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NARROW
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all geography including DSDP/ODP Sites and Legs
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Africa
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U–Pb zircon age and mineralogy of the St Georgen halloysite tuff shed light on the timing of the middle Badenian (mid-Langhian) transgression, ash dispersal and palaeoenvironmental conditions in the southern Vienna Basin, Austria
ABSTRACT The nineteenth century was the dawn of scientific and systematic paleontology. The foundation of Natural History Museums—built as microcosmic “Books of Nature”—not only contributed to the establishment of this new discipline but also to its visual dissemination. This paper will take the metaphor of the “book” as a starting point for an examination of the paleontological exhibition at the Natural History Museum in Vienna. In keeping with “Natural Theology,” the earliest natural science museums in Britain were designed as expressions of the medieval idea of the “Holy Book of Nature.” Contrary to this, the Natural History Museum Vienna, opened in 1889, wanted to be a nonreligious museum of evolution. Nevertheless, the idea of the “book” was also influential for its design. According to the architects and the first director, it should be a modern “walk-in textbook” instructive for everyone. The most prominent exhibition hall in the museum is dedicated to paleontology. The hall’s decorative scheme forms a unique “Paleo-Gesamtkunstwerk” (Gesamtkunstwerk: total piece of art). The use of grotesque and mythological elements is a particularly striking feature of the hall’s decoration and raises the question of how this relates to the museum’s claim to be a hard-core science institution. As it was paleontology’s task to demystify the monsters and riddles of Earth history systematically, it seems odd that the decorative program connected explicitly to this world. This chapter sheds light on the cultural traditions that led to the creation of this ambiguous program that oscillates between science and imagination. Looking at the results of the research on the nature of the earth, one looks into a book that contains the oldest history we humans know. With amazement, we see the wonders of the first epochs of the earth arising before our mind’s eyes, and what until recently have been incomprehensible hieroglyphs is now almost completely clear to us. How many fables may have been created by the sudden appearance of prehistoric structures in the form of animals and plants? No fairy tales, no fantasies, tangible reality now stands before us and yet no less wonderful, even more wonderful, and this miracle has been achieved by science, the restless seeker. —J. Hoffmann (undated, ca. 1885, p. 1; translation from German)
History and importance of the geoscience collections at the Natural History Museum Vienna
ABSTRACT The Natural History Museum Vienna is one of the most important museums of natural history in the world. Its collections date back to the year 1750, when the Emperor Franz Stephan of Lorraine (Franz I. Stephan) purchased (from Italy) what was then the largest and most famous collection of natural history specimens. The meteorite collection of the Natural History Museum in Vienna, Austria, has the longest history of all comparable collections in the world. In the second half of the eighteenth century, soon after the foundation of the Imperial Natural History Cabinet in 1750, the Viennese curators began to collect meteorites. Although the first curators neither believed in the extraterrestrial origin nor accepted—in several cases—the written and witnessed histories of these allegedly “heavenly” stone and iron masses, they preserved them in the Natural History collection. Among the first acquisitions were the historical important meteorites Hraschina (Agram), Tabor, Krasnojarsk (Pallas iron), and Eichstädt. These and other well-documented specimens from the Vienna collection were, for example, used by E.F.F. Chladni for his seminal treatises of 1794 and 1819, respectively. The central figure in the early history of the collection is Carl von Schreibers (1775–1852). After the fall of the Stannern meteorite in 1808, he availed himself of every opportunity to acquire meteorite specimens. His continued interest in meteorites laid the foundation for the Vienna collection to be of the historical and scientific importance it is today. Due to the efforts of Schreibers, who also is regarded as founder of meteoritic science in Vienna, and his successors, the Vienna collection became the largest and most extensive in the course of the nineteenth century. In terms of the geological and paleontological collections, early expeditions and collecting campaigns were mainly targeting exotic animals and plants, while paleontological objects were welcome but subordinate. It was only in the early nineteenth century that the paleontological collections were—literally and figuratively speaking—systematically enlarged. Internationalization and diversification became the focus of the collection strategy. The paleontology collections at the Vienna museum also became important in the Darwinian view of evolution.
Taxonomic and numerical sufficiency in depth- and salinity-controlled marine paleocommunities
High-resolution 3D surface modeling of a fossil oyster reef
Long-term ecosystem stability in an Early Miocene estuary
Mendicodinium mataschenensis : a new endemic dinoflagellate cyst from the Late Miocene (Tortonian) of Lake Pannon (Austria)
Abstract Changes in molluscan diversity across the 3rd order sequence boundary from the Lower to the Middle Miocene of the Paratethys were evaluated in the context of environmental bias. Taken at face value, quantitative data from nearshore and sublittoral shell beds suggest a transition from low-diversity Karpatian (Upper Burdigalian) to highly diverse Badenian (Langhian and Lower Serravallian) assemblages, but environmental affiliation of samples reveals a strong facies shift across the sequence boundary. Ordination methods show that benthic assemblages of the two stages, including 4 biozones and four 3rd order depositional sequences over less than four million years, are developed along the same depth-related environmental gradient. Almost all samples are from highstand systems tracts, but Karpatian faunas are mostly from nearshore settings, and Badenian faunas are strongly dominated by sublittoral assemblages. This study emphasizes the importance of highly resolved stratigraphic and palaeoenvironmental frameworks for deciphering palaeodiversity patterns at regional scales and highlights the effort required to reach the asymptote of the collector's curve. Abundance data facilitate the recognition of ecological changes in regional biota and it is suggested that in second and higher order sequences the facies covered within systems tracts will drive observed diversity patterns.
A FOSSIL EVERGLADES-TYPE MARL PRAIRIE AND ITS PALEOENVIRONMENTAL SIGNIFICANCE
Oligocene–Miocene basin evolution in SE Anatolia, Turkey: Constraints on the closure of the eastern Tethys gateway
Abstract The Oligocene–Miocene was a time characterized by major climate changes as well as changing plate configurations. The Middle Miocene Climate Transition (17 to 11 Ma) may even have been triggered by a plate tectonic event: the closure of the eastern Tethys gateway, the marine connection between the Mediterranean and Indian Ocean. To address this idea, we focus on the evolution of Oligocene and Miocene foreland basins in the southernmost part of Turkey, the most likely candidates to have formed this gateway. In addition, we take the geodynamic evolution of the Arabian–Eurasian collision into account. The Muş and Elazığ basins, located to the north of the Bitlis–Zagros suture zone, were most likely connected during the Oligocene. The deepening of both basins is biostratigraphically dated by us to occur during the Rupelian (Early Oligocene). Deep marine conditions (between 350 and 750 m) prevailed until the Chattian (Late Oligocene), when the basins shoaled rapidly to subtidal/intertidal environment in tropical to subtropical conditions, as indicated by the macrofossil assemblages. We conclude that the emergence of this basin during the Chattian severely restricted the marine connection between an eastern (Indian Ocean) and western (Mediterranean) marine domain. If a connection persisted it was likely located south of the Bitlis–Zagros suture zone. The Kahramanmaraş basin, located on the northern Arabian promontory south of the Bitlis–Zagros suture zone, was a foreland basin during the Middle and Late Miocene, possibly linked to the Hatay basin to the west and the Lice basin to the east. Our data indicates that this foreland basin experienced shallow marine conditions during the Langhian, followed by a rapid deepening during Langhian/Serravallian and prevailing deep marine conditions (between 350 and 750 m) until the early Tortonian. We have dated the youngest sediments underneath a subduction-related thrust at c . 11 Ma and suggest that this corresponds to the end of underthrusting in the Kahramanmaraş region, i.e. the end of subduction of Arabia. This age coincides in time with the onset of eastern Anatolian volcanism, uplift of the East Anatolian Accretionary Complex, and the onset of the North and East Anatolian Fault Zones accommodating westward escape tectonics of Anatolia. After c . 11 Ma, the foreland basin south of the Bitlis formed not (or no longer) a deep marine connection along the northern margin of Arabia between the Mediterranean Sea and the Indian Ocean. We finally conclude that a causal link between gateway closure and global climate change to a cooler mode, recorded in the Mi3b event (δ 18 O increase) dated at 13.82 Ma, cannot be supported.
Palaeogene and Neogene
Abstract Over the last 65 Ma, our world assumed its modern shape. This timespan is divided into the Palaeogene Period, lasting from 65 to 23 Ma and the Neogene, which extends up to the present day (see Gradstein & Ogg (2004) and Gregory et al. (2005) for discussion about the Quaternary). Throughout the Cenozoic Era, Africa was moving towards Eurasia in a northward direction and with a counterclockwise rotation. Numerous microplates in the Mediterranean area were compressed, gradually fusing, and Eurasia underwent a shift from a marine archipelago to continental environments, related to the rising Alpine mountain chains ( Figs 17.1 & 17.2 ). Around the Eocene-Oligocene boundary, Africa's movement and subduction beneath the European plate led to the final disintegration of the ancient Tethys Ocean. The Indo-Pacific Ocean came into existence in the east while various relict marine basins remained in the west. In addition to the emerging early Mediterranean Sea, another relict of the closure of the Tethys was the vast Eurasian Paratethys Sea. The Oligocene and Miocene deposits of Central Europe are largely related to the North Sea in the north, the Mediterranean Sea in the south and the intermediate Paratethys Sea and its late Miocene to Pliocene successor Lake Pannon. At its maximum extent, the Paratethys extended from the Rhône Basin in France towards Inner Asia. Subsequently, it was partitioned into a smaller western part consisting of the Western and the Central Paratethys and the larger Eastern Paratethys. The Western Paratethys comprises the Rhône Basin and the Alpine Foreland Basin of Switzerland, Bavaria and Austria. The Central Paratethys extends from the Vienna Basin in the west to the Carpathian Foreland in the east where it abuts the area of the Eastern Paratethys. Eurasian ecosystems and landscapes were impacted by a complex pattern of changing seaways and land bridges between the Paratethys, the North Sea and the Mediterranean as well as the western Indo-Pacific (e.g. Rögl 1998 ; Popov et al. 2004 ). This geodynamically controlled biogeographic differentiation necessitates the establishment of different chronostratigraphic/geochronologic scales. The geodynamic changes in landscapes and environments were further amplified by drastic climate changes during the Cenozoic. The warm Cretaceous climate continued into the early Palaeogene with a distinct optimum near the Palaeocene-Eocene boundary (Palaeocene-Eocene Thermal Maximum) and the Early Eocene (Early Eocene Climate Optimum). A gradual decrease in temperature during the later Eocene culminated in the formation of the first icesheets in Antarctica around the Eocene-Oligocene boundary ( Zachos et al. 2001 ; Prothero et al. 2003 ). A renewed warming trend that began during the Late Oligocene continued into the Middle Miocene with a climax at the Mid-Miocene Climatic Optimum. The turning point at around 14.2 Ma led to the onset of the Middle Miocene Climate Transition indicated by the cooling of surface waters and the expansion of the East Antarctic icesheet ( Shevenell et al. 2004 ). A final trend reversal during the Early Pliocene is reflected by a gentle warming until 3.2 Ma ( Zachos et al. 2001 ) when the onset of permanent Arctic glaciation heralded the Pleistocene ice ages (see Litt et al. 2008 ). The Cenozoic history of Central Europe is chronicled in a dense pattern of Palaeogene and Neogene basins. In addition to the more stable North Sea Basin, the majority of these basins were strongly influenced by the Alpine compressive tectonics which caused a general uplift of Europe during the Cenozoic (see Froitzheim et al. 2008 ; Reicherter et al. 2008 ). The marginal position of the seas covering the area and the considerable synsedimentary geodynamic control resulted in incomplete stratigraphic sequences with frequent unconformities, erosional surfaces and depositional gaps. This chapter deals with the Paleogene and Neogene (“Tertiary”) geological development of Central Europe and its adjacent areas. It is structured according to the main geological regions relevant for the Cenozoic: (1) The European Plate; (2) the Alps and Alpine Foredeep; (3) the Carpathians, their foredeep and the Pannonian Basins System; and (4) the Southern Alps and Dinarides. Each subchapter is arranged from west to east, and north to south.