampoco fu\xc3\xa9 posible realizar an\xc3\xa1lisis de los cantos. As\xc3\xad es que s\xc3\xb3lo se puede observar que los sedimentos de la Terraza Baja deben reflejar las caracter\xc3\xadsticas de la terraza HC, porque \xc3\xa9sta se encuentra casi en todos los sitios sobre la terraza baja, en la ribera derecha. Los numerosos meandros indican que, si han estado presentes anteriormente, los restos de terrazas intermedias pueden haber desaparecido f\xc3\xa1cilmente por la erosi\xc3\xb3n lateral de este valle bastante angosto.\nAs\xc3\xad es que s\xc3\xb3lo hemos podido estudiar los dep\xc3\xb3sitos de la terraza HC. En dib. 44 se presenta la naturaleza litol\xc3\xb3gica de los cantos, de la cual se ve claramente la importancia de los cantos compuestos del Tri\xc3\xa1sico. La influencia del K\xc3\xado Rubag\xc3\xb3n en este sedimento se manifiesta en un aumento del porcentaje de cantos cuarcitosos. Los cantos cuareitosos que han sido encontrados en el valle del Arroyo de la Canal, en cambio, deben ser procedentes de bancos de conglomerado grueso cuarcitoso, que seguramente est\xc3\xa1n presentes en el Tri\xc3\xa1sico.\nEn la direcci\xc3\xb3n r\xc3\xado abajo, observamos un aumento de desgaste de los cantos (dib. 45). Influencias periglaciarias resultan ausentes. De los an\xc3\xa1lisis granulom\xc3\xa9tricos (dib. 46A) se ve que la fracci\xc3\xb3n de di\xc3\xa1metro 〈 2000 micrones es bastante hom\xc3\xb3gena. Los bancos arenosos bajo los cantos de la terraza tambi\xc3\xa9n son de origen fluvial, y pueden ser m\xc3\xa1s antiguos que la terraza HC.\nEl desgaste de granos de cuarzo de 500\xe2\x80\x941050 micrones de di\xc3\xa1metro est\xc3\xa1 representado gr\xc3\xa1ficamente en dib. 47. Son angulares, con muy pocas excepciones. Los minerales densos se han puesto en el cuadro 16.\nSon muy similares los caracteres fisiogr\xc3\xa1ficos de las terrazas HC del Camesa y de HP del Pisuerga. Por ejemplo, el espesor de las coberturas sedimentarias es casi igual en ambos casos; adem\xc3\xa1s, las dos terrazas se han desarrollado igualmente como \xe2\x80\x9cterrazas de plataforma\xe2\x80\x9d, y, salvo la naturaleza litol\xc3\xb3gica de los cantos, son muy semejantes los caracteres petrograf\xc3\xadco-sedimentarios. La terraza HR del Rubag\xc3\xb3n desemboca en la terraza HC, de tal manera que el \xe2\x80\x9cRubag\xc3\xb3n Alto\xe2\x80\x9d debe haber sido un afluente del \xe2\x80\x9cCamesa Alto\xe2\x80\x9d. Llenaban los r\xc3\xados juntos parte de la llanura, situada entre la Cordillera Cant\xc3\xa1brica y el \xe2\x80\x9cPays Pliss\xc3\xa9\xe2\x80\x9d (cot\xc3\xa9jese Cap. 11).\nCap\xc3\xadtulo 11: Superficies de planaci\xc3\xb3n Prerrod\xc3\xa1nico. Tras los movimientos tect\xc3\xb3nicos de la fase s\xc3\xa1vica en el centro de la Meseta y en las cordilleras marginales, se desarroll\xc3\xb3 la \xe2\x80\x9cPenillanura fundamental de la Meseta\xe2\x80\x9d, bien conocida de publicaciones de diversos autores, y discutida ampliamente por Sol\xc3\xa9 Sabaris (1952). Ya antes del Pontiense exist\xc3\xada esta penillanura, que se extend\xc3\xada ampliamente y que fu\xc3\xa9 levantada y basculada por la fase rod\xc3\xa1nica. En Galicia, tambi\xc3\xa9n han sido encontrados restos de la penillanura fundamental de la meseta, y seg\xc3\xban Stickel (1930) tambi\xc3\xa9n estar\xc3\xadan presentes en numerosos sitios en la Cordillera Cant\xc3\xa1brica, por ejemplo en las comarcas del Puerto de Piedras Luengas. Nosotros, sin embargo, no hemos observado ninguna indicaci\xc3\xb3n de tal penillanura en este sitio. Puede ser que se encuentre m\xc3\xa1s al Oeste, pero en la regi\xc3\xb3n investigada por nosotros, seguramente falta en la actualidad.\nPostrod\xc3\xa1nico. Despu\xc3\xa9s de los movimientos rod\xc3\xa1nicos, la erosi\xc3\xb3n form\xc3\xb3 otra vez amplias superficies de planaci\xc3\xb3n, bajo un clima \xc3\xa1rido o semi-\xc3\xa1rido; son pedimentos, claramente visibles en muchas partes de Espa\xc3\xb1a. Al Sur de la Cordillera Cant\xc3\xa1brica, se desarroll\xc3\xb3 un pedimento del cual se reconocen ahora los restos al Sur de la villa de Guardo. Sobre los pedimentos se hallan coberturas de derrubios, generalmente cantos angulares o mal rodados, las ra\xc3\xb1as. Hasta ahora las ra\xc3\xb1as y los pedimentos fueron considerados como siendo de la misma edad, pero recientemente, Mensching (1958) pronunci\xc3\xb3 la posibilidad de que los pedimentos fuesen de m\xc3\xa1s edad, e.d. del Plioc\xc3\xa9nico, que las ra\xc3\xb1as, que tienen edad Villafranquiense.\nAl Sur de la Sierra del Brezo se presenta un fen\xc3\xb3meno similar: existe una llanura, cubierta de una brecha calc\xc3\xa1rea. Es el \xc3\xbanico sitio donde se hallan sedimentos con derrubios de la Caliza de Monta\xc3\xb1a en la regi\xc3\xb3n que hemos investigado. Probablemente, esta llanura es de la misma edad y del mismo origen que las ra\xc3\xb1as, es decir de la \xc3\xa9poca Villafranquiense.\nEn nuestra regi\xc3\xb3n, existen numerosos restos de superficies de planaci\xc3\xb3n que, sin embargo, no tienen car\xc3\xa1cter de pedimento y sobre los cuales tampoco se hallan derrubios angulares.\nHay m\xc3\xa1s razones para no considerarlas como pedimentos. Est\xc3\xa1n claramente relacionadas con las rocas de poca resistencia, y, por tanto, la planaci\xc3\xb3n debe haber originado de los valles de un sistema fluvial subsecuente. Pero como son m\xc3\xa1s antiguas que las terrazas altas, tambi\xc3\xa9n deben ser de edad Villafranquiense.\nTodos los restos de superficies de planaci\xc3\xb3n son evidentemente partes de una superficie, o puede decirse que todas las partes son de la misma edad. La superficie est\xc3\xa1 situada m\xc3\xa1s alto en la llamada superficie de Muda (v\xc3\xa9ase mapa 1: A), bajando hacia el Sureste. Para facilitar la descripci\xc3\xb3n, hemos indicado las partes individuales con nombres de pueblos situados en estas partes. S\xc3\xb3lo el nivel de Redondo parece formarse activamente hasta ahora; puede ser que originalmente fuera de la misma edad que las otras, pero ahora existe una diferencia con \xc3\xa9stas, que son f\xc3\xb3siles.\nCap\xc3\xadtulo 12: Morfog\xc3\xa9nesis Despu\xc3\xa9s de las fases orog\xc3\xa9nicas herc\xc3\xadnicas, la Cordillera Cant\xc3\xa1brica ha tenido una historia muy compleja. Los efectos de las or\xc3\xb3genas terciarias se muestran en la plegadura de los sedimentos Mesozoicos marginales alrededor del bloque mesete\xc3\xb1o, y en los movimientos epirog\xc3\xa9nicos del mismo. As\xc3\xad se formaron las depresiones castellanas y la Cordillera Central (Sol\xc3\xa9 Sabaris, 1952). El Terciario al Sur de la r\xc3\xa9gion investigada se presenta como dos series de conglomerados: una de cantos de calizas Cretaceicas, de edad probablemente Eocena u Oligocena, y otra de cantos cuarcitosos de edad Miocena. Seg\xc3\xban Mabesoone (1959), el conglomerado inferior, de cantos calic\xc3\xadferos, fu\xc3\xa9 depositado despu\xc3\xa9s de la fase pirenaica, y plegado en la fase s\xc3\xa1vica. Despu\xc3\xa9s de esta fase, continu\xc3\xb3 inicialmente la entrega de cantos de caliza, que posteriormente fueron sustitu\xc3\xaddos por cantos cuarcitosos. Despu\xc3\xa9s, el tipo de sedimentos fu\xc3\xa9 haci\xc3\xa9ndose m\xc3\xa1s fino. Pero de esto no puede concluirse que existiera un relieve llano en la Cordillera Cant\xc3\xa1brica.\nTras la fase rod\xc3\xa1nica, que caus\xc3\xb3 el levantamiento del bloque mesete\xc3\xb1o y su basculaci\xc3\xb3n, por la que se formaron las grandes arterias fluviales de la meseta que se dirig\xc3\xadan hacia occidente, se inici\xc3\xb3 en muchas partes de Espa\xc3\xb1a la pedimentaci\xc3\xb3n, como ya hemos indicado en el cap\xc3\xadtulo precedente. En nuestra regi\xc3\xb3n, la planaci\xc3\xb3n ten\xc3\xada otro tipo, pero tambi\xc3\xa9n es de edad Villafranquiense. En el Villafranquiense superior, el r\xc3\xa9gimen fluvial cambi\xc3\xb3 de tal manera que los r\xc3\xados tuvieron el car\xc3\xa1cter de \xe2\x80\x9cbraiding rivers\xe2\x80\x9d, que depositaban importantes masas de cantos en las llanuras intramontanas, que ya exist\xc3\xadan como resultado de la planaci\xc3\xb3n. Hab\xc3\xada, en aquella \xc3\xa9poca, el sistema del Pisuerga Alto, y el del Camesa Alto, del cual el sistema del Rubag\xc3\xb3n Alto era un importante afluente. No exist\xc3\xada una conexi\xc3\xb3n entre los dos sistemas. Posteriormente, el Pisuerga Alto fu\xc3\xa9 capturado por un afluente del sistema del Camesa Alto, que ten\xc3\xada gran potencia erosiva, por pasar, en un tramo subsecuente, por rocas de poca resistencia. Luego, en tiempos de clima glaciario o periglaciario, se depositaron las terrazas intermedias y bajas. La terraza baja es de edad W\xc3\xbcrmiense, los niveles LM/LMR y MM/MR son de edad Rissiense, no siendo segura a\xc3\xban la edad del nivel HM, e. d. o de Rissiense antiguo, o Mindeliense. Las formas de relieve glaciares, en esta regi\xc3\xb3n, no tienen gran importancia, las periglaciares son los bloques, los \xe2\x80\x9cdellen\xe2\x80\x9d, que se hallan en dos tipos, y la soliflucci\xc3\xb3n.\nHablando geol\xc3\xb3gicamente, en el futuro pr\xc3\xb3ximo, una captura del sistema Rubag\xc3\xb3n/Camesa superior por el Arroyo Mardancho, afluente del Ebro, tendr\xc3\xa1 lugar en Quintanilla de las Torres. Se predice, asimismo, una captura del tramo superior del Ebro por el R\xc3\xado Besaya cerca de Reinosa.\nAs\xc3\xad le quedar\xc3\xa1 claro al lector, que las modificaciones de sistema fluvial que hemos establecido en el pasado, no ser\xc3\xa1n las \xc3\xbaltimas; en el futuro geol\xc3\xb3gico, si la naturaleza puede actuar libremente, se producir\xc3\xa1n modificaciones igualmente importantes.

Description: The present paper deals briefly with the main geological features of the Casavegas area (Northern Palencia, Spain). Though incomplete, the sequence of Carboniferous strata in this region is regarded as a reference-section for correlation purposes within the larger N. Palencia area. A local subdivision on fusulinids of a part of the Carboniferous is proposed. Three zones are distinguished: Protricites Zone F. ex gr. bra\xc3\xb1oserae Subzone Fusulinella Zone F. delepinei Subzone Profusulinella Zone Fusulinella bocki, var. delepinei is brought to species level as F. delepinei Van Ginkel, sp. nov.

Description: Het Belledonne Massief wordt overlangs in twee\xc3\xabn gedeeld door een samengeknepen synclinale zone, die plaatselijk permocarbonische of mesozo\xc3\xafsche sedimenten bevat. Het onderzochte gebied strekt zich ter weerszijde van deze zone uit.\nHet westelijke of externe deel bestaat in hoofdzaak uit sericietchlorietschisten, veelal met albietporfieroblasten (St. Hugon schisten). Deze porfieroblasten zijn geen latere vormingen, doch behoren tot de oorspronkelijke metamorphose van deze schisten. Het oostelijke of interne deel bestaat overwegend uit granieten, amfibolieten en glimmerschisten. De metamorfosegraad is hier meestal hoger dan in het externe deel, zoals blijkt uit het anorthietgehalte van de plagioklaas en uit de aanwezigheid van de mineralen granaat, stauroliet en distheen. In het onderzochte gebied zijn onderscheiden de Lac Crop formatie, bestaande uit in banden afwisselende glimmerschisten en amfibolieten, en de Ferrouillet amfibolieten. De laatste zijn waarschijnlijk van magmatische herkomst, gezien de eentonigheid van de formatie, de rijkdom aan titaniet en de aanwezigheid van klinopyroxeenkernen en complex vertweelingde plagioklaasmegacrysten, die beiden als magmatische relicten worden opgevat. Vergelijken we het kristallijn van het Belledonne Massief met dat van de naburige hercynische massieven, dan blijkt de metamorfosegraad in het algemeen minder hoog te zijn dan elders het geval is. Vermoedelijk vertegenwoordigt het Belledonne Massief een structuurelement dat oorspronkelijk verder naar buiten (westelijk) heeft gelegen dan de andere massieven.\nDe zojuist beschreven regionale metamorfose, die zeker ouder is dan het Boven-Carboon, is op vele plaatsen grotendeels uitgewist door laathercynische of alpiene dynamometamorfose. Dit is o. a. in het noordelijk gedeelte van het gekarteerde gebied het geval. Herkenning van de oorspronkelijke metamorfe gesteenten is vaak slechts microscopisch mogelijk. De dynamometamorfose uit zich soms in mylonitisatie, soms in verbrijzeling en omzetting zonder dat aanzienlijke bewegingen in het gesteente schijnen te hebben plaatsgevonden. Deze jongere metamorfose hangt uiteraard samen met de hercynische en alpiene tektogenesen. In beide gevallen heeft niet zozeer plooi\xc3\xafng als wel intensieve beweging van kristallijnblokken plaatsgehad.\nDe permocarbonische en mesozo\xc3\xafsche sedimenten komen \xc3\xb2f wel ingeklemd tussen deze blokken, \xc3\xb2f als een weinig geplooid dek op de blokken voor. Het Boven-Carboon (Westphalien D\xe2\x80\x94Stephanien A) bestaat grotendeels uit zwarte continentale afzettingen : conglomeraten, fijngelaagde zandstenen, leien en wat kool. In de \xe2\x80\x9eGr\xc3\xa8s d\xe2\x80\x99Allevard\xe2\x80\x9d (continentaal Perm) zijn twee gedeelten te onderscheiden. Het onderste gedeelte bevat grijze of zwarte pelieten en lichtgekleurde veldspaathoudende zandstenen. Enkele plantafdrukken wijzen op een onder-permische ouderdom. In het bovenste deel, waarin paarsrode muscoviethoudende pelieten overheersen, zijn geen fossielen gevonden. Microscopisch onderzoek wijst uit dat zowel de boven-carbonische als de permische sedimenten vaak grote hoeveelheden rhyolitisch of rhyodacitisch materiaal bevatten. De vooral in het Carboon veelvuldig voorkomende verkiezeling houdt waarschijnlijk verband met dit vulkanisme. In de Trias spelen, zoals bijna overal in de Alpen, caverneuze kalken de hoofdrol. Gips- en anhydrietrijke lagen hebben als glijvlak gediend, waarover het erboven liggende sedimentaire dek \xe2\x80\x94 voornamelijk Jura in B\xc3\xbcndnerschieferfacies \xe2\x80\x94 van de omhoogkomende kristallijnblokken is afgegleden. Op deze wijze zijn de ten Westen van het eigenlijke Belledonne Massief gelegen \xe2\x80\x9ecollines liasiques\xe2\x80\x9d ontstaan.

Description: It one has a group of samples from one population and a group of samples from another population, one is often faced with the question whether both populations are the same or not. For this situation several statistical tests are available, one of these being the well-known Student\'s test (cf. Dixon and Massey, 1951, chapter 9). One of the assumptions underlying Student\'s test is that the quantities, of which observations are available, have a normal distribution. In many cases, however, it is not known whether or not this assumption is satisfied. In these cases it is advisable to use a statistical test, not based on the assumption of normal distributions. In the problem concerned one can use, e.g., Wilcoxon\'s two-sample test. The assumptions underlying this test are : a. all observations are taken at random and are independent; b. the observations in group I are taken from the same population; c. the observation in group II are taken from the same population.\nAs an example we take the following situation. A type of rock has been found in two localities; at each locality one has taken 6 samples* at random. The sodium content (in percentages) of these samples is: locality I; 6.3; 3.9; 3.5; 10.0; 2.5; 3.4. locality II; 5.6; 5.2; 6.0; 3.3; 1.1; 3.0.

Description: In previous publications Bishop & Crisp (1957, 1958) described the distribution of Elminius modestus on the coasts of France, based on surveys made in 1953 and 1954. Further information including some observations made in 1955 was given by Bishop, Crisp, Fischer-Piette & Prenant (1957). Elminius was shown to be centred on three main areas; the Channel coast east of Cap de la Hague, the river systems of North Brittany, and the Rade de Brest. Further south scattered individuals only were to be found, nowhere in sufficient abundance to allow the majority to breed. Bishop & Crisp (1957) pointed aut that the scarcity of Elminius on this part of the Brittany coast was surprising, since there are numerous suitable estuaries and harbours and an abundance of fishing craft which might disseminate the species.\nA further survey was made in August and September 1957. No significant changes had taken place along the coast of the Channel nor in the Rade de Brest itself. However in the vicinity of the important fishing ports of Concarneau and Lorient a marked increase in the population of Elminius had taken place between 1954 and 1957 (fig. 1). Established colonies were found in the harbour at Concarneau, and in the river systems of the Aven, Belon and Laita. The greatest abundance was found at the junction of the Scorff and Blavet near Lorient, while in the adjacent estuary of the Etel the species was quite common. Further south the only evidence of Elminius was a single specimen seen on the harbour wall at Point St. Jacques. No specimens were found anywhere in the inland sea of Morbihan, an area of sheltered water very suitable for this species, nor in the estuary of the Loire. Probably the very exposed Quiberon peninsula is for the time being a barrier to its further spread to the south.

Description: Description of an ulcerated epidermoid carcinoma of the lower lip in an adult male of the Cichlid Hemichromis bimaculatus Gill.\nHistologically the tumour was composed of masses and strands of pleomorphic, columnar or polyhedral tumour cells, partly arranged in papillary pegs, which were supported by a vascular connective tissue stroma. The chromatin network of the nuclei was densely structured. The tumour tissue showed an invasive growth and had locally pierced the basement membrane.\nEmboli of tumour cells and metastases were lacking.

Description: Since the publication of the Revision of the Genus Dillenia (Blumea 7, 1952, pp. 1\xe2\x80\x94145) a number of additional collections have come to my notice. As is to be expected, the most interesting ones are from Eastern Malaysia, where the genus has developed a high degree of diversity and where the number of collections is still relatively small.

Description: During 1957 two important collections of fishes were obtained from off the coast of Suriname and adjacent regions. The first of these was made by the motor vessel \xe2\x80\x9cCoquette\xe2\x80\x9d, a commercial shrimp trawler which engaged in exploratory work for the Government of Suriname. Mr. JAMES B. HIGMAN of the United States Fish and Wildlife Service was invited to accompany the \xe2\x80\x9cCoquette\xe2\x80\x9d during part of this work, and the collection of fishes which resulted was due largely to his efforts. The second collection was obtained by the motor vessel \xe2\x80\x9cOregon\xe2\x80\x9d, exploratory vessel of the United States Fish and Wildlife Service. During November, 1957, the \xe2\x80\x9cOregon\xe2\x80\x9d occupied over a hundred trawl stations along the northern coast of South America between Venezuela and the Equator. Most of these collections are now in the U. S. National Museum and the Chicago Natural History Museum.\nBoth the \xe2\x80\x9cOregon\xe2\x80\x9d and the \xe2\x80\x9cCoquette\xe2\x80\x9d collections contain representatives of a distinctive new species of Lonchopisthus. The definition of this species has required a review of the western Atlantic species of the genus. I take pleasure in naming this new species of Lonchopisthus from Suriname in honour of its collector:

Description: The fossil remains of rodents described in the present paper are from various localities. The large extinct musk rat Megalomys occurs in reddish-brown phosphatic \xe2\x80\x9coolite\xe2\x80\x9d fillings of irregular cavities in a marine limestone found by Mr. P. H. DE BUISONJ\xc3\x89 in the north-western part of the Duivelsklip, eastern Cura\xc3\xa7ao, about 50 m above sea-level. The \xe2\x80\x9coolite\xe2\x80\x9d also contains scanty remains of lizards, snakes, and of a bat. Fragmentary molluscs present possibly include Cerion uva (L.), a recent, very common, terrestrial species, as well as other gastropods, many opercula of which were found.\nSamples of a phosphatic \xe2\x80\x9co\xc3\xb6lite\xe2\x80\x9d deposit collected in 1937 by Dr. P. WAGENAAR HUMMELINCK from an escarpment near Fontein, Bonaire, proved to contain jaws, with teeth, of a genus of hesperomyine rodents, Thomasomys a single snake vertebra; and mollusc remains including what seem to be their coprolites.

Description: In a previous paper, published in the same series, Vol. 2 (1940), the author dealt with a small collection of snakes obtained by Dr. P. WAGENAAR HUMMELINCK in 1930 and 1936 on the islands off the Venezuelan coast and on the adjacent mainland. The present article reports on some specimens, chiefly from the Dutch islands of the Windward Group, presented by him to the Rijksmuseum van Natuurlijke Historie at Leiden in later years. Some notes are included on three specimens of Alsophis from the same area that were already present in the collections of this museum (indicated by M.L.). \xe2\x80\x94 The photographs were made by Dr. HUMMELINCK.

Description: The present study is based on material obtained by Dr. P. WAGENAAR HUMMELINCK on his various trips to the Caribbean, the greater part of which was received from the Zo\xc3\xb6logisch Museum at Amsterdam, where the types and most of the other specimens are deposited. Mr. R. H. COBBEN, entomologist of the Landbouwhogeschool at Wageningen, who collected on the Netherlands Antilles in 1956, was also kind enough to let me have his material for study.\nThe following species are now known to occur in the area under consideration:

Description: A small area limited in the north by the Boca del Cant\xc3\xb3, in the west by the Pallaresa river and in the south by the crest of the Monta\xc3\xb1a de Bahent and reaching westwards as far as the village of Feixa was surveyed in detail. Previous work by Prof. de Sitter and some of his pupils had revealed that in the steep southern slope of the Boca del Cant\xc3\xb3 several recumbent folds occur with Ordovician shales in the anticlinal cores and Devonian in the synclines. The work was carried out on the topographical base of an 1:25.000 enlargement of the official 1:50.000 map, sheets 214, Sort and 215 Seo de Urgel, which proved to be far from satisfactory. Aerial photographs were not available.\nThe Tornafort area is limited in the north by an important fault, which runs practically in the bed of the Boca del Cant\xc3\xb3. Tins fault forms the southern limit of the axial zone of the Pyrenees, north of it we find the Lower Triassic conglomerates, sandstones and shales covering unconformably strongly microfolded non metamorphic Ordovician. Near the mouth of the Boca del Cant\xc3\xb3 this clastic Trias is covered by the evaporite facies of the Keuper, with ophites and muschelkalk floats. The latter formation forms also the western boundary of our region on the lower slopes of the Tornafort hill towards the Pallaresa river, again separated from the Paleozoic by a north-cast trending fault. Thus the Tornafort area forms the northern border zone of the Nogueras zone as it has been defined by Peter Misch (1934). This Nogueras zone is known to have been strongly deformed by alpine orogeny because a little further south and west we see that the paleozoic has been folded together with the Triassic. A section by de Sitter (1957) crossing the Pallaresa river just west of our region shows a Devonian anticlinal core with Trias in the flanks. Our Tornafort region, however, is separated from the structure given by this section by a thrust along which the Devonian with Silurian at its base has been thrusted on the Triassie. This thrust forms the southwest boundary of our map, and the Tornafort structure does not seem to be connected with the just mentioned anticline, as has been done by de Sitter in his section, where the Tornafort structure is drawn as the core of a second anticline further south.

Description: In an adult female of the common eel Anguilla anguilla a large lipoma was found, situated on the left side, caudally of the left operculum. Microscopically, the tumour, which originated from the subcutaneous connective tissue, was composed of areas of adipose tissue and areas of fibrous connective tissue.\nThe tumour belongs to the fibrolipomatous type and shows a striking resemblance with the lipoma, described by Stolk (in press) in the lizard Lacerta muralis.

Description: The main purpose of this study is to search for an explanation of the curious differentiation within the genus Chamaeleo. Since the species of this genus are rather doubtful units, I have studied the geograpical distribution of characters, not of the species, a method first used in botany (BAUR, ROTHMALER a.o.). I found that the number of characters is largest in east Afrika, gradually decreasing from this area to the periphery of the total range of the genus. East Africa proved to be still more important, as practically all the characters occur in it. This means that the chameleons in the other areas practically never possess characters that are not found in east Africa.\nThis pattern of distribution fits in rather well with REINIG\xe2\x80\x99S elimination theory (1938): \xe2\x80\x9e.. bei Einzelwanderungen wird nur ein Teil des gesamten Allelbestandes einer Art mitgef\xc3\xbchrt... eine durch Einzelwanderung entstandene Population weist eine geringere Zahl von Allelen auf als die Ausgangspopulation.\xe2\x80\x9d The existence of many parallel series of variation (meaning that several characters originated several times independently in different groups) led me to the conclusion that the mechanism described in REINIG\xe2\x80\x99S theory as elimination, has consequences also for the genes predisposed to change into others.\nThis reasoning gave a key to the reconstruction of the ancestral chameleon. By two different ways I arrived at the same conclusion, viz. the ancestral chameleon was probably an animal resembling mostly Chamaeleo chamaeleon s.l. (\xc2\xa7 21).\nAs for this theoretical part of my study a survey of the species was needed, I first made an attempt at a natural system. I have divided the genus into groups of related species. For practical reasons the chameleons of Madagascar are treated separately. Their connections with the species of the African continent are examined in a special section (\xc2\xa7 11).\nAs a result of my investigations I had to propose the following taxonomic changes: Ch. rhinoceratus var. lineatus + Ch. labordi + Ch. voeltzkowi + Ch. barbouri = Ch. rhinoceratus (\xc2\xa7 3), Ch. lambertoni = Ch. lateralis (\xc2\xa7 4), Ch. semicristatus = \xe2\x99\x80 Ch. verrucosus (\xc2\xa7 5), Ch. guibei nov. spec. (\xc2\xa7 6), Ch. calcarifer = Ch. chamaeleon calcarifer, Ch. zeylanicus = Ch. chamaeleon zeylanicus, Ch. etiennei = Ch. gracilis etiennei (\xc2\xa7 12), Ch. anchietae vinkei + Ch. anchietae mertensi + Ch. marunguensis = Ch. anchietae (\xc2\xa7 13), Ch. unicornis = Ch. oweni unicornis (\xc2\xa7 14), Ch. pumilus = Ch. pumilus pumilus, Ch. melanocephalus = Ch. pumilus melanocephalus, Ch. gutturalis = Ch. pumilus gutturalis, Ch. ventralis = Ch. pumilus ventralis, Ch. ventralis occidentalis = Ch. pumilus occidentalis, Ch. ventralis karrooicus = Ch. pumilus karrooicus, Ch. damaranus = Ch. pumilus damaranus, Ch. caffer = Ch. pumilus caffer, Ch. taeniobronchus = Ch. pumilus taeniobronchus. (\xc2\xa7 16).