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Book Chapter

Palaeogene and Neogene

By
Michael W. Rasser
Michael W. Rasser
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Mathias Harzhauser
Mathias Harzhauser
(co-ordinators)
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Olga Y. Anistratenko
Olga Y. Anistratenko
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Vitaliy V. Anistratenko
Vitaliy V. Anistratenko
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Davide Bassi
Davide Bassi
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Mirko Belak
Mirko Belak
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Jean-Pierre Berger
Jean-Pierre Berger
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Gianluca Bianchini
Gianluca Bianchini
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Safet Čičić
Safet Čičić
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Vlasta Ćosović
Vlasta Ćosović
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Nela Doláková
Nela Doláková
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Katica Drobne
Katica Drobne
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Sorin Filipescu
Sorin Filipescu
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Karl Gürs
Karl Gürs
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Šárka Hladilová
Šárka Hladilová
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Hazim Hrvatović
Hazim Hrvatović
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Bogomir Jelen
Bogomir Jelen
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Jacek Robert Kasiński
Jacek Robert Kasiński
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Michal Kováč
Michal Kováč
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Polona Kralj
Polona Kralj
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Tihomir Marjanac
Tihomir Marjanac
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Emö Márton
Emö Márton
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Paolo Mietto
Paolo Mietto
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Alan Moro
Alan Moro
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András Nagymarosy
András Nagymarosy
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James H. Nebelsick
James H. Nebelsick
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Slavomír Nehyba
Slavomír Nehyba
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Bojan Ogorelec
Bojan Ogorelec
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Nestor Oszczypko
Nestor Oszczypko
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Davor Pavelić
Davor Pavelić
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Rajko Pavlovec
Rajko Pavlovec
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Jernej Pavšič
Jernej Pavšič
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Pavla Petrová
Pavla Petrová
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Marcin Piwocki
Marcin Piwocki
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Marijan Poljak
Marijan Poljak
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Nevio Pugliese
Nevio Pugliese
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Rejhana Redžepović
Rejhana Redžepović
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Helena Rifelj
Helena Rifelj
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Reinhard Roetzel
Reinhard Roetzel
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Dragomir Skaberne
Dragomir Skaberne
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L’ubomír Sliva
L’ubomír Sliva
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Gerda Standke
Gerda Standke
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Giorgio Tunis
Giorgio Tunis
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Dionýz Vass
Dionýz Vass
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Michael Wagreich
Michael Wagreich
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Frank Wesselingh
Frank Wesselingh
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Published:
January 01, 2008

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.

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Contents

Geological Society, London, Geology of Series

The Geology of Central Europe Volume 2: Mesozoic and Cenozoic

Geological Society of London
Volume
2
ISBN electronic:
9781862393899
Publication date:
January 01, 2008

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