Search

Of the 21 species recorded from the greater Azores region during the HMS ‘Challenger’ Expedition, 12 were newly introduced during the late 19th century. The respective types of these species are fixed, and eight species are redescribed based on scanning electron microscope analysis (Notoplites bilobus, Raxifabia minuta, Hemicyclopora canalifera, Smittoidea oratavensis comb. nov., Buskea ovalis comb. nov., Buskea fayalensis comb. nov., Celleporina ansata comb. nov. and Reteporella atlantica comb. nov.). Another four species are merely dealt with shortly either because the material is insufficiently preserved for a thorough revision (Columnella gracilis, Carbasea pedunculata), or because the species have recently been revised already (Notoplites clausus, Microporella hastigera). Moreover, two Azorean species that were introduced by later workers are synonymized with ‘Challenger’ species: S. oratavensis is considered a senior synonym of Smittia ensifera, and Lekythopora laciniosa is synonymized with C. ansata.

11 pages, 3 figures, 1 table, supplementary material https://doi.org/10.1126/sciadv.abm7452.-- Data and materials availability: All data needed to evaluate the conclusions in the paper are present in the paper, the Supplementary Materials, Dryad, and Zenodo, Phylogenetic relationships and the timing of evolutionary events are essential for understanding evolution on longer time scales. Cheilostome bryozoans are a group of ubiquitous, species-rich, marine colonial organisms with an excellent fossil record but lack phylogenetic relationships inferred from molecular data. We present genome-skimmed data for 395 cheilostomes and combine these with 315 published sequences to infer relationships and the timing of key events among c. 500 cheilostome species. We find that named cheilostome genera and species are phylogenetically coherent, rendering fossil or contemporary specimens readily delimited using only skeletal morphology. Our phylogeny shows that parental care in the form of brooding evolved several times independently but was never lost in cheilostomes. Our fossil calibration, robust to varied assumptions, indicates that the cheilostome lineage and parental care therein could have Paleozoic origins, much older than the first known fossil record of cheilostomes in the Late Jurassic, This project is funded by the European Research Council (ERC) under the European Union’s Horizon 2020 research and innovation programme (grant agreement no. 724324 to L.H.L.). Extra funding for specific sampling expeditions were provided by the National Science Centre of Poland (grant PANIC/2016/23/B/ST10/01936 to P.K.), the ASSEMBLE Plus (Horizon 2020), the Leverhulme Trust (Research Project Award RPG-2016-429 to A.W.), the Russian Science Foundation (grant 18-14-00086 to A.N.O.), Conselho Nacional de Desenvolvimento Científico e Tecnológico, Brazil [PQ-CNPq 308768/2018-3], Fundação de Amparo à Pesquisa do Estado de São Paulo, Brazil [FAPESP 19/17721-9] and the DISTANTCOM project (CTM2013-42667/ANT to C. Avila). B.F. was supported by Beatriu de Pinós (2019-BP-00183), funded by the AGAUR (Government of Catalonia) and by the Horizon 2020 programme under the Marie Skłodowska-Curie grant (no. 801370). The CAML-CEAMARC cruise of RV Aurora Australis (IPY project no. 53) were supported by the Australian Antarctic Division, the Japanese Science Foundation, the French Polar Institute IPEV, and the Muséum national d’Histoire naturelle, led by voyage leader, M. Riddle, With the institutional support of the ‘Severo Ochoa Centre of Excellence’ accreditation (CEX2019-000928-S)

Located on the northern coast of Santa Maria Island (Azores Archipelago, central North Atlantic), the Lagoinhas section preserves a carbonate buildup correlated with Marine Isotope Substage (MIS) 5e, the warmest interval of the Last Interglacial. The buildup is formed mainly by crustose coralline algae (CCA) identified as Spongites sp., and some subordinate crusts of Lithophyllum sp. and Neogoniolithon sp., as well as cf. Titanoderma sp. Extant CCA buildups are not recorded in the archipelago. Herein, we describe in detail the morphological and taphonomical features of the Lagoinhas CCA buildup and interpret the environment in which it grew. Additionally, this buildup is compared with another of similar age, exposed in the Prainha-Praia do Calhau section on the island's opposite southern coast. The hydrodynamic regime appears to play a crucial role in the development of Azorean CCA buildups during the MIS 5e. We thank Direccao Regional da Ciência e Tecnologia (Regional Government of the Azores), FCT (Fundação para a Ciência e a Tecnologia) of the Portuguese Government, and Camara Municipal de Vila do Porto for financial support. We also acknowledge the field assistance of Camara Municipal de Vila do Porto. We are grateful to the organizers and participants of the 16 editions of the International Workshop Palaeontology in Atlantic Islands who helped with fieldwork (2002 2020). A.C.R. was supported by a grant SFRH/BPD/117810/2016 from FCT (Fundação para Ciência e Tecnologia), Portugal. S.P.A. and R.S.R. acknowledge their research contracts (IF/00465/2015 and IF/01641/2015, respectively) funded by Fundação para a Ciência e a Tecnologia (FCT). C.S.M. is benefiting from a PhD grant M3.1.a/F/100/2015 from Fundo Regional para a Ciência e Tecnologia (FRCT). This work was supported by FEDER funds through the Operational Programme for Competitiveness Factors -COMPETE, by Portuguese National Funds through FCT under the projects UID/BIA/50027/2013, UID/BIA/00329/2013-2023, POCI-01-0145-FEDER-006821, PLATMAR (PTDC/GEO-GEO/0051/2014) and under DRCT-M1.1.a/005/Funcionamento-C-/2016 (CIBIO-A) project from FRCT, and by FEDER funds (in 85%) and by funds of the Regional Government of the Azores (15%) trough Programa Operacional Acores 2020, in the scope of the projects "AZORESBIOPORTAL -PORBIOTA": ACORES-01-0145FEDER-000072 and VRPROTO -Virtual Reality PROTOtype: the geological history of "Pedra-que-pica": ACORES-01-0145-FEDER000078. A.U. benefited from additional support by the Jagiellonian University. info:eu-repo/semantics/publishedVersion

The Turonian–Coniacian continental fossil record in Europe is scarce. Here we present a new fossil assemblage of early Coniacian age that was systematically collected from the coal-bearing Gosau Group of the Tiefengraben locality near St. Wolfgang, Austria. The diverse assemblage is composed of at least 60 taxa including sporomorphs and Normapolles-related pollen, seeds and leaves of angiosperms and gymnosperms, charophytes, gastropods, bivalves, ostracods, termites, fishes, crocodiles and dinosaurs. Concerning charophytes, ostracods, gastropods, crocodiles and dinosaurs, the discovered specimens either extend the temporal and spatial range of specific groups (in some cases as possible relict forms) or suggest the occurrence of new taxa. The discovered remains of algae, molluscs, ostracods, calcareous nannofossils and lepisosteid fish represent a mixed faunal assemblage from different palaeohabitats, from marginal marine to low salinity and freshwater or terrestrial environments. As Normapolles-related angiosperm plants dominate the flora with a relatively high number of dentate leaves, a slightly cooler microenvironment compared to other Turonian–Coniacian Central European localities is indicated. The characteristically grooved crocodylian teeth of Tiefengraben differ from the previously known Upper Cretaceous European crocodyliform teeth and suggest a more diverse crocodyliform fauna in the region. Dinosaurs are represented by teeth of at least three different theropods, the largest of which is referred here to as basal tetanurans. The fossil assemblage of this early Gosau Group occurrence is of great importance for our understanding of the continental floristic and faunistic composition of the western Tethyan archipelago during the Cenomanian–Campanian gap.

The Mediterranean bryozoan fauna is considered to be well studied compared to other marine areas of the world. However, in the Levantine Basin, bryozoan diversity has not yet been adequately documented. This report presents the first systematic and most comprehensive study of bryozoans sampled in Cyprus during census surveys from 2011 to 2018. The specimens were collected between 9 and ~620 m depth from several habitat types (mainly soft-bottom environments but also hard natural/artificial substrata, ancient shipwrecks, a marine cave, and deep-water coral habitats) around the island by means of bottom trawls, remotely operated vehicles, and scuba diving. The surveys produced a total of 91 species, 26 of which (=28%) are new records for the Levantine Basin, and 10 (=11%) are probably new to science. Our results thus show that the diversity of bryozoans in the eastern Mediterranean Sea is still significantly underestimated.

The bowl-shaped trace fossil Piscichnus waitemata Gregory 1991 appears in Pliocene sandstones from Santa Maria Island (Azores Archipelago), extensively excavated during a stage of island evolution when the volcanic edifice was a guyot (flat-topped seamount) isolated in the NE Atlantic. The host sediments were deposited at depths from the intertidal zone to fair-weather wave base in a tropical climate under the influence of periodic storms and hurricanes. The traces were produced by ray fishes hunting for polychaetes, crustaceans and bivalves living in the sediment, similar to present-day nearshore, warm waters in the Azores, Baja California Sur (Mexico), and New Zealand, from which examples of feeding depressions are drawn (incipient Piscichnus). While P. waitemata is abundantly present in planar sediments on top of the guyot, far fewer trace fossils occur in sandstone deposited on the guyot's margins. Presumably, the different densities of ray holes in the two sedimentary bodies were a response to lesser availability of prey, lower seawater temperatures (due to greater depths), and a more dynamic environment in which life conditions were less favorable. Moreover, the potential preservation of bowl-shaped depressions was lower in this setting, given the steepness of the seafloor, stronger currents, and constant sediment mobility. The top of the guyot was a more favorable habitat, refuge and/or nursery ground for many ray fishes. Measurement of the diameters of the ray holes indicate three distinct size classes, which may suggest that several species were responsible for their formation.

Bryozoan records from the shores and upper shelf (≤50 m depth) of the remote Azores Archipelago (central North Atlantic) have been analyzed, along with unpublished data and data from recent surveys. A checklist of 67 shallow-water species is hereby compiled for the region, of which more than one third represent records from campaigns conducted during the last 20 years. A classification on the origin of the species indicates that the majority (62%) are cryptogenic while 27% (n = 18) are considered native. Given the natural limitations for genetic exchange between the archipelago’s bryozoan populations and those from neighboring shores, the taxa presently considered as cryptogenic may yield a considerable amount of endemic species after taxonomic revision. The remaining 11% are confirmed as non-indigenous species, highlighting the importance of human-mediated transport in considerably enhancing the diversity of bryozoans in remote oceanic archipelagos, which would otherwise be off-limits to their natural dispersal capacity. In view of the need to quantitatively evaluate the certainty of species-level identification when assembling such biodiversity inventories, we have developed a method to attribute a degree of certainty to species records. The application of this method to the current checklist highlights the importance of further studies to ascertain the identification of many species recorded for the Azores, and to be able to categorize them confidently as either native, cryptogenic or non-indigenous.

The Azores, Madeira, Selvagens, Canary Islands and Cabo Verde are commonly united under the term “Macaronesia”. This study investigates the coherency and validity of Macaronesia as a biogeographic unit using six marine groups with very different dispersal abilities: coastal fishes, echinoderms, gastropod molluscs, brachyuran decapod crustaceans, polychaete annelids, and macroalgae. We found no support for the current concept of Macaronesia as a coherent marine biogeographic unit. All marine groups studied suggest the exclusion of Cabo Verde from the remaining Macaronesian archipelagos and thus, Cabo Verde should be given the status of a biogeographic subprovince within the West African Transition province. We propose to redefine the Lusitanian biogeographical province, in which we include four ecoregions: the South European Atlantic Shelf, the Saharan Upwelling, the Azores, and a new ecoregion herein named Webbnesia, which comprises the archipelagos of Madeira, Selvagens and the Canary Islands., SCOPUS: ar.j, info:eu-repo/semantics/published

Hazards and disasters have occurred throughout Earth's History and thus the geological record is an important resource for understanding future hazards and disasters. The Earth Science Group (ESG) of the Consortium of European Taxonomic Facilities (CETAF) carried out a “Hazard and Disaster Event Survey” to identify Earth Science collections in European museums that represent hazards and disasters throughout the geological record, and recent times. The aim is to use the collections within the survey as an educational and research resource that promotes the importance of museum collections for understanding past and future hazard and disaster events. The survey pinpointed a wide variety of hazards (e.g. earthquakes, volcanism, floods, impact events, etc.), representing a vast time span in Earth’s history (Proterozoic to Holocene), that are documented in the collections of the participating museums. Each hazard and disaster event has been described in terms of how they are preserved (e.g. fossil record or rock record), spatial scale, impact on life, and geological age. Here we showcase seven examples in detail which include well-known and less-known events from the survey that have contributed to our understanding of hazard and disaster processes and their impact on life. Also we present general conclusions and lessons learnt from the “Hazard and Disaster Event Survey”.

A synthetic model is presented to enlarge the evolutionary framework of the General Dynamic Model (GDM) and the Glacial Sensitive Model (GSM) of oceanic island biogeography from the terrestrial to the marine realm. The proposed ‘Sea‐Level Sensitive’ dynamic model (SLS) of marine island biogeography integrates historical and ecological biogeography with patterns of glacio‐eustasy, merging concepts from areas as diverse as taxonomy, biogeography, marine biology, volcanology, sedimentology, stratigraphy, palaeontology, geochronology and geomorphology. Fundamental to the SLS model is the dynamic variation of the littoral area of volcanic oceanic islands (defined as the area between the intertidal and the 50‐m isobath) in response to sea‐level oscillations driven by glacial–interglacial cycles. The following questions are considered by means of this revision: (i) what was the impact of (global) glacio‐eustatic sea‐level oscillations, particularly those of the Pleistocene glacial–interglacial episodes, on the littoral marine fauna and flora of volcanic oceanic islands? (ii) What are the main factors that explain the present littoral marine biodiversity on volcanic oceanic islands? (iii) How can differences in historical and ecological biogeography be reconciled, from a marine point of view? These questions are addressed by compiling the bathymetry of 11 Atlantic archipelagos/islands to obtain quantitative data regarding changes in the littoral area based on Pleistocene sea‐level oscillations, from 150 thousand years ago (ka) to the present. Within the framework of a model sensitive to changing sea levels, we discuss the principal factors affecting the geographical range of marine species; the relationships between modes of larval development, dispersal strategies and geographical range; the relationships between times of speciation, modes of larval development, ecological zonation and geographical range; the influence of sea‐surface temperatures and latitude on littoral marine species diversity; the effect of eustatic sea‐level changes and their impact on the littoral marine biota; island marine species–area relationships; and finally, the physical effects of island ontogeny and its associated submarine topography and marine substrate on littoral biota. Based on the SLS dynamic model, we offer a number of predictions for tropical, subtropical and temperate volcanic oceanic islands on how rates of immigration, colonization, in‐situ speciation, local disappearance, and extinction interact and affect the marine biodiversity around islands during glacials and interglacials, thus allowing future testing of the theory.

Hazards and disasters have occurred throughout Earth's History and thus the geological record is an important resource for understanding future hazards and disasters and its Impact. The Earth Science Group (ESG) of the Consortium of European Taxonomic Facilities (CETAF) carried out a “Hazard and Disaster Event Survey” to identify Earth Science collections in European museums that represent hazards and disasters throughout the geological record, and recent times. The aim is to use the collections within the survey as an educational and research resource that promotes the importance of museum collections for understanding past and future hazard and disaster events. The survey pinpointed a wide variety of hazards (e.g. earthquakes, volcanism, floods, impact events, etc.), representing a vast time span in Earth’s history (Proterozoic to Holocene), that are documented in the collections of the participating museums. Each hazard and disaster event has been described in terms of how each is preserved (e.g. fossil record or rock record), spatial scale, impact on life and biodiversity, and geological age. The results were published in Research ideas and outcomes journal RIO (https://riojournal.com/article/34087/) as seven examples, which include well-known and less-known events from the survey that have contributed to our understanding of hazard and disaster processes and their impact on life and biodiversity. For better visualisation and education purposes we also created and specialised website, which will be launched during summer 2019. In the presentation we will talk about general conclusions and lessons learnt from the “Hazard and Disaster Event Survey”.

Pliocene body fossils from Santa Maria Island, Azores, have been studied for decades, but only more recently have ichnofossils received their due attention. Calcareous Pliocene deposits from the Baia de Nossa Senhora section contain numerous, diverse, well-preserved natural casts of invertebrate borings. The study of this type of fossils adds to knowledge on the dispersal of benthic faunas across oceans to volcanic oceanic islands. The borings belong to seven ichnogenera and twenty-two ichnotaxa at the ichnospecies level with more than half pertaining to Entobia, which is produced by clionaid sponges. Other borings found were produced by bivalves (Gastrochaenolites), polychaete worms (Caulostrepsis and Maeandropolydora), sipunculid worms (Trypanites), phoronid worms (Talpina) and ctenostome bryozoans (Iramena). The occurrence, ichnogeny, distribution and preservational state of the borings suggest that the bearing bioclasts have been exposed for several years on the sea floor. The borings derive from different bathymetric zones on the shelf, and their formation took place during several bioerosional phases. The association of borings belongs to the Entobia ichnofacies, which is typical of carbonate rocky shores, and shows close similarity to those described from the Paratethys, Mediterranean and partly the eastern Atlantic regions. This fits the idea that most of the Neogene shallow-water marine fauna in the Azores is biogeographically related to the eastern Atlantic shores.

The family Strombidae is one of the twenty-three families and subfamilies of gastropods associated with tropical environmental conditions, and therefore useful as a biogeographical and paleoclimatic proxy. Today, the strombid genus Persististrombus is represented in the NE Atlantic by a single species restricted to the tropical Mauritanian–Senegalese Province. This work reports the occurrence of Persististrombus coronatus from the lower Pliocene of Santa Maria Island in the Azores Archipelago. Based on this occurrence, and on the Mio-Pliocene fossil record of the NE Atlantic oceanic islands, paleoclimatological considerations are discussed, which allow, for the first time, to include the Azores and the other Macaronesian islands in a wider context of the NE Atlantic paleobiogeographical molluscan provinces. Late Miocene to present day molluscan biogeographic units, ranging in latitude from 60°N down to 17°S, are here defined and the boundaries of the proposed climatic zones are outlined. We suggest that during the upper Miocene–lower Pliocene, the paleoclimate at Santa Maria Island was drastically different from that seen at those latitudes today, with mean annual sea surface temperatures (SSTs) about 3.7 °C to 6.3 °C higher than the present-day 20.6 °C, and with mean monthly SSTs ranging from 20 °C to 28 °C, with six months with mean SSTs over 24 °C, conditions typical of a tropical setting.

The origin of the Paleontological Collection of the Upper Austrian State Museum goes back to the 1830s. Historically subordinate to mineralogy and petrology, today’s Paleontological Collection is the largest and scientifically most important of the three subunits of the museum’s Geoscience Collections. Fossils from the Upper Austrian part of the Mesozoic Northern Limestone Alps, especially Triassic ammonoids, and from the Cenozoic Alpine Foreland Basin, in particular marine and terrestrial mammals, form the backbone of the collection.

Massive fossil shell accumulations require particular conditions to be formed and may provide valuable insights into the sedimentary environments favouring such concentrations. Shallow-water shell beds appear to be particularly rare on reefless volcanic oceanic islands on account of narrow, steep and highly-energetic insular shelves where the potential for preservation is limited. The occurrence of an exceptional coquina (Pedra-que-pica) within the Miocene–Pliocene deposits of Santa Maria Island (Azores), therefore provides a rare opportunity to understand the conditions that led to the formation and preservation of a massive shell bed at mid-ocean insular setting. This study provides a detailed analysis regarding a 10–11-m-thick bivalve-dominated fossil assemblage exposed at Pedra-que-pica on Santa Maria Island in the Azores. Integration of taphonomical, palaeoecological and sedimentological observations are used to reconstruct the genesis of the coquina bed and related events, and to discuss why such exceptional sedimentary bodies are so rare on shelves around reefless volcanic oceanic islands. The sequence at Pedra-que-pica demonstrates a complex succession of sedimentary environments in response to the drowning of an existing coastline during a period of rapid sea-level rise. The Pedra-que-pica shell bed incorporates storm-related materials and possible debris falls that originated nearby in a shallow and highly productive carbonate factory. Deposition took place below fair-weather wave base, at around 50 m depth, as inferred from the overlying volcanic succession. The preservation of this coquina was favoured by deposition on a platform laterally protected by a rocky spur, combined with rapid burial by water-settled volcanic tuffs and subsequent volcanic effusive sequences. The recent exhumation of the deposit is the result of island uplift and subsequent erosion.

Ten new species belonging to three new genera ( Atlantisina gen. nov., Bathycyclopora gen. nov., Calvetopora gen. nov.) of umbonulomorph bryozoans from northeastern Atlantic seamounts, islands, and the continental slope are introduced. We furthermore erect the new family Atlantisinidae fam. nov. for these genera. Eight new species belong to the new genus Atlantisina : Atlantisina atlantis gen. et sp. nov. (type species), A. acantha gen. et sp. nov., A. gorringensis gen. et sp. nov., A. inarmata gen. et sp. nov., A. lionensis gen. et sp. nov., A. meteor gen. et sp. nov., A. seinensis gen. et sp. nov., and A. tricornis gen. et sp. nov. The genus Bathycyclopora gen. nov. is introduced for ? Phylactella vibraculata Calvet from the Azores, and also includes Bathycyclopora suroiti gen. et sp. nov. The type species of Calvetopora gen. nov. is Lepralia inflata Calvet from the Gulf of Cadiz; this genus also includes Calvetopora otapostasis gen. et sp. nov. and another species left in open nomenclature. Of the 13 species described herein, 11 occur on seamounts and islands, and nine species are endemic to a single seamount, island or station. The present results show that bryozoans provide striking examples of the function of seamounts as areas of endemism, most likely intrinsically linked to the low dispersal abilities of bryozoan larvae.

The diversity of calcareous epiliths along a bathymetrical transect spanning the intertidal to bathyal (0–500 m) was investigated during a two-year carbonate cycling experiment deployed in the Faial Channel, Azores. The epilith inventory comprises 47 taxa of bryozoans, 9 serpulids, 3 bivalves, 3 cirripeds, 3 foraminiferans, 2 vermetid gastropods, and 1 scleractinian coral, along with 6 rhodophyte morphotypes. Colonised surface area, carbonate accretion rates, and biodiversity peak in the deeper euphotic zone (15 and 60 m), where mature biocoenoses were established after 2 years exposure, whereas colonisation was retarded at dysphotic and aphotic depths. Particularly in the photic zone, colonised surface area, accretion rates, as well as species richness and abundance were higher on down-facing compared to up-facing surfaces. Analyses of similarity (ANOSIM) and non-metrical multidimensional scaling (NMDS) of species abundance data revealed that water depth and substrate orientation were the dominant factors controlling the community structure as a result of direct (photosynthesis) and indirect (bioerosion pressure; nutrient supply) effects of the light regime, while exposure time and substrate type had little influence. The same hierarchy applies for the ichnodiversity of bioerosion traces, but with an inverse pattern in case of substrate orientation, reflecting the interaction of encrustation and bioerosion. Positive net carbonate production rates support the development of oyster bioherms and heterozoan-dominated carbonate/volcaniclastic sediments accumulating in the Faial Channel and adjacent slope. A comparison with biogenic sediments from other Macaronesian archipelagos and seamounts demonstrates the abundance and diversity of non-tropical heterozoan carbonates in oceanic islands.

Genus Lentiarenium Voss gen. nov. urn:lsid:zoobank.org:act:A67C71FB-CBC3-460E-953C-5774A3EA9939 Type species Halitherium cristolii Fitzinger, 1842 Diagnosis Dugongid based on the following combination of synapomorphies: absence of alisphenoid canal, open foramen ovale, loss of permanent ffth premolar, and squamosal reaching temporal crest. Differs from the Dugonginae (Crenatosiren Domning, 1991, Nanosiren Domning & Aguilera, 2008, Dugong Lacépède, 1799, Rytiodus Lartet, 1866, Corystosiren Domning, 1990, Callistosiren Vélez-Juarbe & Domning, 2015, Bharatisiren Bajpai & Domning, 1997, Domningia Thewissen & Bajpai, 2009, Kutchisiren Bajpai, Domning, Das, Vélez-Juarbe & Mishra, 2010, Dioplotherium Cope, 1883 and Xenosiren Domning, 1989), the Hydrodamalinae Simpson, 1932 (Dusisiren Domning, 1978 and Hydrodamalis Retzius, 1794), and other dugongid genera (Eotheroides Palmer, 1899, Prototherium De Zigno, 1887, Eosiren Andrews, 1902, Caribosiren Reinhart, 1959, Priscosiren Vélez-Juarbe & Domning, 2014b, Metaxytherium De Christol, 1840, and other species formerly lumped under “ Halitherium ”) by displaying the following unique combination of plesiomorphies: frontal roof fat; supraorbital process of the frontal dorsoventrally fattened with well-developed, prominent posterolateral corner; supraoccipital wider dorsally than ventrally; exoccipitals meet in a suture dorsal to the foramen magnum; posttympanic process with a prominent anteroventral process for attachment of m. sternomastoideus; paroccipital process of exoccipital long, reaching as far ventrally as occipital condyles; accessory mental foramina present; horizontal ramus of mandible slender dorsoventrally; permanent premolars (P2/p2 – P4/p4) present. Synapomorphies: nasals reduced and not meeting in midline (shared with Eosiren imenti Domning et al., 1994, Caribosiren, Priscosiren, and all later dugongid taxa), nasal incisure at posterior end of the mesorostral fossa deep, extending posterior to the supraorbital processes of the frontals (shared with some Metaxytherium spp., dugongines, and Hydrodamalis); strongly concave ventral border of the horizontal mandibular ramus (shared with Priscosiren, Metaxytherium spp., and dugongines), masticating surface of mandible broad (shared with Metaxytherium ssp., dugongines, and hydrodamalines). In contrast to the similar species Priscosiren atlantica it has a supraorbital process with the posterolateral corner projecting posteriorly; prominent temporal crests on frontal and parietal; supraoccipital distinct in height, only slightly wider than high. Etymology A combination of the Latin terms for the Linz Sands (Lentia and arenium), the informal name for the upper Oligocene sediments in which the species was found.

Lentiarenium cristolii (Fitzinger, 1842) comb. nov. Figs 2–10, Tables 1–5 Halitherium cristolii Fitzinger, 1842: 71, pl. 1. Metaxytherium (?) pergense Toula, 1899: 459, pl. 12. Halitherium abeli Spillmann, 1959: 36, pls. 1–4, fgs 19–20, 22, 24–27, 29b, 31–32, 33b, 34. Manatus christolii – De Blainville 1844: 122. Metaxytherium christolii – Laurillard 1846: 172. Halianassa collinii – Meyer 1847: 189, 578 (partim). — Ehrlich 1850: 14–15, fgs a–c. — Ehrlich 1855: 3, pls. 1–2, corresponding fgs on pages 14–17. Halitherium schinzii – Peters 1867: 310. Halitherium schinzi – Lepsius 1882: 164 (partim). Halitherium christoli – Abel 1904: 25, pl. 1, fgs 12–13, pl. 2, fgs 4, 11, 17, pl. 5, fg. 8, fg. 1. — Spillmann 1959: 17, fgs 8–18, 21, 23, 28, 29a, 30, 33a; 1969: 62, pl. 8, fg. 2; 1973: 198, pl. 40, fg. 4. Halitherium pergense – Spillmann 1959: 11, fgs 6–7; 1969: 61, fg. 1; 1973: 197, pl. 39, fgs 1–2. Halitherium abeli – Spillmann 1969: 62, pl. 9, fg. 3; 1973: 205. Diagnosis As for the genus. Type Material Lectotype (present designation) A mandible (OLL 2012/1) of an adult individual (based on the presence of a large retromolar space and erupted m3 in wear) with left dp5–m2 and right m1–3, “Sicherbauer” sandpit, Linz. Paralectotypes Fragment of right maxilla with worn M1 crown and remnants of DP5 roots (OLL 2012/2), and an isolated crown of M3 (OLL 2012/3) from the right side, both from the “Sicherbauer” sandpit, Linz. Holotype (by monotypy) of Metaxytherium pergense Cast of a parietal-supraoccipital skullcap (OLL 1899/11), sandstone quarry near the town of Perg. Holotype (by original designation) of Halitherium abeli Mandible of an adult individual (based on the presence of a large retromolar space and erupted m3 in wear), fragments of basicranium, cervical and other vertebrae (OLL 1939/257), “Limoni” sandpit, Linz. Referred material OLL 1854/327, 1863/184, 1917/7, 1921/71, 1926/394, 1926/395, 1927/200, 1928/82, 1931/21, 1931/263, 1948/33, 2012/4, 2012/5, 2012/6, 2012/7, 2013/1. For a detailed listing of the preserved skeletal parts see Table 1. Type horizon and locality “Sicherbauer-Sandgstätte”, a former sandpit within the city limits of Linz (Upper Austria). Linz-Melk Formation, Linzer Sande (= Linz Sands), upper Oligocene, lower Egerian (Chattian). Range and distribution Known only from the upper Oligocene of Linz and the surrounding area. Description The following description is based on the available sirenian material housed in OLL, regardless of the different species that were proposed in the past. It will be outlined in detail in the Discussion why the respective skeletal material represents a single species. Lentiarenium cristolii is known from cranial and postcranial elements. However, the premaxilla and lacrimal are unknown as are the pelvis, zeugopod and autopod. The following description is mainly based on a partial skull (OLL 1926/394) and two mandibles (OLL 1939/257 and OLL 2012/1). PREMAXILLA. The premaxilla is not preserved in any specimen but some morphological characters can be indirectly determined. The external nares are retracted and enlarged (Fig. 2), as in all sirenians, and reach beyond the anterior margin of the orbit. Judging from the recesses in the anterior margin of the frontal, the nasal processes are not broadened and bulbous at their posterior ends but taper, having lengthy overlap with the frontals. The angle of the rostrum most likely exceeds 50° considering the defection of the mandibular symphysis of about 60° (Fig. 7). NASAL. The exact status of the nasals cannot be determined without doubt due to the poor preservation of the nasal area in specimen OLL 1926/394 (Fig. 2). Judging from the right anteromedial margin of the frontals, which is not damaged, but smooth without an attachment area for the nasals, these elements are at least considered to have been small without meeting in the midline. A nasal incisure is present at the posterior end of the mesorostral fossa, but unlike in Metaxytherium albifontanum (Velez-Juarbe & Domning, 2014a) and Priscosiren atlantica (Velez-Juarbe & Domning, 2014b) it is deep, extending posterior to the supraorbital processes of the frontals, though not to the extent seen in dugongines like Crenatosiren olseni (Domning 1997). It is uncertain whether the nasals were fused or coalesced with the frontals. ETHMOIDAL REGION. The ethmoid is incompletely preserved and not easily observable in all aspects. A prominent perpendicular plate of the mesethmoid is visible in dorsal and anterior views of the skull OLL 1926/394 (Fig. 2). This vertical wall measures 10 mm to 15 mm in width, is narrower dorsally and ventrally, and apparently also becomes thinner posteriorly. Ventrally, the perpendicular plate is fused with the likewise distinctly developed vomer. On the right side of the skull, and medial to the frontal (Fig. 2), the almost complete large ethmoturbinal (concha maxima ethmoidalis (Kaiser 1974)) extends nearly parallel to the mesethmoid. Its left counterpart is only fragmentarily preserved. The crista galli and lamina papyracea are either not preserved or not visible. VOMER. The vomer is exposed on the ventral side of the skull OLL 1926/394 but broken anteriorly (Fig. 3). It is fused with the presphenoid posteriorly and forms the cranial extension of its median crest. The vomer is triangular in cross section, frmly fused with the ethmoid via its fat dorsal surface, and contacts the maxilla laterally. In lateral view (Fig. 4B), the vomer is also visible through the orbit due to the incomplete preservation of the skull. FRONTAL. In dorsal view (Fig. 2), the frontal roof is fat between the temporal crests, and bears no knoblike bosses as present in some dugongines (e.g., Crenatosiren olseni (Domning 1997)). The straight to slightly concave anterior margin of the frontal has no internasal process. The temporal crests form distinct keels (morphotype B; Domning 1988) and are as prominent on the frontal as on the parietal. In lateral view (Fig. 4B), the supraorbital process is dorsoventrally fattened with its dorsal surface inclined gently ventrolaterad. Its lateral margin is not divided, and it has a prominent posterolateral corner that projects posteriorly. An orbitotemporal crest is distinct relative to what is observed in Metaxytherium albifontanum (Velez-Juarbe & Domning 2014a), and forms a craniocaudally-extending ridge. The lamina orbitalis is signifcantly less than 10 mm thick. PARIETAL. The parietal roof (Fig. 2) is fat between the temporal crests and characterised by a strong intertemporal constriction that reaches its maximum behind the centre of the skull roof with the parietal bulging laterally. An external sagittal crest is not developed. The frontal processes of the parietal are short and do not exceed half the length of the frontal in the midline, a condition similar to that in Priscosiren atlantica (Velez-Juarbe & Domning 2014b). The parietal is longer than the frontal, and the overall proportions of the cranial roof indicate a slight brachycephaly when the value of the frontal length is divided by the width of the supraoccipital, i.e., the ratio l FP/w SO, which is below 2. In endocranial view (Fig. 3), the bony falx cerebri extends from a prominent tentoric process and fattens out anteriorly before reaching the frontoparietal suture. The tentorium osseum is well developed and an internal parietal spine (or tentorial process as illustrated in Voss (2008: Fig. 4B)) is missing. On both sides of the bony falx, the fat internal parietal surface shows the depressions for the superior parts of the brain hemispheres. SUPRAOCCIPITAL. This element is widest dorsally rather than ventrally (Fig. 4A), relative to what is observed in Metaxytherium spp. (e.g., M. albifontanum (Velez-Juarbe & Domning 2014a)). The supraoccipital is only slightly wider than high (width to height ratio Crenatosiren olseni (Domning 1997). Dorsally, the nuchal crest is constantly narrow along its transversal length and relatively sharp-edged. It makes up the dorsolateral margin of the supraoccipital. The external occipital protuberance rises above the parietal roof and is also prominent posteriorly. Ventrad, the protuberance continues as the external occipital crest that forms a distinct ridge, which slightly fattens out after one third of the supraoccipital’s height, almost reaching its ventral margin. Dorsolateral to this median ridge the deep and large insertions for the semispinalis capitis muscle occupy about the upper third of the external lamina. The area of the muscle insertion is triangular and defned by distinct ridges medioventrally and the nuchal crest dorsolaterally. The ventral margin of the supraoccipital forms an angle of approximately 135° in specimen OLL 1926/394. Specimen OLL 1899/11 (Fig. 5), formerly designated as the holotype of “ Halitherium ” pergense but now referred to Lentiarenium cristolii, also shows a distinct nuchal crest. However, the protuberance, median ridge and defnitions of the muscle insertions are less prominently developed than in OLL 1926/394, indicating its juvenile status. In interior view (Fig. 3), the supraoccipital is fat with the exception of longitudinal bulges dorsolaterally that are merged in the median plane and separated by a deep transverse sulcus from the tentorium osseum. Posterolaterally, the parietals extend between the supraoccipital and squamosal, forming a short fange. EXOCCIPITAL. The dorsal parts of these paired elements are not preserved in any specimen. However, the total length of the ventral margin of the supraoccipital in OLL 1926/394 (Figs 3, 4A) reveals the articulation surface for the exoccipitals, indicating that these bones evidently meet in a suture dorsal to the foramen magnum. Additionally, specimen OLL 1939/257 preserves the ventralmost parts of the exoccipitals, which Spillmann (1959: fg. 19) illustrated in ventral view. During the personal examinations, the paroccipital processes were detected to be long, projecting as far ventrally as the occipital condyles, which is similar to what can be observed in some dugongines (e.g., Nanosiren garciae Domning & Aguilera, 2008 and N. sanchezi Domning & Aguilera, 2008 (Domning & Aguilera 2008: fg. 3, 11)). Medioventral to the paroccipital processes, the hypoglossal foramen is not opened to form a notch or incisure but is well surrounded by bone. The supracondylar fossae are distinct and defne the occipital condyles across their entire width. BASIOCCIPITAL. An isolated basioccipital fused with the lower parts of the exoccipitals is preserved in specimen OLL 1939/257 (Spillmann 1959: fg. 19). It contributes to the occipital condyles ventrolaterally and extends craniad as a short, columnar bone. On its ventral side, the sphenooccipital eminences for the longus capitis muscles are concave and separated by a short but distinct ridge. Specimens OLL 1939/257 and 1926/394 (Fig. 3), in which either the basioccipital or basisphenoid is preserved, show smoothed attachment areas for the adjacent bone, indicating that the basioccipital and basisphenoid were not fused. On that basis, both specimens can be determined as subadults. BASISPHENOID, PRESPHENOID, ORBITOSPHENOID. In specimen OLL 1926/394, the sphenoidal region is clearly observable (Fig. 3). The basisphenoid has a fat ventral surface that is defned laterally by antero posteriorly-broad pterygoid processes. Cranially, the basisphenoid continues with a slight anterodorsal slope into the presphenoid. Both bones are frmly fused with each other and with the orbitosphenoid anterolaterally, the alisphenoid dorsolaterally, and the pterygoid posterolaterally. The median crest of the presphenoid is not prominently developed, which might be related to the state of preservation of the skull in this area, and only becomes distinct at the level of the adjacent vomer. On the lateral side of the skull (Fig. 4B), the orbitosphenoid is exposed and contributes to the anteromedial wall of the temporal fossa. The orbitosphenoid is defned by the frontal dorsally, the alisphenoid posterodorsally, and apparently by the maxilla ventrally. Its sutures with the palatine are not detectable. ALISPHENOID. The alisphenoid is visible in the lateral view of the skull (Fig. 4B). Its sutural contacts with the frontal, parietal and squamosal can be clearly determined. Furthermore, the alisphenoid forms the slightly uneven posterolateral side of the pterygoid process. An alisphenoid canal is absent, and the foramen ovale is opened to form a notch or incisure. PTERYGOID. As in other sirenians, the pterygoid is present on the posteromedial side of the pterygoid process but fully fused with the surrounding bones (Fig. 3). Though not well preserved in OLL 1926/394, the wing-shaped pterygoid processes each bear a dorsoventrally elongated pterygoid fossa posteriorly that extends above the level of the roof of the internal nares, relative to the condition observed in some dugongines like Dioplotherium manigaulti (Domning 1989). The distal ends of both pterygoid processes are somewhat damaged, although the distomedial angle of the right pterygoid process is still distinct and indicates a hamula process. PALATINE. Only the posteriormost parts of the palatines are preserved in OLL 1926/394, and are best observable on the right side (Fig. 3). There the palatine forms the anteromedial margin of the pterygoid process. Its sutures with the surrounding bones are only barely visible on the distal and medial sides of the pterygoid process and on the posterior side of the maxillary alveolar margin. MAXILLA. The zygomatic-orbital bridge (Fig. 3) is not completely preserved in any of the specimens. However, in the maxillary fragment of OLL 1939/257 its dimensions are 47 mm in minimum length and 17.5 mm in nearly original height (Spillmann 1959: fg. 20). On the basis of these data, the zygomaticorbital bridge can be clearly determined to be long anteroposteriorly, relative to what is observed in the genus Hydrodamalis (Domning 1978; Velez-Juarbe & Domning 2014a). Additionally, and in contrast to some hydrodamalines, e.g., Dusisiren jordani Kellogg, 1925 and Hydrodamalis cuestae Domning, 1978 (Domning 1978; Velez-Juarbe & Domning 2014a), it is only slightly elevated above the alveolar margin, and its posterior edge is thickened. Remnants of the infraorbital canal reveal no obstruction. SQUAMOSAL. The cranial part of the squamosal (Figs 2, 4B) extends up to the temporal crests but does not interrupt the course of the temporal crests, so that these reach the occipital nuchal crest. The posttympanic process is not club like distally (Fig. 4B), but concave anteroventrally for the attachment of the sternomastoid muscle. In the posterior view of the skull (Fig. 4A), a prominent sigmoid ridge is visible forming the laterocaudal margin of the squamosal. Posterolaterally, the mastoid foramen is present, flled by the periotic, and enclosed by the squamosal anteriorly, the exoccipital posteriorly, and the supraoccipital dorsally. Lateral to the braincase (Figs 2, 4B), each of the zygomatic processes projects from a zygomatic root that, though partially broken, is characterised by a distinct notch posteriorly. The zygomatic process is triangular in shape, tapering anteriorly. Its lateral and medial sides are fat to concave with the dorsal margin distinctly inclined inwards to form a sigmoid ridge. The posterodorsal end of the zygomatic process is straight to concave. The external auditory meatus is short mediolaterally and about as wide as high anteroposteriorly. Ventrally (Fig. 3), the elements of the mandibular articulation surface are elongated transversely. The mandibular fossa forms a distinct depression relative to the slightly convex tuberculum anteriorly. Posterior to the mandibular fossa, the postglenoid process forms a rounded and longitudinal knob, which rises above the level of the tuberculum. The posterior end of the zygomatic process, the processus retroversus, shows a moderate inward-directed infection in contrast to what is observed in the living dugong (e.g., Domning & Aguilera 2008; Velez-Juarbe & Domning 2014a). JUGAL. Only a fragmentarily preserved middle part of the right jugal is known from specimen OLL 1926/394 (Fig. 4B), indicating that a postorbital process is probably present. Considering the position and shape of the supraorbital processes of the frontal, the development of a postorbital bar can be excluded. The zygomatic process of the jugal is not preserved but according to its imprint on the ventral side of the zygomatic process of the squamosal it reaches the tuberculum, exceeding the diameter of the orbit. EAR REGION. In specimen OLL 1926/394, the right periotic is poorly preserved (Figs 3, 4A). It is not fused with the adjacent skull bones, and is set in a closely-ftting socket in the squamosal. The tegmen tympani is only indicated by its imprints on the dorsolateral side of the squamosal. It was most likely about as big as the mastoid or slightly smaller. The petrosal is fragmentarily preserved medioventrally, with the perilymphatic foramen apparently not separated into a fenestra rotunda and cochlea canaliculus. The processus fonticulus flls the mastoid foramen posteriorly (Fig. 4A). MANDIBLE (Table 3). The mandibular symphysis is broad, as is the masticating surface that is lacking a median furrow and houses four large and shallow alveoli for vestigial incisors and canines. This is best visible in OLL 1939/257 (Fig. 6A), which exhibits a completely preserved masticating surface, whereas in OLL 2012/1 (Figs 6B, 7A) the ventralmost end is broken. In lateral view (Fig. 7), the symphysis is higher than long and bears the mental foramen laterally, which is joined dorsoposteriorly by two accessory mental foramina on each side in specimen OLL 1939/257 (Fig. 7B). The accessory mental foramina are large relative to what is observed in more plesiomorph dugongid taxa, e.g., “ Halitherium ” taulannense (Sagne 2001a), but they are still smaller than the principal foramen. This observation is interpreted here in analogy with Trichechus (Domning 1982, 1994, and personal observations), as “true” accessory mental foramina, which are present in addition to and usually posterior to the large principal foramen. In the lectotype (OLL 2012/1; Fig. 7A), the mental foramen is broken off dorsoposteriorly, and therefore the accessory mental foramina are not identifable, but their open canals are merged with the main foramen. The overall build of the horizontal mandibular ramus appears to be broad dorsoventrally, but it is evaluated to be slender on the basis of its minimum dorsoventral height, which is smaller than 0.25 × the length of the mandible. The ventral border

Pywackia baileyi Landing in Landing et al., 2010, from the upper Cambrian Yudachica Member of Oaxaca State, southern Mexico, consists of small, phosphatic, proximally tapering cylindrical rods covered by shallow polygonal calices. The bryozoan-like morphology of this fossil prompted its interpretation as the first bryozoan known from the Cambrian. However, restudy of some of the original material, employing scanning electron microscopy for the first time, questions the assignment of Pywackia to the Bryozoa. Striking similarities between Pywackia and the modern pennatulacean octocoral Lituaria lead to an alternative hypothesis interpreting Pywackia an early fossil octocoral. While Pywackia is probably not a true pennatulacean, a group with a definitive fossil record stretching back only to the Late Cretaceous, it can be envisaged as having had a similar skeletal structure and ecology to Lituaria, the rods representing mineralized axes of tiny colonies that lived with their proximal ends buried in the sediment and distal ends covered by feeding polyps. Landing et al. (2010) considered the phosphatic composition of Pywackia specimens to be the result of diagenetic replacement, but the evidence is equivocal. If Pywackia had a primary phosphatic skeleton, this would support the hypothesized existence of phosphatic biomineralization early in the evolutionary history of Cnidaria, as well as providing further evidence that Pywackia is not a bryozoan.

Made available in DSpace on 2021-06-25T12:17:32Z (GMT). No. of bitstreams: 0 Previous issue date: 2016-11-23 Villanova Univ, Dept Biol, Villanova, PA 19085 USA Museu Nacl Hist Nat & Ciencia, Lisbon, Portugal Univ Brasilia, Dept Zool, Inst Ciencias Biol, BR-70910900 Brasilia, DF, Brazil Smithsonian Inst, Natl Museum Nat Hist, Washington, DC 20560 USA Sorbonne Univ, Museum Natl Hist Nat, ISYEB, Paris, France Univ Nacl Tucuman, San Miguel De Tucuman, Argentina King Saud Univ, Riyadh, Saudi Arabia Cornell Univ, Ithaca, NY USA Univ Fed Sao Paulo, Diadema, Brazil Upper Austrian Museum, Ctr Biol, Linz, Austria Villanova Univ, Villanova, PA 19085 USA Univ Salzburg, Salzburg, Austria Plazi, Bern, Switzerland Univ Brasilia, Brasilia, DF, Brazil Univ Sao Paulo, Ribeirao Preto, Brazil Zool Forsch Museum A Koenig, Bonn, Germany Museu Paraense Emilio Goeldi, Belem, Para, Brazil Russian Acad Sci, St Petersburg, Russia Pontificia Univ Catolica Rio Grande do Sul, Porto Alegre, RS, Brazil Museo Reg Sci Nat, Turin, Italy Univ Fed Rio Grande do Sul, Porto Alegre, RS, Brazil Royal Museum Cent Africa, Tervuren, Belgium Univ Nacl Autonoma Mexico, Mexico City, DF, Mexico Univ Innsbruck, Inst Ecol, Innsbruck, Austria Hasselt Univ, Hasselt, Belgium Univ Fed Pernambuco, Recife, PE, Brazil Univ Fed Espirito Santo, Vitoria, ES, Brazil Univ Nacl Misiones, Felix De Azara, Argentina Albany Museum, Grahamstown, South Africa Natl Museum, Bloemfontein, South Africa Senckenberg Nat Hist Sammlungen, Dresden, Germany Univ Estadual Paulista, Botucatu, SP, Brazil Stephen F Austin State Univ, Nacogdoches, TX 75962 USA Landesmuseum, Leonding, Austria Univ Camerino, Camerino, Italy Univ Fed ABC, Sao Bernardo, Brazil Univ Estadual Londrina, Museu Zool, Londrina, Parana, Brazil Senckenberg Res Inst, Frankfurt, Germany Museo Civ Storia Nat, Carmagnola, Italy Polskiej Akad Nauk, Muzeum & Inst Zool, Warsaw, Poland Museo Civ Storia Nat, Genoa, Italy Russian Acad Sci, Inst Zool, St Petersburg, Russia Univ Estadual Paulista, Sao Vicente, Brazil Sorbonne Univ, ISYEB, Museum Natl Hist Nat, Paris, France Port Elizabeth Museum, Port Elizabeth, South Africa Sam Noble Museum, Norman, OK USA Harvard Univ, Museum Comparat Zool, Cambridge, MA 02138 USA North West Univ, Potchefstroom, South Africa Museu Nacl, Rio De Janeiro, Brazil Nat Hist Museum, Basel, Switzerland Senckenberg Nat Kundemuseum, Gorlitz, Germany North Carolina Museum Nat Sci, Raleigh, NC USA Univ Rennes 1, Rennes, France Univ Sao Paulo, Museu Zool, Sao Paulo, SP, Brazil Amer Museum Nat Hist, New York, NY 10024 USA Univ Huddersfield, Huddersfield, W Yorkshire, England North Dakota State Univ, Fargo, ND USA Univ Sao Paulo, Sao Paulo, SP, Brazil Fac Sci Sfax, Sfax, Tunisia DPTC PC, Manaus, Amazonas, Brazil Louisiana State Univ, Museum Nat Sci, Baton Rouge, LA 70803 USA Zool Survey India, Kolkata, India Univ Tennessee, Chattanooga, TN USA Ohio State Univ, Columbus, OH 43210 USA Univ Luterana Brasil, Museu Ciencias Nat, Canoas, Brazil Univ Firenze, Florence, Italy Univ Ovidius Constanta, Constanta, Romania Univ Mississippi, Oxford, MS USA Royal Belgian Inst Nat Sci, Brussels, Belgium Univ New Mexico, Albuquerque, NM 87131 USA Inst Nacl de Pesquisas da Amazonia, Manaus, Amazonas, Brazil Univ Stellenbosch, Matieland, South Africa Univ Fed Minas Gerais, Belo Horizonte, MG, Brazil CIBIO Ctr Invest Biodiversidade & Recursos Genet, Vairao, Portugal Museum Hist Nat, Geneva, Switzerland Univ Fed Mato Grosso, Cuiaba, Brazil Univ Austral Chile, Valdivia, Chile Univ Malaysia, Sarawak, Malaysia Indian Inst Sci, Bangalore, Karnataka, India Scottish Assoc Marine Sci, Oban, Argyll, Scotland Sam Houston State Univ, Huntsville, TX 77340 USA Museo Nacl Ciencias Nat, Madrid, Spain Sorbonne Univ, CR2P, Museum Natl Hist Nat, Paris, France Drexel Univ, Acad Nat Sci, Philadelphia, PA 19104 USA Univ Richmond, Richmond, VA 23173 USA Ctr Pesquisas Cacau, Itabuna, Brazil Univ Torino, Turin, Italy Soc Hist Nat Alcide dOrbigny, Aubiere, France Wolfden Sci Consulting, Murcia, Spain Univ Fed Rio de Janeiro, Macae, Brazil Univ Tennessee, Knoxville, TN USA Inst Humboldt, Villa De Leyva, Colombia Escuela Politec Nacl, Quito, Ecuador Calif Acad Sci, San Francisco, CA 94118 USA Museum Dept Hist Nat Var, Toulon, France Nat Environm & Wildlife Soc, Angul, India Univ Kansas, Lawrence, KS 66045 USA Kyoto Univ, Kyoto, Japan Consejo Nacl Invest Cient & Tecn, Museo Argentino Ciencias Nat Bernardino Rivadavia, Buenos Aires, DF, Argentina Univ Fed Paraiba, Joao Pessoa, Paraiba, Brazil Univ Fed Parana, Curitiba, Parana, Brazil Univ Fed Rio de Janeiro, Rio De Janeiro, Brazil Nat Hist Museum Narodini Museum, Prague, Czech Republic Nat Hist Museum Zimbabwe, Bulawayo, Zimbabwe Ateneo Manila Univ, Quezon City, Philippines Pontificia Univ Javeriana, Bogota, Colombia RACINE, St Maugan, France Univ Paris 06, Sorbonne Univ Paris, ISYEB, Paris, France Ocean Univ China, Qingdao, Peoples R China Museo Nacl Hist Nat Paraguay, San Lorenzo, Paraguay Univ Carabobo, Valencia, Venezuela Natl Ctr Biol Sci, Bengaluru, India Univ Nebraska, Lincoln, NE USA CENAK Ctr Nat Kunde, Hamburg, Germany Ohio Hist Connect, Columbus, OH USA Univ Fed Amazonas, Manaus, Amazonas, Brazil Univ Malaga, Malaga, Spain Chinese Acad Sci, Qingdao, Shandong, Peoples R China Benemerita Univ Autonoma Puebla, Puebla, Mexico Natl Polytech Inst, Ctr Res & Adv Studies, Irapuato, Mexico Field Museum Nat Hist, Chicago, IL 60605 USA Univ Texas El Paso, El Paso, TX 79968 USA Univ Fed Lavras, Lavras, Brazil Nat Hist Museum, Vienna, Austria La Sierra Univ, Riverside, CA USA Univ San Francisco Quito, Quito, Ecuador Univ Hong Kong, Hong Kong, Peoples R China CUNY, New York, NY 10021 USA CAS, Inst Vertebrate Biol, Brno, Czech Republic Sorbonne Univ, MECADEV, Museum Natl Hist Nat, Paris, France Univ Estadual Paulista, Rio Claro, Brazil Zool Staatssammlung Munchen, Munich, Germany Univ Michigan, Dearborn, MI 48128 USA Smithsonian Inst, Natl Museum Nat Hist, Washington, DC USA Helmholtz Ctr Environm Res, Leipzig, Germany Santa Rosa Jr Coll, Santa Rosa, CA USA George Washington Univ, Washington, DC 20037 USA Inst Teknol Bandung, Bandung, Indonesia Earlham Coll, Richmond, IN USA Senckenberg Forschungsinst & Nat Museum, Frankfurt, Germany Univ Estadual Londrina, Londrina, Parana, Brazil Univ Koblenz Landau, Koblenz, Germany Nat Hist Museum, London, England Ditsong Natl Museum Nat Hist, Pretoria, South Africa Bombay Nat Hist Soc, Bombay, Maharashtra, India Philipps Univ Marburg, Marburg, Germany Hess Landesmuseum, Darmstadt, Germany Smithsonian Conservat Biol Inst, Washington, DC USA Univ Pannonia, Keszthely, Hungary Staatliches Museum Nat Kunde, Stuttgart, Germany UFT, Tocantins, Portugal Museum Nat Kunde, Berlin, Germany Nat Hist Riksmuseet, Stockholm, Sweden Hikarigaoka, Munakata, Japan Inst Agr & Environm Sci, Tartu, Estonia Univ Los Andes, Merida, Venezuela Bat Jungle, Monteverde, Costa Rica Texas A&M Univ, College Stn, TX USA Yale Univ, New Haven, CT USA Univ Estadual Paulista, Sao Jose Do Rio Preto, Brazil Museo Nacl Hist Nat, Montevideo, Uruguay Consejo Nacl Invest Cient & Tecn, Fdn Miguel Lillo, San Miguel De Tucuman, Argentina Roger Tory Peterson Inst Nat Hist, Jamestown, VA USA Univ Fed Reconcavo Bahia, Cruz Das Almas, Brazil South China Normal Univ, Guangzhou 510631, Guangdong, Peoples R China Museu Ciencias Tecnol PUCRS, Porto Alegre, RS, Brazil Univ Fed Tocantins, Porto Nacl, Brazil Univ Toronto, Scarborough, ON, Canada Univ Nacl Colombia, Inst Ciencias Nat, Bogota, Colombia Natl Museum Philippines, Manila, Philippines NOVA Univ Lisbon, Caparica, Portugal Royal Saskatchewan Museum, Regina, SK, Canada Deutsch Zentrum Marine Biodiversitatsforsch, Hamburg, Germany Ctr Invest Biol Noroeste, La Paz, Mexico Naturalis Biodivers Ctr, Leiden, Netherlands Univ Douala, Douala, Cameroon Vet & Farmaceut Univ Brno, Brno, Czech Republic Univ Swaziland, Kwaluseni, Eswatini Fundacao Oswaldo Cruz, Rio De Janeiro, Brazil Univ Claude Bernard, Lyon, France Museum Vertebrate Zool, Berkeley, CA USA Smithsonian Inst, Washington, DC 20560 USA Nat Hist Museum & Inst, Chiba, Japan Senckenberg Biodiversitat & Klima Forschunsgzentr, Frankfurt, Germany Marquette Univ, Milwaukee, WI 53233 USA Univ Firenze, Museo Storia Nat, Florence, Italy Univ Fed Bahia, Salvador, BA, Brazil Fed Univ ABC, Sao Bernardo, Brazil Univ Fed Goias, Goiania, Go, Brazil Univ Alaska Museum, Fairbanks, AK USA Egerton Univ, Egerton, Kenya Museo Hist Nat, Lima, Peru IKIAM Univ Reg Amazon, Tena, Ecuador Univ Hyogo, Sanda, Japan Inst Rech Dev, Paris, France Univ Sao Paulo, Piracicaba, Brazil Niedersachs Landesbetrieb Wasserwirtschaft Kusten, Hannover, Germany Univ Complutense Madrid, Madrid, Spain Consejo Nacl Invest Cient & Tecn, Ctr Nacl Patagon, Puerto Madryn, Argentina Roosevelt Univ, Coll Profess Studies, Chicago, IL 60605 USA Western Kentucky Univ, Bowling Green, KY 42101 USA Univ Naples Federico II, Naples, Italy Univ Fed Acre, Rio Branco, Acre, Brazil Univ Fed Santa Catarina, Florianopolis, SC, Brazil Inst Bio & Geociencias Noroeste Argentino, Salta, Argentina Inst Venezolano Invest Cient, Caracas, Venezuela Umweltbundesamt, Vienna, Austria Penclen, Plumelec, France CNRS MNHN UPMC, Ctr Rech Paleobiodivers & Paleoenvironm, Paris, France Staatl Museum Nat Kunde, Stuttgart, Germany Consejo Nacl Invest Cient & Tecn, Museo Argentino Ciencias Nat Bernardino Rivada, Buenos Aires, DF, Argentina Ctr Biol Gest Populat INRA, Montferrier Sur Lez, France Loyola Univ Chicago, Chicago, IL USA Pontificia Univ Catolica Rio do Sul, Porto Alegre, RS, Brazil Durban Museum Nat Sci, Durban, South Africa Univ Estado Amazonas, Manaus, Amazonas, Brazil Brigham Young Univ, Provo, UT 84602 USA Museo Hist Nat La Salle, Caracas, Venezuela Univ Vet Med Hannover, Hannover, Germany Australian Museum, Sydney, NSW, Australia Texas Tech Univ, Lubbock, TX 79409 USA Francis Marion Univ, Florence, SC USA Univ Washington, Seattle, WA 98195 USA Univ Connecticut, Groton, CT USA Fed Univ ABC, Santo Andre, SP, Brazil Univ Fed Uberlandia, Uberlandia, MG, Brazil Fed Univ Para, Belem, Para, Brazil Yale Peabody Museum, New Haven, CT USA Univ Texas Arlington, Arlington, TX 76019 USA Senckenberg Deutsch Entomol Inst, Muncheberg, Germany CSIRO, Natl Res Collect, Canberra, ACT, Australia Univ Venda, Thohoyandou, South Africa Univ Ulsan, Ulsan, South Korea Univ Estadual Sao Paulo, Botucatu, SP, Brazil Senckenberg Forsch Inst & Nat Museum, Frankfurt, Germany Ocean Univ China, Inst Marine Biodivers & Evolut, Qingdao, Shandong, Peoples R China Univ Fed Para, Altamira, Brazil Univ Estadual Paulista, Assis, Brazil UPMC, Ctr Rech Paleobiodiversite & Paleoenvironm, CNRS, MNHN, Paris, France Tech Univ Kaiserslautern, Kaiserslautern, Germany Charles Univ Prague, Dept Zool, Prague, Czech Republic Univ Nacl Expt los Llanos Occident Ezequiel Zamor, Guanare, Venezuela Long Isl Univ, Brooklyn, NY USA Univ Ryukyus, Okinawa, Japan Pontificia Univ Catolica Ecuador, Museo Zool, Escuela Ciencias Biol, Quito, Ecuador Indiana Univ Penn, Indiana, PA USA IRD, Dakar, Senegal State Museum Nat Hist Karlsruhe, Karlsruhe, Germany Univ Toulouse III Paul Sabatier, Toulouse, France Univ Ghent, Ghent, Belgium Univ Antwerp, Antwerp, Belgium Karlsruhe Inst Technol, Karlsruhe, Germany Ctr Cellular & Mol Biol, Hyderabad, India Univ Fed ABC, Santo Andre, Brazil Yale Peabody Museum Nat Hist, New Haven, CT USA Univ Innsbruck, Mondsee, Austria Bethune Cookman Univ, Daytona Beach, FL USA Natl Museum Nat & Sci, Tokyo, Japan Zool Garten Koln, Cologne, Germany Univ Estadual Paulista, Botucatu, SP, Brazil Univ Estadual Paulista, Sao Vicente, Brazil Univ Estadual Paulista, Rio Claro, Brazil Univ Estadual Paulista, Sao Jose Do Rio Preto, Brazil Univ Estadual Paulista, Assis, Brazil

Galicia Bank is a large seamount situated c. 200 km off NW Iberia with a minimum depth of 600 m. It was recently included in Natura 2000, an EU-wide network of nature protection areas. We here present the first taxonomic descriptions of cheilostome bryozoans from this bank. The specimens were collected through the Spanish project INDEMARES (during BANGAL 0811 cruise conducted in 2011) and during two previous campaigns, the French Seamount 1 in 1987 and the German Victor Hensen in 1997). Twenty-five species were found, including 12 that are new to science, while five species remain in open nomenclature. Three new cheilostome genera (Breoganipora, Galiciapora and Placidoporella) are described. A lectotype is designated for Setosella vulnerata (Busk), and Palmicellaria tenuis Calvet is transferred to the genus Porella [as Porella tenuis (Calvet) n. comb.]. Additionally, our study shows that 48-60% of the bryozoan species are endemic to Galicia Bank. The degree of endemism of the Cheilostomata is thus the highest among all orders present on this seamount.

Rhodoliths are a common producer of carbonates on modern and ancient shelves worldwide, and there is growing evidence that they thrive on volcanic insular shelves. However, little is still known on how rhodoliths cope with the demands of this particularly dynamic environment. In this study, the focus is placed on fossil rhodoliths from a Pliocene sequence at Santa Maria Island, Azores, in order to gain further insight into the life cycle (and death) of rhodoliths living within a mid-ocean active volcanic setting. These rhodoliths occur as a massive accumulation within a larger submarine volcano-sedimentary sequence that was studied from the macro- to the micro-scale in order to reconstruct the paleoenvironmental conditions under which the rhodolith accumulation was deposited and buried. All fossil rhodoliths from this setting are multi-specific and demonstrate robust growth forms with a lumpy morphology. Moreover, taphonomical analyses show the succession of several destructive events during rhodolith growth, suggesting life under a highly dynamic system prior to stabilization and burial. The rhodoliths therefore tell a story of an eventful life, with multiple transport and growth stages, owing to the environment in which they lived. Transport and deposition to their final resting place was storm-associated, as supported by the general sedimentary sequence. In particular, the sequence features an amalgamation of tempestites deposited under increasing water depths, sediment aggradation, and before burial by volcanic activity. This transgressive trend is also attested by the overall characteristics of the volcano-sedimentary succession, which exhibits the transition to subaerial environment in excess of 100 m above the rhodolith bed.

The two odontocete taxa Squalodon grateloupii and Patriocetus ehrlichii, both the type species of their respective genera, have been at the centre of a great deal of taxonomic confusion. Originally regarded to be conspecific, these two taxa have been the subject of a bewildering taxonomic debate lasting for more than a century, which recently led to the suggestion to abandon these widely used names and replace S. grateloupii with the similar, yet independently and later proposed name S. gratelupi as the type species of Squalodon. Here, we attempt to summarise the events leading to the current confused situation in the hope of resolving this issue once and for all and argue that the name Squalodon grateloupii, as originally proposed, should be reinstated.

Facies analyses of Pleistocene deposits from southern coastal Tanzania (Lindi District) document that sediments formed in a wetland evolving on a coastal terrace in the Lindi Fracture Zone foreland. The exposed succession shows a marked sedimentary change from tidal to terrestrial facies. 14C analyses on gastropod shells indicate the emergence of the Lindi coast at ∼ 44 14C ka BP. Emergence and subsequent elevation of terraces to 21 m above present-day sea level was linked to the falling eustatic sea level prior to the last glacial maximum, and to a periodic elevation due to extensional tectonic episodes in the eastern branch of the East African Rift System (EARS). Since ∼ 44 14C ka BP tectonic uplift at the coast was 80-110 m, comparable to that in the extreme uplift areas of the EARS.

Located at the interface between land and sea, marl prairies are sensitive to changes in water balance and useful recorders of climate and sea-level changes. Palustrine carbonate in marl prairies precipitates in temporary, barely flooded grasslands within microbial mats. Despite the special mode of carbonate production, descriptions of the sedimentary facies are exceptional and cursory because marl prairies are so far reported only from the recent of the Everglades (Florida, USA), where they produce an unspectacular calcite mud. We present a Pleistocene Everglades-type marl prairie from coastal Tanzania as the first fossil example. The unique preservation and high productivity (two times higher than in the Everglades) of the periphyton community in this marl prairie is due to increased calcification of coccoid and filamentous cyanobacteria. The excellent preservation allows us to characterize a marl prairie facies in great detail for the first time. Facies analyses of the sediments reveal a transition from tidal to terrestrial settings that started at ca. 44 14 C ka in response to eustatic sea-level fall and coastal tectonic uplift. The resultant drop of the groundwater table triggered the development of the marl prairie. The decline of the marl prairie was initiated at ca. 33 14 C ka due to the onset of the Last Glacial Aridity Maximum in equatorial East Africa.

Shallow marine gastropod assemblages from Chattian, Aquitanian and Burdigalian sections in the Indian Kutch Basin are described. They provide insight into the composition and biogeographic relations of the gastropod assemblages at this junction between the Western Tethys and Proto-Indo-Pacific Ocean. For the first time, an improved biostratigraphy allows a clear separation of the assemblages, especially for the hitherto undifferentiated Early Miocene faunas. Throughout the Oligocene, about one-third of the species are also frequently found in the Western Tethys, documenting a passable Tethyan Seaway for nearshore molluscs. A considerable provincialism is evident as well. The expected turnover during the Early Miocene, due to the closing of the Tethyan Seaway, is reflected in the Miocene assemblages. Surprisingly, however, the cut appears very early, i.e. already during the Aquitanian, when the West–East interrelation drops to zero despite the passage having been open during this interval. In contrast, the Burdigalian assemblages witness a minor re-appearance of Western Tethys taxa, suggesting the re-establishment of rather ineffective migration pathways prior to the final closure of the Tethyan Seaway. Cerithium bermotiense and Lyria (Indolyria) maniyaraensis are introduced as new species.

Considering the diversity and abundance of larger foraminifera examined from a wide range of Late Oligocene to Early Miocene palaeoenvironments in the Tethyan Seaway, encrusting bryozoans make extremely little use of their tests as substratum. Significant encrustations by bryozoans were exclusively found on large (o c. 6 cm), undulating tests of Lepidocyclina spp., on which, however, a remarkable 34 taxa of encrusting bryozoans were recorded. This shallow-water fauna of Chattian age was analyzed in respect of the bryozoan taxa present, colony growth type, and mode of budding, colony size, as well as onset of reproduction. Taxic and morphological similarities between the fossil assemblage and modern faunas encrusting mobile substrata indicate a long history of bryozoans as part of the interstitial habitat, while the tests of certain larger foraminifera may have played a significant role in the evolution of shallow-water bryozoans by providing substrata for encrusting species in otherwise unfavorable environments.

The cheilostome genera Herentia Gray and Therenia David and Pouyet, placed in the recently established family Escharinidae Tilbrook, were hitherto generally regarded as synonyms of Escharina Milne Edwards. Here we resurrect and define both genera, and revise their eastern Atlantic and Mediterranean species, which turn out to be species complexes. Besides presenting a re‐description of the genotype of Herentia, H. hyndmanni (Johnston) from the British Isles, new species from Madeira (Herentia andreasi n. sp.) and the Adriatic Sea (Herentia majae n. sp.) are introduced. The ancestrula of H. hyndmanni, a kenozooid with an almost completely calcified, gymnocystal frontal shield, is here documented for the first time. For Therenia it can be shown that the type species T. porosa (Smitt) from Florida differs from the eastern Atlantic and Mediterranean congeners, all of which were hitherto referred to as this species. Consequently, three new species (Therenia cryptooecium n. sp. from Ghana, Therenia peristomata n...

In this study we revise the cheilostome bryozoan genus Buffonellaria Canu & Bassler, 1927 and its Mediterranean and north-east Atlantic species, thereby addressing several existing problems. First, a lectotype for the type species, Buffonellaria divergens (Smitt, 1873) from Florida, is chosen, which proves to be distinct from the European species. Second, the two hitherto established north-east Atlantic species [Buffonellaria nebulosa (Jullien & Calvet, 1903) and Buffonellaria porcellanum Aristegui Ruiz, 1987], are redescribed, which were poorly documented until now. Third, close inspection of material, collected from Spitsbergen to tropical West Africa, using scanning electron microscopy reveals that the actual number of species, all previously referred to either B. divergens or Stephanosella biaperta (Michelin, 1848), is distinctly greater in the north-east Atlantic than has been previously acknowledged. As a result, seven new species are introduced (Buffonellaria acorensis sp. nov., Buffonellaria antoniettae sp. nov., Buffonellaria arctica sp. nov., Buffonellaria harmelini sp. nov., Buffonellaria jensi sp. nov., Buffonellaria muriella sp. nov., and Buffonellaria ritae sp. nov.), whereas two are left in open nomenclature. With the increase in number of species, the extremely broad geographical range of distribution assumed for B. divergens breaks down to numerous restricted areas. However, although most species have only been reported from a single location, B. arctica sp. nov. seems to have a fairly wide distribution in the Arctic region. © 2008 The Linnean Society of London, Zoological Journal of the Linnean Society, 2008, 152, 537–566.

Sessile barnacle assemblages, dominated by Concavus concavus (Bronn) and Balanus perforatus Bruguiere, are very abundant in the Lower Pliocene deposits of the Almeria-Nijar and Carboneras basins (southeastern Spain). They occur in shallow-coastal siliciclastic and mixed siliciclastic-carbonate sediments, forming dense concentrations in two contexts: (1) sheltered shallow-marine depressions and (2) the mouth of distributary channels feeding a delta lobe. Extensive colonization took place during periods of quiescence with a high nutrient and food supply inducing the formation of hummocks. Crowding of high morphotypes was presumably triggered by a high larval supply and recruitment rate. The barnacles are exceptionally well preserved, often as in situ clusters, many with opercula, and include a range of ontogenetic stages with some specimens preserving original colouration. Good preservation is probably due to sudden burial without further reworking.

Extensive terrestrial exchanges were initiated by the closure of the Tethyan Seaway during the Early Miocene. Proboscideans are among the most prominent African immigrants, which arrived in Eurasia about 19 Ma ago via the ‘‘Gomphotherium Landbridge’’. Several distinct waves of continental migrations, however, document that the formation of this landbridge was a multiphase process. Until the closure, a marine faunal exchange was enabled via the Mesopotamian Trough and the Zagros Basin, as reflected by contributions of Indonesian corals in the Iranian basins and by the occurrence of ‘‘western’’ gastropods in Pakistan and India. Nevertheless, the emergence of the landbridge was preceded in the marine biosphere by first biogeographic divergences on both sides of the seaway already during Oligocene times (e.g. within the tridacnines and strombids). Around the closure event, the breakdown of biogeographic relations was near-complete and the Proto-Mediterranean faunas bear little in common with those of the Indo-West Pacific Region (IWPR). Some of the discussed examples suggest that the Western Tethys Region (WTR) had acted as centre of origin and diversity during Oligocene and Early Miocene times. After the closure of the seaway, this centre had shifted to the southeast, heralding the enormous biodiversity of the modern IWPR. Some originally WTR elements managed to follow this shift and formed the Miocene stock for the modern IWPR faunas. In contrast, the marine fauna in the Mediterranean cul-de-sac suffered strong impoverishment due to the Miocene cooling, the Messinian Salinity Crisis and the late Pliocene and Pleistocene glacials – a fact which might explain the receptivity of the Mediterranean Sea for Lessepsian migrants. This synthesis tries to document the practical problem of recognising biogeographic patterns despite the heterochronous developments in different systematic groups, which, in addition, are often obscured by a stratigraphically incomplete and geographically patchy fossil record. r 2007 Elsevier GmbH. All rights reserved.

In the central Iranian Esfahan-Sirjan and Qom basins sedimentation of the Oligo-/Miocene Qom Formation took place on extensive mixed carbonate–siliciclastic ramps. During this time, both basins were positioned at the Eurasian margin of the Tethyan Seaway, which connected the western and eastern regions of the Tethys Ocean at least until the late Burdigalian. During the so-called Terminal Tethyan Event the Tethyan Seaway was then closed due to the collision of the African/Arabian and Iranian/Eurasian plates. Facies analysis of the sedimentary record of both basins indicates paleoenvironments ranging from terrestrial to open marine settings, including mangrove, restricted inner shelf lagoon, seagrass meadow, reefal, and deeper offshore environments. Recognition of eight depositional sequences and elaboration of an integrated biostratigraphic framework (calcareous nannoplankton, planktic and larger benthic foraminifers, gastropods, and pectinids) allow us to construct a basin-spanning stratigraphy. The assignment of the recognized sea-level lowstands to the Ru 3 to Bur 3 lowstands of the global sea-level curve enables a comparison with time-equivalent sections from the Zagros Basin, which was part of the African/Arabian Plate on the opposing southern margin of the Tethyan Seaway. The so calibrated sections display restrictions of the Tethyan Seaway and interruption of the south Iranian gateways between the Qom Basin and the Proto-Indopacific in relation to ongoing plate collision during the early Burdigalian.

Fossil and Recent specimens of the Mediterranean bryozoan Myriapora truncata show considerable intra- and intercolonial differences in branch diameter and zooid size. Statistically significant variability occurs within colonies, between colonies within sites, and between sampled sites, while the presence of intracolonial variability clearly shows that branch diameter is largely controlled by environmental parameters. The three structural traits measured (branch diameter, zooid size and zooid depth) do not correlate, thus indicating a disconnection between the controls on overall zooid size and branch diameter. Possible environmental parameters that may have an influence on morphology are temperature, food supply or current energy. Whereas current energy has an effect on the colony branching pattern (branch spacing), there are indications that temperature may be the main, but not the only, parameter controlling zooid size, and it is suggested that food supply largely determines the branch diameter in M. truncata. However, the identification of the decisive factors and quantification of the relationships between environmental and morphological change is beyond the scope of this study. The results nevertheless show that, if the control factors of morphological variability can be ascertained in Recent M. truncata, this species may prove to be an indicator of environmental conditions and their change at different spatial and temporal scales in Cenozoic to Recent Mediterranean habitats.

Eight NE Atlantic and Mediterranean species, which were originally assigned to the genus Schizoporella (Family Schizoporellidae) when introduced, are redescribed and stabilized by typification. Seven of these species are transferred to the bitectiporid genus Schizomavella: S. fischeri, S. glebula, S. neptuni, S. obsoleta, S. richardi, S. triaviculata, and S. triaviculata var. paucimandibulata, which is here raised to species rank. The eighth species, Schizoporella fayalensis, is transferred to the lanceoporid genus Stephanotheca. Schizomavella obsoleta and S. glebula are considered junior subjective synonyms of S. fischeri and S. richardi, respectively. Two new species are described: Schizomavella rectangularis n. sp. from the Strait of Gibraltar, and Schizomavella phterocopa n. sp. from the Great Meteor Bank. A new subgenus, Calvetomavella n. subgen. is established as a result of a phylogenetic analysis based on morphological characters; it includes S. neptuni, S. triaviculata, S. paucimandibulata and S. phterocopa n. sp., together with Schizomavella discoidea and Schizomavella noronhai. The rest of the species remain in the nominotypical subgenus Schizomavella. The work by ORG and JS was partially supported by the project “Fauna Ibérica: Briozoos II (Familia Cribrilinidae – Familia Watersiporidae)” (CGL2010-22267-C07-02), co-financed by the Ministerio de Economía y Competitividad (Spanish Government) and FEDER. BB acknowledges support from the SYNTHESYS Project (http://www.synthesys.info/), which is financed by the European Community Research Infrastructure Action under the FP7 “Capacities” Program, and which allowed studying type and comparative material at the MNHN (FR-TAF-1902) and the NHMUK (GB-TAF-3347). JS thanks the Austrian Science Fund (FWF, Lise Meitner Program, grant M1444-B25) for financial support (https://www.fwf.ac.at/). SI