Depositional sequences originating in semi-enclosed basins with endemic biota, partly or completely isolated from the open ocean, frequently do not allow biostratigraphic correlations with the standard geological time scale (GTS). The Miocene stages of the Central Paratethys represent regional chronostratigraphic units that were defined in type sections mostly on the basis of biostratigraphic criteria. The lack of accurate dating makes correlation within and between basins of this area and at global scales difficult. Although new geochronological estimates increasingly constrain the age of stage boundaries in the Paratethys, such estimates can be misleading if they do not account for diachronous boundaries between lithostratigraphic formations and for forward smearing of first appearances of index species (Signor-Lipps effect), and if they are extrapolated to whole basins. Here, we argue that (1) geochronological estimates of stage boundaries need to be based on sections with high completeness and high sediment accumulation rates, and (2) that the boundaries should preferentially correspond to conditions with sufficient marine connectivity between the Paratethys and the open ocean. The differences between the timing of origination of a given species in the source area and timing of its immigration to the Paratethys basins should be minimized during such intervals. Here, we draw attention to the definition of the Central Paratethys regional time scale, its modifications, and its present-day validity. We suggest that the regional time scale should be adjusted so that stage boundaries reflect local and regional geodynamic processes as well as the opening and closing of marine gateways. The role of eustatic sea level changes and geodynamic processes in determining the gateway formation needs to be rigorously evaluated with geochronological data and spatially-explicit biostratigraphic data so that their effects can be disentangled.

The Danube Basin is situated between the Eastern Alps, Central Western Carpathians and Transdanubian Range. The northwestern embayment of the basin is represented by the Blatné depression with deposits ranked into the Langhian-Serravallian (Badenian, Sarmatian) and Tortonian-Pliocene (Pannonian-Pliocene). They are documented by the NN4, NN5 and NN6 calcareous nannoplankton zones; the CPN7 and CPN8 foraminiferal zones (equivalent to N9, N10 and N11 of global foraminiferal zones and to the MMi4a, MMi5 and MMi6 of Mediterranean foraminiferal zones) and by the mammalian zones MN9, MN10, MN13 and by Be isotopes. Sedimentation in basin began with basal conglomerates formed by local fan-deltas short before and during the initial rifting phase. Early Langhian conglomerates are composed of Mesozoic rocks derived from the sedimentary cover and nappe units of the Eastern Alps and Central Western Carpathians. The content of crystalline rocks increases upwards, which documents a continual denudation of the emerged source area (at present forming the pre-Neogene basement of the Danube Basin). The middle to late Langhian synrift stage of the basin development was accompanied by volcanic activity. Gravity transport of sediment took place on the basin slopes formed by pronounced fault activity. The basin floor reached the deep neritic zone. During the early Serravallian shelfal offshore sedimentary conditions prevailed and gradually passed into the late Serravallian regressive coastal plains with normal to brackish salinity. Tortonian transgressive sedimentation on the muddy shelves of Lake Pannon followed and was subsequently replaced by a relatively short-living deltaic environment and later by deposition on an alluvial plain. Final Pliocene to Quaternary fluvial sedimentation is characterized by gravel and sand beds. •

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The Danube Basin is situated between the Eastern Alps, Western Carpathians and Transdanubian mountain ranges and represents a classic petroleum prospection site. The basin fill is known from many 2D reflection seismic lines and deep wells with measured e-logs which provided a good opportunity for theories about its evolution. New analyses of deep wells situated in the Danube Basin northeastern margin allowed us to refine stratigraphy and to interpret various depositional systems. This also allowed us to outline changes in provenance of sediment during the Cenozoic. The performed interpretation of the Palaeogene and Neogene depositional systems also confirmed the Oligocene-Early Miocene exhumation of the basin pre-Neogene basement. Opening and development of the Middle to Late Miocene basin depocentres above the boundary between the Western Carpathians and Northern Pannonian domain was recognized. Our analysis contributed to a better understanding of the Hurbanovo-Di€ osjen} o fault which acts as an inherited weakness zone along the boundary of two crustal fragments with different provenance. We document various basin types stacked one on another (retro-arc, back-arc and extensional hinterland basin). The analysis of sediment sources reveals intricate geodynamic processes during the Eastern Alpine-Western Carpathian orogenic system collision with European platform (formation of ALCAPA microplate) and its successive tectonics escape during the Pannonian Basin System origination.

Alpheid snapping shrimps (Decapoda: Caridea: Alpheidae) constitute one of the model groups for inferences aimed at understanding the evolution of complex structural, behavioural, and ecological traits among benthic marine invertebrates. Despite being a super-diverse taxon with a broad geographical distribution, the alpheid fossil record is still poorly known. However, data presented herein show that the strongly calcified fingertips of alpheid snapping claws are not uncommon in the fossil record and should be considered a novel type of mesofossil. The Cenozoic remains analysed here represent a compelling structural match with extant species of Alpheus. Based on the presence of several distinct snapping claw-fingertip morphotypes, the major radiation of Alpheus lineages is estimated to have occurred as early as 18 mya. In addition, the oldest fossil record of alpheids in general can now be confirmed for the Late Oligocene (27–28 mya), thus providing a novel minimum age for the entire group as well as the first reliable calibration point for deep phylogenetic inferences.