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After more than forty years since the 1980 Irpinia-Lucania earthquake, with this Special Issue "The 23 November 1980 Irpinia-Lucania, Southern Italy Earthquake: Insights and Reviews 40 Years Later" we revisit this milestone geological and seismological event, bringing together the latest views and news on this earthquake, with the aim of improving the dissemination of wide-ranging information on this remarkable case history. This earthquake struck Irpinia-Lucania region (Lucania is also called Basilicata; Southern Italy) on 23 November 1980 (Ms 6.9, Io X MCS) [1,2], and it is remembered in Italy not only for being the strongest earthquake recorded in the last 100 years causing devastation of entire regions and severe loss of human life, but also for the destruction of the cultural heritage in the epicentral area. It was felt throughout Italy, from Sicily in the South, to Emilia Romagna and Liguria in the North (Figure 1) causing damage in over 800 localities spread in the regions of Campania and Basilicata with a total of 75,000 houses destroyed and 275,000 seriously damaged. The number of victims was about 3000

As supplementary material we propose a publication, in which there is the first preliminary attribution of macroseismic intensity for the 1980 earthquake: "Il terremoto del 23-11-1980. Rilievo Macrosismico Stato di Avanzamento al 27-1-1981" [29] and some topographic maps of the effects induced by the 1980 IrpiniaLucania earthquake, which were plotted in the field. Soon after the November 23, 1980 Irpinia - Lucania earthquake, several groups of geologists of the CNR-PFG projects, mapped the coseismic geological effects in a wide portion of the epicentral area. We include some of the original sketch of topographic maps (form 1:25.000 topographic maps of Istituto Geografico Militare, I.G.M., 1955) saved as a historical record of the time, that the Professor Paolo Scandone, as leader of PFG project, made available many years after the earthquake on which the coseismic effects of the 1980 earthquake were mapped. On the excerpts of the topographic maps mainly earthquake-induced fractures are shown, and in some cases it has been marked occurrence of landslides as well as portions of earthquake-induced faults. Although it must be pointed out that many researchers at the time did not believe that these faults were of tectonic origin but ascribed all of them either to pure gravitative sliding or to debris compactation [11]. Only a few Italian researchers interpreted as due tectonic origin the fractures occurred along the Piano di Pecore on Mt. Marzano (186 Colliano IISW), or Sele Valley and at Pantano di S. Gregorio Magno (198 Buccino, I, NE; 199 Vietri di Potenza, IV, NW) [9,10], as later documented by several researchers who reconstructed the end to end seismogenic fault segments [12-17]. As supplementary material, the following are the cartographic union framework of the 1: 25,000 topographic maps attached and the extracts of these maps on which are mapped the coseismic effects detected during the field survey

SUMMARY Following the Mw 3.9 earthquake that occurred in the Ischia island (Naples, southern Italy) on 21 August 2017, the local monitoring seismic network was significantly improved in terms of both number of stations and instrumentation performance. Due to the huge amount of collected seismic ambient noise data, in this paper we present a first 3-D shear wave velocity model of the island retrieved from the inversion of horizontal-to-vertical spectral ratio curves by fixing the shear wave velocities (Vs) and modifying the thicknesses to get the corresponding 1-D Vs models. We are confident about the robustness of the attained models since the inversion process provided a good convergence towards the best-fitting solutions. Then, a first 3-D velocity model was obtained by contouring all the 1-D models obtained for the selected seismic stations to highlight possible lateral variations of the layer thicknesses and to reconstruct the morphology of the deeper interface characterized by a high-impedance contrast. A good correspondence between the 3-D Vs model and the geological features of the island was observed, especially in the northern sector where most of the stations are installed. In particular, the top of the high-impedance contrast interface appears deeper in the northern coastal areas and shallower in the central sector. This result agrees with the structural settings of the island likely due to the resurgence of Mount Epomeo.