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The Sibari Plain is located close to the boundary between the Calabrian Arc and the Southern Apennines. During the Holocene, the plain was characterized by the Crati delta building and by the re-activation of the transverse Sybaris Fault Zone (SFZ), a northward dip fault interpreted as an oblique normal-dextral fault zone, 45°N-55°N striking, recognized by archaeoseismic data recorded in the Sybaris ruins. We carried out a muldisciplinary approach combining boreholes stratigraphy and ancient cartography analysis and acquisition of 2D Electrical Resistivity Tomography (ERT). We identified four main units: (1) the Late Pleistocene sandygravelly alluvial and coastal plain deposits, (2) early-middle Holocene clayey sediments of marine-marshy-lagoon origin, (3) a middle-late Holocene sandy beach ridge system and (4) late Holocene deltaic sediments. The elevation contours of the top for the Pleistocene basement reveal a Holocene SFZ activity or reactivation that has probably created space for a different arrangement of late Pleistocene and Holocene units in the surrounding Crati River area. Furthermore, an ERT allows to observe evidences of the SFZ close to Sybaris. Considering the different stratigraphic units thickness and association, we suggest that the SFZ Holocene activity drove the plain evolution influencing the development of different depositional environmental conditions between hanging wall and footwall. In detail, major delta-building events reconstruction suggests that at the end of last-glacial transgression (around 6 kyr B.P.) a wide wetland and a shallow water bay environment took place on the hanging wall. On the foot wall, the Crati River built its terminal plain and its delta. Up to Sybaris time (2.7-2.5 kyr B.P.), the high subsidence on the hanging wall favoured the deposition of thick wetland deposits passing seaward to the shallow water sediment of the coastal embayment. At the same time, on the foot wall the Crati Delta progradation went on reaching the area southward from the Sybaris settlement. Up to the present day, the tectonics has been influenced the plain topography, producing a depressed area on the hanging wall, marked by widespread presence of humid zones. The present confluence between Crati and Coscile Rivers happens in correspondence to the SFZ. We suggest that the the ground-tilting drives the Coscile River channel to avulse periodically toward the SFZ (the down-tilt side with minimum elevation), with the consequent confluence in the Crati River, during the active tectonic period and to move away from the SFZ during quiescent one producing the two rivers separation. The latter can be favored by sediments accumulation close to the SFZ, which re-establish the pre-tilting equilibrium. In conclusion, our approach aims to identify the SFZ as a major agent controlling deposition and landform development by creating accommodation space for the deposition of coastal sediments along Sibari Plain during the Holocene.

A stratigraphic revision of the Paludi Formation, cropping out in Northern Calabria on the north-eastern side of Sila Massif, has confirmed that it has been deposited between two main tectonic phases. Actually the formation is involved only by top to the north-east thrusts, different from those separating the crystalline and ophiolitic nappes of Northern Calabria, and rests unconformably on the Sila Unit, the uppermost nappe of the tectonic stack. In the frame of the interpretation of Northern Calabria as a fragment of the Alps, the Paludi Formation play the role of a deposit post-dating the eo-alpine tectonic phases and pre-dating the Apenninic orogenic transport. Therefore the Aquitanian age of the formation, obtained by nannofloras analyses, can be considered the minimum age to the Apulia-verging orogenic transport, witnessed by top to north-east thrusts. It fairly corresponds to the age referred to the Lucanian ocean closure.

The branched trace fossil Chondrites affinis (Sternberg, 1833), synonymised so far with C. targionii (Brongniart, 1828), has been analyzed in an exceptionally well preserved specimen from the Saraceno Formation (?Upper Cretaceous; ?Eocene-Miocene) in the southern Italy, its holotype (Prague Museum), and in other materials. It appeared that C. affinis displays a smaller burrow system/burrow width ratio and a larger size (burrow width typically over 4 mm and burrow system width over 150 mm) than C. targionii, without continuity of the latter parameters between these ichnospecies. Therefore, Chondrites affinis is considered as a separate ichnospecies, and is recommended for further use. It occurs in Upper Cretaceous to Neogene offshore, deep-sea, mostly marly sediments, and its unquestionable occurrences are known so far from the European Alpides., Rivista italiana di Paleontologia e Stratigrafia, Vol 118, No 2

Gli autori presentano la loro esperienza nella ricostruzione post-traumatica dell'arto inferiore.

L'importanza del lobo auricolare nell'estetica del volto giustifica il gran numero di tecniche chirurgiche utilizzate per la correzione di perdite di sostanza parziali (schisi) o totali in questa sede. Gli Autori, dopo un'attenta revisione della letteratura internazionale presentano le tecniche ricostruttive da loro piừ utilizzate nel trattamento di questa patologia.

Three cores (MBS1, MBS2 and MBS3), 15-12 m thick, were drilled offshore near the Trigno river mouth (Central Adriatic coast, Molise Region), 150-300 m from the present coastline. Palaeoecological analyses by means of benthic foraminifers, molluscs and ostracods, supported by stratigraphic and chronological data, have been performed to reconstruct the Late Quaternary palaeoenvironmental evolution of the northern sector of the Molise Adriatic coast.At the bottom of the cores MBS1 and MBS3 (fig. 1), fluviatile barren gravels (lithofacies G) are present. In the core MBS2 the succession starts with grey clays (lithofacies Cg) containing marine infralittoral foraminifers, hygrophilous terrestrial molluscs and freshwater ostracods. Sediments of lithofacies Cg were also recognized above lithofacies G in the core MBS3; here the fossil record consists of marine infralittoral foraminifers, freshwater and hygrophilous terrestrial molluscs, freshwater and marine infralittoral ostracods. Two AMS C dates constrain the deposition of lithofacies Cg (MBS3) between 19945 ± 345 and 19165 ± 195 yr BP (fig. 1). In the cores MBS2 and MBS3, lithofacies Cg is overlaid by light brown silty clays (lithofacies Csb) containing marine infralittoral foraminifers and molluscs, and marine and freshwater ostracods. In the core MBS1, both lithofacies Cg and Csb lack, and lithofacies G is overlaid by grey silty clays (lithofacies Csg) containing hygrophilous terrestrial molluscs and mainly freshwater ostracods. The three cores are closed up by brown, fine to medium sands (lithofacies S) recording the dominance of marine infralittoral fauna. One AMS C date carried out on benthic foraminifers (Ammonia sp.) collected from the lower portion of lithofacies S (core MBS3) gave an age of 8120.5 ± 108.5 yr BP.

In the academic literature on technological innovation there are repeated arguments demonstrating that disruptive innovations are difficult to adopt for incumbents, and often cause failures to enter into new markets. There is evidence that many incumbents need a long time to achieve the entry. This is mainly due to the reluctance to adopt technologies that render obsolete the established knowledge base. While there is a general consensus about the elements determining these difficulties, it is still unclear how and to what extent these elements affect the time needed to incumbent firms to achieve the entry. The main purpose of this paper is to understand the determinants of time-to-entry of incumbent firms in face of disruptive innovations. The proposed contribution is theoretical and is developed in three components: (1) development of a theoretical model that breaks down time-to-entry process in three constructs: time of recognition, i.e. the identification of innovative technology; time of reaction, that is the speed to invest in the new know-how; and time of implementation, specifically the time to integrate new technologies in productive processes. (2) Formulation of some theoretical propositions on the determinants of the temporal length of the above mentioned sub-processes that precede entry. (3) Articulation of suggestions for an agenda of future research on time-to-entry.