The 2013 European Seismic Hazard Model (ESHM13) results from a community-based probabilistic seismic hazard assessment supported by the EU-FP7 project "Seismic Hazard Harmonization in Europe" (SHARE, 2009(SHARE, -2013. The ESHM13 is a consistent seismic hazard model for Europe and Turkey which overcomes the limitation of national borders and includes a through quantification of the uncertainties. It is the first completed regional effort contributing to the "Global Earthquake Model" initiative. It might serve as a reference model for various applications, from earthquake preparedness to earthquake risk mitigation strategies, including the update of the European seismic regulations for building design (Eurocode 8), and thus it is useful for future safety assessment and improvement of private and public buildings. Although its results constitute a reference for Europe, they do not replace the existing national design regulations that are in place for seismic design and construction of buildings. The ESHM13 represents a significant improvement compared to previous efforts as it is based on (1) the compilation of updated and harmonised versions of the databases required for probabilistic seismic hazard assessment, (2) the adoption of standard procedures and robust methods, especially for expert elicitation and consensus building among hundreds of European experts, (3) the multi-disciplinary input from all branches of earthquake science and engineering, (4) the direct involvement of the CEN/TC250/SC8 committee in defining output specifications relevant for Eurocode 8 and (5)

Local and regional earthquake locations provide seismic evidence that large shield earthquakes have occurred in northern Fennoscandia. These paleoearthquakes, with fault lengths of up to 160 kilometers and average displacements of up to 15 meters, were triggered by nonisostatic compressive stresses caused by the removal of the ice at the end of the last deglaciation. The Fennoscandian faults were probably formed by single events that ruptured through most of the crust. The largest event, moment magnitude M, -8.2, was larger than other known stable continent earthquakes outside failed rifts or extended crust.Large-scale surface lineaments (up to 160 km) in northern Fennoscandia (1) have been interpreted as postglacial fault scarps (PGFs) formed by thrust earthquakes shortly after the local deglaciation 9000 years aeo. The formation of these faults mav have " been due to stresses caused hy early postglacia1 rebound. and if so. the faults can be used to estilnate the rate of early postglacial rebound and to infer lithospheric dynamics (2). Offsets of Quaternary sediments and the clustering of paleolandslides and liquefaction phenomena (3) along the scarps indicate that these faults mark Quaternary earthquakes. Such evidence would not be observable if the PGFs formed before deglaciation (3) and restricts the oldest age for the displacements on the PGFs to the time of local deelaciation. 8500 to 9000 vears " ago. The younger age limit is set by undis---turbed postglacial sediments, including littoral sediments, that overlie parts of the Lansjarv PGF, glacier meltwater channels that cut through the Parvie scarp, and 14C dates of peat in a landslide close to Lansjarv of 8200 ? 200 years ago (3). The shallow littoral sediments have depths of (10 m and were formed within 200 years after deglaciation, after which, on the basis of the rate of landrise ( 4 ) , they were raised above sea level. In view of the length of the faults in the stable shield of northern Fennoscandia, the causative earthquakes would have had magnit~~des of -8. Intraplate earthquakes of such magnitude have elsewhere only been located in failed rifts or extended crustal regions (5). I analyzed seismic data to determine whether the observed lineaments are due to earthquakes, and to estilnate the likely magnitudes, fault dimensions, and numher of events that produced the PGFs. The existence of an active fault zone is

S U M M A R YThe Cyprian Arc forms the plate boundary between the Anatolian plate in the north and the Nubian and Sinai plates in the south. We examine the tectonic setting and seismic activity along the arc in light of new geodetic studies indicating relative NE-SW plate motions across the arc. The first-order tectonic variations are determined by the arc's geometry. The eastern arc, oriented subparallel to relative motion, is dominated by transcurrent tectonism. The western arc is oriented almost normal to relative plate motion and is subjected to convergent processes. Variations in the level and depth of seismic activity along the western arc suggest that the northwestern section of the arc represents a subduction boundary, whereas the southeastern section represents a collision boundary. The two tectonic domains of the western arc are separated by a NE-SW trending tear fault, which produces large earthquakes, such as the M W = 6.8, 1996 Paphos earthquake. We compare the geometrically similar Cyprian and Hellenic Arcs and find significant differences in the rate, direction and type of convergence across the two arcs. The Hellenic Arc is subjected mainly to subduction, whereas the shorter Cyprian Arc is subjected to subduction, collision and transcurrent tectonic processes.

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S U M M A R YFocal mechanisms from 18 major Swedish earthquakes, M,(UPP) 2 3, reveal that:(1) several of the studied earthquakes have focal mechanisms with significant extensional stresses which fit well t o the idea of postglacial rebound as a.n important stress generator, ( 2 ) in areas like south-hestern Sweden, the north-westerly trending compressional axes indicate that ridge push from the North Atlantic Ridge is also a considerable stress contributor; (3) some local tectonic features, like the Skalderviken depression in Kattegat, are momentous for seismotectonic interpretations. In addition to first P polarities, full waveform modelling for frequencies up to 3Hz and epicentral distances u p to 225 km provides rather robust focalmechanism determinations. Focal depths of seven events, ranging from 11 t o 37 km, are well resolved within a few km by waveform modelling.