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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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Atlantic Ocean
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North Atlantic
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Blake Plateau
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Blake Nose (1)
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Europe
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Alps
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Central Alps (1)
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Prealps (1)
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Southern Europe
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Italy
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Lombardy Italy
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Valtellina (1)
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Po Valley (1)
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Venetia (1)
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Veneto Italy
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Belluno Italy (1)
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Possagno Italy (1)
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Verona Italy (1)
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Vicenza Italy (2)
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South America
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Argentina
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Neuquen Argentina (1)
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Neuquen Basin (1)
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fossils
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Invertebrata
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Mollusca
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Gastropoda (1)
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Protista
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Foraminifera
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Rotaliina
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Rotaliacea
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Nummulitidae
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Nummulites (1)
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microfossils (2)
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geologic age
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Cenozoic
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Tertiary
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Paleogene
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Eocene
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upper Eocene
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Priabonian (1)
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Mesozoic
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Jurassic
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Lower Jurassic
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Pliensbachian (1)
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Primary terms
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Atlantic Ocean
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North Atlantic
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Blake Plateau
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Blake Nose (1)
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biogeography (1)
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Cenozoic
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Tertiary
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Paleogene
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Eocene
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upper Eocene
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Priabonian (1)
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continental drift (1)
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earthquakes (1)
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Europe
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Alps
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Central Alps (1)
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Prealps (1)
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Southern Europe
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Italy
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Lombardy Italy
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Valtellina (1)
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Po Valley (1)
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Venetia (1)
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Veneto Italy
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Belluno Italy (1)
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Possagno Italy (1)
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Verona Italy (1)
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Vicenza Italy (2)
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faults (1)
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Invertebrata
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Mollusca
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Gastropoda (1)
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Protista
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Foraminifera
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Rotaliina
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Rotaliacea
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Nummulitidae
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Nummulites (1)
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Mesozoic
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Jurassic
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Lower Jurassic
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Pliensbachian (1)
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Ocean Drilling Program
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Leg 171B
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ODP Site 1051 (1)
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paleoecology (1)
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paleogeography (1)
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plate tectonics (1)
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sedimentary rocks (1)
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sedimentation (2)
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South America
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Argentina
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Neuquen Argentina (1)
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Neuquen Basin (1)
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stratigraphy (1)
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tectonics (1)
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tectonophysics (1)
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rock formations
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Scaglia Formation (1)
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sedimentary rocks
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sedimentary rocks (1)
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Monte Grappa Massif
The Priabonian platform of the Venetian Prealps in the «flessura pedemontana» (southern Altopiano di Asiago and southern Monte Grappa Massif, Northern Italy): a case history of confused lithostratigraphic nomenclature
Reappraising the 25 February 1695 Asolano Earthquake
A bstract In the central-eastern sector of the Southern Alps, the Upper Cretaceous is represented mainly by basinal deposits of the ScagliaRossa Formation. Shallow-water carbonates of the Friuli Platform crop out towards the northeast. Since the eighteenth century rudist bivalves in this area have been reported embedded in Scaglia Rossa basinal rocks. These rocks weredeposited tens of kilometers away from any known Late Cretaceous carbonate platform, which is normally considered the typical sourceof these mollusks. Paleontologic and sedimentologic studies carried out in the Lessini Mountains rule out the possibility that these rudists, represented by radiolitids, could have been transported by gravitational redeposition; instead it is assumed that they lived in situ elevatedabove the substrate or lying on one side with the commissure directed upwards. Evidence supporting this is (1) the great distance fromany carbonate platform source, (2) the lack of resedimentation features, and (3) the absence of other shallow-water organisms. To explain the occurrence of these radiolitids in such an anomalous setting, it has been hypothesized that the physiography and paleobathymetry of the studied area during late Turonian to Coniacian (Late Cretaceous) was characterized by a paleoenvironment whichfavored the existence of these rudist taxa in the lower photic zone of a basinal high.
Subsidence and Sedimentation on Jurassic Passive Continental Margin, Southern Alps, Italy
REASSESSMENT OF THE EARLY–MIDDLE EOCENE PLANKTIC FORAMINIFERAL BIOMAGNETOCHRONOLOGY: NEW EVIDENCE FROM THE TETHYAN POSSAGNO SECTION (NE ITALY) AND WESTERN NORTH ATLANTIC OCEAN ODP SITE 1051
Early Jurassic Trochotomidae (Vetigastropoda, Pleurotomarioidea) from the Neuquén Basin, Argentina
Seismotectonic characteristics of the Italian central Alps and implications for the seismic hazard
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.
Abstract Jurassic reef patterns reflect the fulminant global and regional changes initiated by the breakup of northern Pangea. The pattern of reef distribution across the Jurassic reflects a complex mix of (1) different and changing tectonic styles along the continental margins and adjacent shelf seas; (2) sea-level rise and its modulating influence on extrinsic sedimentation; (3) oceanographic and climatic reorganizations related to general sea-level rise and the new plate-tectonic configurations; and (4) evolutionary changes in the ecological demands and abilities of reef biota, which, in part, appear to have been triggered by the extrinsic changes during the breakup of northern Pangea. Rifting and onset of drift in the central Atlantic as well as in the western Tethys resulted in a distinct sea-level rise, which transformed Jurassic shelf seas along the northern Tethys margin from dominantly siliciclastic to dominantly carbonate settings. The opening of the ocean passageway from the Tethys to the Caribbean and Pacific completely reorganized global oceanic circulation patterns. During the Late Jurassic, shelf seas were considerably deep, increasing the areas of settings suitable for development of siliceous sponge mounds on the northern Tethys margin. In contrast, many parts of the southern Tethys margin underwent strong morphological changes due to rift tectonics within the Triassic carbonate platforms, which resulted in a completely different pattern in Jurassic reef distribution relative to the northern Tethys. After the end-Triassic extinction event, Jurassic reefs recuperated gradually during the Early Jurassic, with a first major reef domaindeveloping in Morocco Their temporal distribution through the Middle Jurassic was more balanced, but reefs occurred in scattered domains often distant from each other (e.g., Portugal, France, Madagascar, Iran). Late Jurassic reefs expanded rapidly in the course of the ongoing sea-level rise and the oceanographic reorganization, resulting in mostly interconnected domains. A pattern of waxing and waning of reef abundanceand spatial reef distribution through time is superimposed on this trend. It is again, at least to a large extent, correctable with sea-level fluctuations of greater magnitude. Jurassic reef growth had pea ks during the transgressivc episodes of the Sinemurian-Pliensbachian, Bajocian-Bathonian, and Oxfordian-Kimmeridgian, with superimposed higher-frequency peaks. The Jurassic represents the peak not only of development of Mesozoic coral reefs but equally of development of sponge mounds. Sponge mounds represent siliceous sponge-microbolite mud mounds, which expanded enormously during the Oxfordian along the European part of the northern Tethys. A peculiar type of bivalve reefs, the Lilhiothis reefs, were widespread particularly during the Sinemurian and Pliensbachian, and they might have partially filled a potential reef-growth habitat not occupied by corals, owing to the reduced availability of coral taxa at that time. Bivalve reefs, in particular oyster reefs, also occurred scattered in Middle and Latejurassic times, mostly representing marginal marine environments. Sea-level rise and tectonic opening of new seaways hod a pronounced influence on climate and marine circulation patterns, which were the principal factors in Jurassic reef development. Particularly in the Late Jurassic, coral and stromatoporoid reefs occurred in high paleolatitudinal settings (e.g., Argentina, Patagonia, japan) evidencing strong climatic equilibration of marine and coastal areas, despite the fact that strong seasonal contrasts should have prevailed in the Gondwana interiors. There are only a few records of low-latitude reef sites, despite the availability of carbonate platforms, which might reflect overheated waters in this area. Humidity was probably higher than previously thought. Siliciclastic influx was partially high during the Kimmeridgian, owing to fluvial runoff and renewed tectonic activity, and reduced the number of reef sites and domains considerably, despite ongoing global sea-level rise. Jurassic, chiefly Upper Jurassic, reefs not only grew within the expanding carbonate settings but also thrived in temgeneously influenced environments. This is particularly obvious in the North Atlantic rift basins, such as the Lusitanian Basin of west-central Portugal, but itisalsodiscernibleinmany other Jurassic reef domains. Occurrence of cora! associations in fine siliciclastics, ratios of skeletal low-density vs. high-density banding, morphological adaptations towards sedimentation, high proportions of bioerosion, and overlap of many coral domains with proposed upwelling areas suggests that there was a considerable stock of Jurassic zooxanthellate corals with a distinct heterotrophic proportion of feeding, thus living in mesotrophic settings. In contrast, reefs on the isolated, oceanic shallow-water Apulia-Adria platforms differ considerably, being dominated by stromatoporoids, chaetetids, and corals. We propose the theory that these oceanic faunas might have already had a more advanced photosymbiotic relationship than the other forms and thus could thrive in presumably strongly oligo trophic settings. Such associations, which might have occurred similarly on oceanic platforms in the Pacific, are thought to have been the stock for Cenozoic development of coral reefs into superoligotrophic settings, whereas the more nutrient-tolerant reefs a long the continental margins vanished in the course of latest Jurassic and Berriasian sea-level drop. Sediment-stressed, nutrient-rich shallow-water settings might then have been reconquered by rudist bivalves in the course of the Cretaceous. Jurassic reefs not only constitute widespread and important hydrocarbon reservoir rocks; their manifold characteristicsand related dependence on basin tectonics, sea-level change, and ecological parameters makes them valuable basin-analysis tools for potential hydrocarbon plays.