Search publications of the members of the Royal Belgian institute of natural Sciences
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Animal Exploitation in Times of Change: Faunal Remains from Zilum, ca. 600-400 BCE, North-Eastern Nigeria
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Corrigendum: Diversity of mesopelagic fishes in the southern ocean - A phylogeographic perspective using DNA barcoding [Front. Ecol. Evol, 6, 120 (2018)] doi: 10.3389/fevo.2018.00120
- However, we highlight potential (pseudo-)cryptic or unrecognized species in Gymnoscopelus bolini, Lampanyctus achirus, and the non-myctophid genus Bathylagus. A correction has been made to the Discussion, Sub-section Phylogeny and Phylogeography of Southern Ocean Mesopelagic Fishes, Paragraph 6: The available sequences identified as Symbolophorus boops (BOLD references DSFSE476-08 to DSFSE480-08 and DSFSG260-10) cluster apart from the two other Symbolophorus clades resolved in our COI tree (one composed of S. californiensis, S. reversus, S. evermanni, Symbolophorus sp., and S. rufinus and the other composed of S. barnardi and S. veranyi; Figure 2). Instead these sequences settle within the Diaphinae (sensu Martin et al., 2017). Unfortunately we discovered a posteriori that the COI sequences included here as S. boops were likely misidentified on BOLD. These sequences are probably from a Diaphus species (P. A. Hulley, pers. comm.) currently also not present on BOLD, but the specimens are in poor condition, preventing definite identification. The correction has been transmitted to the BOLD database. Other studies that included genetic data proposed that Symbolophorus is closer related to Myctophum, Hygophum, and other genera, as opposed to Diaphinae, but they all lacked specimens of S. boops (Poulsen et al., 2013; Denton, 2014; Martin et al., 2017). Therefore, we highly recommend the collection of further samples/sequences in order to resolve the phylogenetic position of S. boops, and to re-identify the specimens erroneously labeled as Symbolophorus boops. In fact, the entire genus would benefit from a detailed systematic revision as already noted by Wisner (1976). © 2018 Christiansen, Dettai, Heindler, Collins, Duhamel, Hautecoeur, Steinke, Volckaert and Van de Putte.
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Favartia kanneri, a new species (Gastropoda: Muricidae: Muricopsinae) from the Galapagos Islands, Ecuador
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Califrapana: a new genus of California and Bája California late Oligocene to early Miocene muricids previously attributed to the genus Rapana (Mollusca: Gastropoda: Muricidae)
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A classic Late Frasnian chondrychtyan assemblage from southern Belgium
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Rumes/Taintignies – « Le Pèlerin », site artisanal (et d'extraction ?) du Haut-Empire et réoccupation rurale tardo-romaine
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Un tumulus arasé à Lexhy (Commune de Grâse-Hollogne-Hesbaye liégeoise)
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Het landschap in de Swifterbant-periode op basis van de fauna
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Dierlijke resten uit de Swifterbantperiode
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Stable isotopes reveal agricultural practices in the Swifterbant period
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Het landschap in de Hazendonk-periode op basis van de fauna
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Dierlijke resten uit de Hazendonkperiode
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Het landschap uit het laat-neolithicum en de bronstijd op basis van de fauna
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Dierlijke resten uit het laat-neolithicum en de bronstijd
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Off-shore enhanced oil recovery in the North Sea: The impact of price uncertainty on the investment decisions
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Révision lithostratigraphique et biostratigraphique de l’Oligocène d’Aquitaine occidentale (France)
- La stratigraphie de l’Oligocène d’Aquitaine occidentale est revue en synthétisant les données bibliographiques et en réexaminant 93 sondages, dont 60 sont datés à l’aide de foraminifères ou nannofossiles calcaires. La révision de ces sondages a permis de reconstituer l’évolution sédimentaire de l’Aquitaine occidentale en relation avec les évènements tectoniques correspondants. Les petits foraminifères benthiques ont permis d’estimer les variations de la tranche d’eau dans les coupes, qui s’étendent du domaine épibathyal jusqu’au domaine saumâtre. Environ 60 % des foraminifères présents au Priabonien disparaissent au cours de cet étage et à la limite Éocène/Oligocène. L’apparition et la disparition des espèces est progressive dans l’Oligocène, ce qui permet d’en utiliser certaines comme marqueurs pour la stratigraphie du Bassin d’Aquitaine. Les foraminifères du Bassin d’Aquitaine montrent de nombreuses affinités avec ceux de la Paratéthys centrale, indiquant que ces deux régions étaient interconnectées à cette époque par le détroit de Gibraltar et la zone bétique. Sept formations sont retenues dans l’Oligocène marin du Bassin de l’Adour, dont une nouvellement introduite (Formation de Capcosle d’âge Rupélien-Aquitanien) et deux redéfinies (Formation de Biarritz d’âge Rupélien inférieur et Formation d’Escornebéou d’âge Chattien supérieur) ; trois sont distinguées dans le domaine continental (les Formations de Jurançon et de Campagne puis celle de l’Agenais). L’Oligocène de la plate-forme nord-aquitaine comprend deux formations marines (la Formation de Bel-Air et la Formation du Calcaire à Astéries avec le Membre à Crassostrea longirostris à la base) et trois formations continentales (du bas vers le haut : les Formations du Fronsadais, de Castillon et de l’Agenais). Trois grandes aires sédimentaires se différencient au cours de l’Oligocène dans la région aquitaine. La première, entre Labenne et Arcachon, se caractérise par les dépôts à dominance argileuse, bathyaux, épais (jusqu’à 1700 m). La deuxième aire forme un arc de cercle autour de la première et représente la plate-forme avec des sédiments plus variés : calcaires bioclastiques, argiles et sables coquilliers de 400-500 m d’épaisseur. La troisième comprend les sédiments continentaux à l’est et au sud du bassin. Les événements tectoniques pyrénéens influencent la sédimentation, comme le montrent, en premier lieu, la transgression du Rupélien moyen, qui est plus importante au nord qu’au sud, tandis que le phénomène inverse s’observe au Rupélien supérieur, et, deuxièmement, les transgressions du Chattien inférieur et supérieur, qui sont conditionnées par la subsidence locale et la réactivation d’anciennes structures.
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The composite Kortrijk section (W Belgium): a key reference for mid-Ypresian (Early Eocene) stratigraphy in the southern North Sea Basin
- The upper part of the Kortrijk Clay Formation (the Roubaix Clay and Aalbeke Clay Members of mid-Ypresian age) has been exposed in road and canal cuttings and clay quarries in the Kortrijk area (western Belgium), and penetrated by several cored boreholes. It is overlain disconformably by the Mont-Panisel Sand Member of the Hyon Sand Formation (upper middle Ypresian). The Roubaix Clay Member contains diverse and well-preserved calcareous nannofossils, dinoflagellate cysts, foraminifera, ostracods and other calcitic microfossils, and less well-preserved mollusc assemblages, while the Aalbeke Clay Member is secondarily decalcified. The calcareous nannofossil subdivision of upper NP11 and lower NP12 has been recognised in the Kortrijk area, and calibrated with the NW European mid-Ypresian dinoflagellate cyst, ostracod and planktonic foraminiferal zones and datums (e.g. Subbotina influx). Several medium-scale depositional sequences, with an estimated duration of 400 kyr or less, have been recorded. Their respective boundaries coincide with the resistivity maxima identified on the majority of the wireline log profiles of the Belgian Ypresian. Integrated biostratigraphic, magnetostratigraphic and sequence stratigraphic analysis enables correlation with other areas in Belgium, with the London Clay Formation of southern England, and with the standard chronostratigraphic scale. A marine erosion surface has been identified at the base of Unit 20 in the Kortrijk area (mid-Ypresian, early Biochron NP12, middle C24n.1n, ~ 52.8 Ma), corresponding to the first occurrence of estuarine channel-fill units in southern England. This indicates a brief but profound sea-level fall, either eustatically or tectonically controlled. The composite Kortrijk section is proposed as a reference section for the middle Ypresian in the southern North Sea Basin, and for similar settings in mid- to high-latitudes of the Northern Hemisphere (e.g. Kazakhstan and Crimea).
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Fish otoliths from the Lutetian of the Aquitaine Basin (SW France), a breakthrough in the knowledge of the European Eocene ichthyofauna
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Ypresian (early Eocene) stratigraphy of the Suvlu-Kaya reference section in the Bakhchisaray area (Crimea)
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Earliest Mysticete from the Late Eocene of Peru Sheds New Light on the Origin of Baleen Whales
- Although combined molecular and morphological analyses point to a late middle Eocene (38–39 million years ago) origin for the clade Neoceti (Odontoceti, echolocating toothed whales plus Mysticeti, baleen whales, and relatives), the oldest knownmysticete fossil dates from the latest Eocene (about 34 million years ago) of Antarctica [1, 2]. Considering that the latter is not the most stemward mysticete in recent phylogenies and that Oligocene toothed mysticetes display a broad morphological disparity most likely corresponding to contrasted ecological niches, the origin of mysticetes from a basilosaurid ancestor and its drivers are currently poorly understood [1, 3–8]. Based on an articulated cetacean skeleton from the early late Eocene(Priabonian, around 36.4million years ago) of the Pisco Basin, Peru, we describe a new archaic tooth-bearing mysticete, Mystacodon selenensis gen. et sp. nov. Being the geologically oldest neocete (crown group cetacean) and the earliest mysticete to branch off described so far, the new taxon is interpreted as morphologically intermediate between basilosaurids and later toothed mysticetes, providing thus crucial information about the anatomy of the skull, forelimb, and innominate at these critical initial stages of mysticete evolution. Major changes in the morphology of the oral apparatus (including tooth wear) and flipper compared to basilosaurids suggest that suction and possibly benthic feeding represented key, early ecological traits accompanying the emergence of modern filter-feeding baleen whales’ ancestors.
