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(a) Geological sketch map of the Cilento area, showing all analyzed outcrop locations. (b) Geological cross-sections (located in a).
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The early stages of southern Apennine development have been unraveled by integrating the available stratigraphic record provided by synorogenic strata (of both foredeep and wedge-top basin environments) with new structural data on the Liguride accretionary wedge cropping out in the Cilento area, southern Italy. Our results indicate that the final o...
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... from the Early Miocene, all of these units were deformed and accreted into the Apennine tectonic wedge Vitale et al., 2010) and then unconformably overlain by wedge-top basin deposits of the Cilento Group ( Amore et al., 1988) and Monte Pruno Fm ( Ciarcia et al., 2009). In the Cilento, only the Parasicilide and Nord-Calabrese Units crop out (Fig. 3a). The 'Internal' Units (i.e. the Liguride Units) tectonically overlie the 'External' Units that were derived from the deformation of sedimentary cover successions belonging to the Apulian continental margin (Fig. 3a). These comprise shallow-water and slope carbonates (Apennine Platform) and pelagic basin (Lagonegro Basin) successions ...
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... et al., 1988) and Monte Pruno Fm ( Ciarcia et al., 2009). In the Cilento, only the Parasicilide and Nord-Calabrese Units crop out (Fig. 3a). The 'Internal' Units (i.e. the Liguride Units) tectonically overlie the 'External' Units that were derived from the deformation of sedimentary cover successions belonging to the Apulian continental margin (Fig. 3a). These comprise shallow-water and slope carbonates (Apennine Platform) and pelagic basin (Lagonegro Basin) successions (e.g. Mazzoli et al., 2008, and references therein). Lower-Middle and Upper Miocene wedge-top basin deposits occur on top of the tectonic pile (Fig. ...
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... Nord-Calabrese Unit is generally tectonically superposed onto the Parasicilide Unit (e.g. Alento and Lambro River Valleys, Fig. 3a). However, in the Sapri area it lies directly over the carbonates of the Apennine Platform, whereas northeastward of Cicerale-Monte Centaurino, this unit does not crop out (e.g. Torrente Pietra and Sele River Valleys Fig. ...
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... Nord-Calabrese Unit is generally tectonically superposed onto the Parasicilide Unit (e.g. Alento and Lambro River Valleys, Fig. 3a). However, in the Sapri area it lies directly over the carbonates of the Apennine Platform, whereas northeastward of Cicerale-Monte Centaurino, this unit does not crop out (e.g. Torrente Pietra and Sele River Valleys Fig. ...
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... Cilento Group unconformably covers the already deformed and imbricated Nord-Calabrese and Parasicilide Units. This feature is shown in the geological map (Fig. 3a) and in cross-section X-X' (Fig. 3b): the Cilento Group seals the Crete Nere and Saraceno Fms (Nord-Calabrese Unit) in the Alento River Valley, west of the Lambro River and in the Sapri area, whereas it covers the Parasicilide Unit (located in the footwall to the Nord-Calabrese Unit) between Monte Sacro and Monte Centaurino and in the ...
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... Cilento Group unconformably covers the already deformed and imbricated Nord-Calabrese and Parasicilide Units. This feature is shown in the geological map (Fig. 3a) and in cross-section X-X' (Fig. 3b): the Cilento Group seals the Crete Nere and Saraceno Fms (Nord-Calabrese Unit) in the Alento River Valley, west of the Lambro River and in the Sapri area, whereas it covers the Parasicilide Unit (located in the footwall to the Nord-Calabrese Unit) between Monte Sacro and Monte Centaurino and in the northeastern area, between the ...
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... type 2-3, Fig. 5a). A crenulation cleavage (S 2 NC ) and a crenulation lineation (L 2 NC ) occur in the pelitic units. Bedding (S 0 NC ) is marked by the occurrence of arenitic beds or by layers of differing composition and color in the fine-grained layers. A macroscale fold (here termed Orria Syncline, as it is exposed around the Orria village; Fig. 3a) and related parasitic folds F 3 NC deform this succession in the NE sector of the study area, whereas rare mesoscale F 3 NC folds occur elsewhere. Orientation data for the main structures exposed between Pisciotta Marina and Pioppi ( Fig. 3a) (Fig. 6b) show a mean plunge of 051/19 and mesoscopic fold hinges A 2 NC ( Fig. 6g) form a ...
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... layers. A macroscale fold (here termed Orria Syncline, as it is exposed around the Orria village; Fig. 3a) and related parasitic folds F 3 NC deform this succession in the NE sector of the study area, whereas rare mesoscale F 3 NC folds occur elsewhere. Orientation data for the main structures exposed between Pisciotta Marina and Pioppi ( Fig. 3a) (Fig. 6b) show a mean plunge of 051/19 and mesoscopic fold hinges A 2 NC ( Fig. 6g) form a cluster around the mean value of 064/12 whereas in the Pioppi area A 1 NC data ( Fig. 6c) define a girdle. The crenulation lineation (L 2 NC ) is parallel to A 2 NC fold hinges ( Fig. 6h), to which is clearly related, and displays a mean plunge ...
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... analysis on the Saraceno Fm has been carried out separately for the pelitic-calcareous lower part (Punta Telegrafo Member) and for the arenitic-marly middle-upper portion. The analyzed lower part of the formation crops out at Pisciotta Marina, Punta Telegrafo and Torre di Caleo (Fig. 3a). The Punta Telegrafo Member is characterized by the superposition of three meso-scale fold sets F 1 NC , F 2 NC and F 3 NC ( Fig. 5b). F 1 NC folds show tight to isoclinal geometries, with shapes ranging from chevron, rounded and box types (Fig. 5b). Generally F 1 NC folds in pelitic rocks are of class 3 of Ramsay (1967), whereas they ...
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... and to analyze the role of bed-thickness on folding style, (i) the lower part (Cannicchio Sandstones Member) of the Pollica Fm, (ii) the middle-upper part of the Pollica Fm, and (iii) the San Mauro Fm have been analyzed separately. The analyzed outcrops are localized around the Pollica, Omignano, Orria, Gioi, Salento and Catona villages (Fig. ...
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... outcrops of the Cannicchio Sandstones Member have been analyzed, particularly in the Cannicchio type-locality (close to the Pollica village; Fig. 3a). In this area the succession is characterized by (F 1 CG ) folds showing kink and chevron shapes (Fig. 8c), and subordinate rounded or box geometries. These folds are often detached along pelitic layers (Fig. 8c) forming SE verging asymmetric fold trains characterized by overturned short limbs. It is common to find stiff beds ...
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... fold trains characterized by overturned short limbs. It is common to find stiff beds sandwiched between pelitic layers and shortened by NW or SE dipping pre-buckle thrusts showing minor displacements (Fig. 8d). Minor thrust faults occur also in fold hinge regions to accommodate shortening in thinner layers (Fig. 8c, inset). In the Omignano area (Fig. 3a) the whole succession is deformed by a SE verging, overturned macroscale F 1 CG fold and associated parasitic structures. In the area between Omignano, Pollica and Ogliastro, F 1 CG fold hinges of both meso-and macro-scale folds show a general NE-SW trend. A spaced, disjunctive cleavage (S 1 CG ) is associated with these ...
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... ranging from open to tight, with chevron, rounded, box and kink shapes (Fig. 8e and f). Deformation in fold hinge regions is often accommodated by thrust faults or by cataclasis producing intense brecciation (Fig. 8f). Also in this part of the succession, pre-buckle thrusts commonly affect single stiff layers (Fig. 8g-i). In the Omignano area (Fig. 3a) minor parasitic folds are related to the previously mentioned overturned, SE verging major F 1 CG fold. The middle-upper part of the Pollica Fm is also deformed by the previously mentioned regional fold and associated S-SW verging parasitic folds in the Orria-Gioi ...
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... to the development of intrafolial folds. Such previously lengthened fold limbs, characterized by boudinage of the stiff layers, were subsequently shortened (locally developing 'folded boudins'; Ramsay and Huber, 1983) ) is characterized by the local development of meso-and macro-scale F 3 NC folds (such as in the Pisciotta-Ascea and Orria areas, Fig. 3a) displaying open to tight ...
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... 2010). Like the NordCalabrese Unit, the Parasicilide succession is also deformed, in the NE part of the study area, by the regional (F 3 PS ) Orria Syncline. A late, extensional origin of the contacts between the NordCalabrese and Parasicilide Units is suggested by the geometry of the tectonic contact in the Castelnuovo Cilento tectonic window (Fig. 3a, cross-sections of Fig. 3b), which dramatically cuts all folds in both footwall and hanging-wall units ( Vitale et al., 2010), as well as in the Sapri area, where the Nord-Calabrese Unit directly overlies the Apennine Platform succession with the tectonic omission of the Parasicilide Unit and part of the Crete Nere Fm. The simple restoration provided in Fig. 10 ...
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... tectonic contact between the Nord-Calabrese Unit and the Parasicilide Unit is gently folded by broad NE-SW trending antiforms, probably related to footwall imbrication as shown in the geological section X-X' in Fig. 3(b). This suggests that thrusting involving the Apennine Platform succession and wedge collapse were roughly coeval. Probably part of the Apennine Platform succession (Monte Bulgheria; Fig. 3a) was exposed already in Middle Miocene time, feeding the Cilento Group with calcareous finegrained sediments (San Mauro Fm). In this case, the ...
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... the Parasicilide Unit is gently folded by broad NE-SW trending antiforms, probably related to footwall imbrication as shown in the geological section X-X' in Fig. 3(b). This suggests that thrusting involving the Apennine Platform succession and wedge collapse were roughly coeval. Probably part of the Apennine Platform succession (Monte Bulgheria; Fig. 3a) was exposed already in Middle Miocene time, feeding the Cilento Group with calcareous finegrained sediments (San Mauro Fm). In this case, the tectonic window of Castelnuovo Cilento (Alento Valley; Fig. 3a) may be interpreted as a breached anticline related to thrusting in the underlying Apennine Platform ...
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... the Apennine Platform succession and wedge collapse were roughly coeval. Probably part of the Apennine Platform succession (Monte Bulgheria; Fig. 3a) was exposed already in Middle Miocene time, feeding the Cilento Group with calcareous finegrained sediments (San Mauro Fm). In this case, the tectonic window of Castelnuovo Cilento (Alento Valley; Fig. 3a) may be interpreted as a breached anticline related to thrusting in the underlying Apennine Platform ...
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... range from tight to open and show kink geometries. Folding occurred at very low-T conditions, as evidenced by brittle deformation associated with tight folds. In the NE sector of the study area, the successions belonging to the Cilento Group and the underlying Nord-Calabrese and Parasicilide Units are all deformed by the regional Orria Syncline (Fig. 3a). This major fold is accompanied by a system of S-SW overturned parasitic folds (cross-section Y-Y' in Fig. 3b). The 1 -axes obtained from the poles to bedding measured in the Pollica and San Mauro Fms from different areas (Fig. 9c, m, n, t and u) point out an overall curved fold hinge for the regional fold. Statistical ( 1 ) Zuppetta ...
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... brittle deformation associated with tight folds. In the NE sector of the study area, the successions belonging to the Cilento Group and the underlying Nord-Calabrese and Parasicilide Units are all deformed by the regional Orria Syncline (Fig. 3a). This major fold is accompanied by a system of S-SW overturned parasitic folds (cross-section Y-Y' in Fig. 3b). The 1 -axes obtained from the poles to bedding measured in the Pollica and San Mauro Fms from different areas (Fig. 9c, m, n, t and u) point out an overall curved fold hinge for the regional fold. Statistical ( 1 ) Zuppetta and Mazzoli (1997), the general lack of cleavage development and of grain-scale deformation associated with the ...
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... order to obtain a synoptic view of the fold trends in the whole study area, mesoscopic fold axis trends (both for the Liguride Units and the Cilento Group) are plotted in the geological map of Fig. 3a. It is worth noting that a broad homogeneity in fold axis trends exists for the Liguride Units (F 1-2-3 NC , F 1-2-3 PS ) and for the Cilento Group (F 1 CG ). The rough coaxiality between the first fold set (F 1 CG ) in the Cilento Group and F 1-2-3 NC and F 1-2-3 PS fold sets in the NordCalabrese and Parasicilide Units suggests a more ...
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... to suppose a main SE/E tectonic transport for these units according to Miocene kinematic reconstructions proposed by several authors (e.g. Vignaroli et al., 2009 and references therein). This is consistent with the SE vergence of first-phase isoclinal folds in the Parasicilide Unit exposed in the tectonic window of Castelnuovo Cilento ( Fig. 3a; Vitale et al., 2010), as well as with top-to-the-ESE kinematics unraveled by Vitale and Mazzoli (2009) for carbonate thrust sheets originally forming part of the Apennine Platform in the Calabria-Lucania border area ( Iannace et al., 2007). Major differences in deformation styles occur between the Liguride Units and the Cilento Group. ...
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... The southern Apennines are the result of compressive tectonic dynamics characterised by an oblique collision of the Calabrian forearc with the Apulian margin (Filice and Seeber, 2019) that evolved from an antecedent subductive phase of thrust emplacement (Vitale et al., 2011;Vitale and Ciarcia, 2013). Currently, the external (eastern) margin preserves the compressive tectonics, while the internal sector is characterised by an extensive dynamic with tension faults that dissect the pre-existent fold and thrust structure (Brozzetti et al., 2009;Schiattarella et al., 2003). ...
Detailed and accurate geomorphological historical landslide inventory maps are an invaluable source of information for many research topics and applications. Their systematic preparation worldwide has been advised by many researchers as it may foster our knowledge on landslides, their spatial and temporal distribution, their potential interaction with the built environment, their contribution to landscape dynamics, and their response to climate change in the past. Due to the extreme variability of the morphological and radiometric elements that can reveal historical landslides, geomorphological historical landslide inventory maps are produced by expert interpretation, which makes it a time-consuming and expensive process, which often discourages wide-area mapping activities. In this paper we present a new geomorphological historical landslide inventory map for a 1460 km2 area in the Daunia Apennines, the north-western sector of the Apulia (Puglia) region, in southern Italy. The inventory contains 17 437 landslides classified according to relative age, type of movement, and estimated depth. Landslides were mapped according to rigorous and reproducible criteria applied by two teams of expert photo interpreters to two sets of stereoscopic aerial photographs taken in 1954/55 and 2003. The dataset consists of a digital archive publicly available at https://doi.org/10.1594/PANGAEA.942427 (Cardinali et al., 2022).
... Miocene wedge-top deposits outcrop in the central and western portion of the CVDA Geopark, where hilly landforms dominate. These deposits are made up of alternating puddingstones, sandstones and mudstones forming the so-called Cilento Group [34][35][36][37][38]. Internal units made up of mainly clayey and silty deposits are preserved in some topographic lows and along some sectors of the coastal belt, such as at Punta Telegrafo near Ascea (Figure 1), where the strongly deformed Crete Nere Formation outcrop is found [39,40]. Quaternary deposits are also present and include marine and continental deposits, mainly made of conglomerates and sandstones, which accumulated both along the coastal strip and in the inner sectors of the Geopark [41][42][43][44][45]. ...
... Here, it is possible to observe a wave-cut terrace carved on the Saraceno Formation during the Last Interglacial period ( Figure 12A) when the climate was warmer, and the sea level was higher than the present. Above it, continental slope breccias are well preserved ( Figure 12B), which testify to the colder climate conditions that occurred during the Last Glacial period [39,67]. The Vallo di Diano is also characterized by the presence of a wide system of coalescing alluvial fans, occurring along the footslope of the Maddalena Mts. ...
... Here, it is possible to observe a wave-cut terrace carved on the Saraceno Formation during the Last Interglacial period ( Figure 12A) when the climate was warmer, and the sea level was higher than the present. Above it, continental slope breccias are well preserved ( Figure 12B), which testify to the colder climate conditions that occurred during the Last Glacial period [39,67]. ...
The interest of the scientific community about geotourism is abruptly increasing, as well as that on geoparks. According to UNESCO, geoparks should define management policies addressed to increasing the awareness of local people and tourists about Earth's dynamics to reduce the impact of climate change and natural disasters. With this aim in mind, we tried to provide a solid scientific approach to geotourism that could be useful to the development of a geotourism strategy in the Cilento, Vallo di Diano and Alburni (CVDA) Geopark, in Southern Italy. Starting from the official inventory of the CVDA Geopark, we defined the potential Education Value (EV) and potential Touristic Value (TV) of each of the 160 sites listed by applying the Brilha method. Then we selected 20 geosites and geomorphosites with high values of both the EV and TV, and we included them in two geoitineraries. The two geoitineraries move in the inner sector of the Geopark (i.e., from the Paestum archaeological area to the Vallo di Diano basin) and along a portion of the coastal stretch (i.e., from Punta Telegrafo cape to the Lambro and Mingardo rivers' mouths). Selected sites are representative of several geoscience disciplines (e.g., geomorphology, structural geology, quaternary geology, hydrogeology), thus suggesting that the CVDA Geopark is an ideal place where dissemination of geoscience concepts may be carried out. The latter point enhances the high geotourism potential of the area. This kind of approach was not tried before in the CVDA Geopark and can be a useful example of how to promote touristic development strategies in the area.
... The superposition of different thrust-sheets characterizes the study area (Figure 1a,b). The main tectonic units refer to three paleogeographic domains: (i) Ligurian Accretionary Complex (Parasicilide unit; [25][26][27][28][29][30][31]); (ii) Apennine Platform (Picentini Mts and Mt Croce units; [7,8,[19][20][21][22][23][24][32][33][34][35][36][37][38][39]); (iii) Lagonegro-Molise Basin (Frigento unit; [7,8,10,[40][41][42][43][44]). ...
... As suggested by [11,31], we associate this extensional event with the formation of several structural depressions where the CVTG sediments were deposited. A synorogenic extensional environment was also envisaged for the older Langhian-lower Tortonian wedge-top basin deposits of the Cilento Group [27,28,31]. A recent study [50] in the Cilento area (Figure 1a) about temperature-dependent clay minerals and vitrinite reflectance in the Cilento Group and Mt Sacro Fm (CVTG) indicates a basin evolution marked by two phases of severe subsidence, interpreted as the result of syn-orogenic extension at shallow crustal levels. ...
We present a structural study on the tectonic windows of Giffoni and Campagna, located in the western sector of the southern Apennines (Italy). We analyzed thrusts, folds, and related minor deformation structures. Here, a major in-sequence E-verging thrust fault juxtaposes Meso-Cenozoic successions of the Apennine Platform (Picentini Mts unit) and the Lagonegro-Molise Basin (Frigento unit). However, out-of-sequence thrusts duplicated the tectonic pile with the interposition of the upper Miocene wedge-top basin deposits of the Castelvetere Group. We reconstructed the orogenic evolution of these two tectonic windows, including five deformation phases. The first (D1) was related to the in-sequence thrusting with minor thrusts and folds, widespread both in the footwall and the hanging wall. A subsequent extension (D2) has formed normal faults crosscutting the D1 thrusts and folds. All structures were subsequently affected by two shortening stages (D3 and D4), which also deformed the upper Miocene wedge top basin deposits of the Castelvetere Group. We interpreted the D3-D4 structures as related to an out-of-sequence thrust system defined by a main frontal E-verging thrust and lateral ramps characterized by N and S vergences. Low-angle normal faults were formed in the hanging wall of the major thrusts. Out-of-sequence thrusts are observed in the whole southern Apennines, recording a crustal shortening event that occurred in the late Messinian-early Pliocene. Finally, we suggest that the two tectonic windows are the result of the formation of an E-W trending regional antiform, associated with a late S-verging back-thrust, that has been eroded and crosscut by normal faults (D5) in the Early Pleistocene.
... In such ridges, karst cave systems associated with the most important underground water reservoirs of the region are preserved [33][34][35]. The carbonate massifs alternate with a hilly landscape, with gentle slopes and dendritic drainage pattern, where pelagic and clastic successions dominate [36][37][38][39][40]. They are represented by the Cilento Group deposits (age between 17.7 and 10.8 million years), with the Pollica and S. Mauro Formations, mainly made up of alternating sandstones, marls and puddingstones [41][42][43]. ...
... They are represented by the Cilento Group deposits (age between 17.7 and 10.8 million years), with the Pollica and S. Mauro Formations, mainly made up of alternating sandstones, marls and puddingstones [41][42][43]. The basinal successions (age between 65 and 22 million years) are well exposed in the southern part of the study area (Ascea-Velia) and are made up of the Crete Nere formation, dark clayey successions more than 500 m thick [36,44]. All these units have been involved in the complex tectonic history leading to the formation of the Southern Apennine chain, and for this reason they appear strongly deformed by fault and fold systems [37,45]. ...
“Geotourism” is a particular type of “sustainable tourism” that is still in an embryonic stage, especially in Italy. The main goal is the transmission of geological knowledge to increase the awareness about geoheritage, geo-resources and geo-hazards. The geoparks represent ideal sites, with a strong educational significance for students, teachers, geo-tourists, and guides interested in geological and environmental sciences, though at different levels. With this in mind, we propose a geoitinerary through some of the most geologically interesting coastal areas in the Cilento, Vallo di Diano, and Alburni Geopark. The aim of the geoitinerary is to provide a good example of how geosites could be promoted through geotourism and used as means of divulgation of geological and environmental knowledge. The selected sites are the San Marco coast, the Licosa Cape and the Elea-Velia archaeological area. They are included in the official list of geosites and geomorphosites of the Geopark and have a relevant stratigraphic and geoarcheological value. The San Marco coast and the Licosa Cape are the “best sites” in the Geopark where Quaternary coastal deposits and morphologies are represented. The Elea-Velia site is one of the most famous archeological sites in the Geopark, which is also representative of complex human-environment interactions. Despite their high scientific significance, the sites that we have selected are not included in a specific promoting program. We have so tried to fill this gap by providing the scientific background for their geotouristic promotion that could also serve as an instrument for the increase of the local economy.
... Moreover, flysch units have been eroded from the high carbonate peaks and are preserved only along the main valleys [75]. The complex tectonic evolution of the area is discussed in other studies [76][77][78][79][80][81][82]. ...
In this paper we want to stress the role of geotourism as a means to promote environmental education and, on occasion, as a way to increase the touristic interest of an area. Geoparks are certainly the territory where geotourism can be best exploited. We propose a geoitinerary to discover the amazing, but poorly known, Middle Bussento Karst System, with the blind valley of the Bussento River, in the southeast of the Cilento, Vallo di Diano and Alburni United Nations Educational, Scientific and Cultural Organization (UNESCO) Global Geopark. This is the only example, in Southern Italy, of a stream sinking underground and it is the second longest subsurface river path in Italy, making this a core area of the Geopark. We combined field surveys and literature data to create a geoitinerary that can be useful in helping to promote this site. This geoitinerary is applicable to both simple generic visitors and geo-tourists and has an educational purpose, especially in explaining the significance and the fragility of karst areas in terms of environmental protection. Moreover, it may represent a sort of stimulus for the growth of touristic activity in this inner area of the Geopark.
... Location of "P.R. 264" linear infrastructure in Campania Region (a), in the geological sketch Location of "P.R. 264" linear infrastructure in Campania Region (a), in the geological sketch map of the Cilento area (b) (modified from[52]) and its reference on the orthophoto map (c) and on a Digital Terrain Model (DTM) (d). ...
The Italian territory is strongly affected by ground instability events such as landslides and subsidence phenomena, representing the main causes of damage along linear infrastructures network. For this reason, an effective monitoring system should be needed during the exercise phase to support control and management activities by owners and authorities. Actually, control of the Italian infrastructures is demanded to technicians and maintenance teams who detect, through visual control, anomalies and failures which require a site-specific monitoring. Such approach could represent a limited and only partial information to fully characterize and to investigate the infrastructure potential damage and can be highly expensive if a high density of measurements suitable for wide-scale infrastructure monitoring is required. Necessity of a very fast procedure for monitoring of these man-made infrastructures, finds in the application of modern remote sensing techniques a valid response to support infrastructures health assessments. In this work, Differential SAR Interferometry (DInSAR) has been used to investigate stability condition of S.P. 264 linear infrastructure, in Salerno Province (Italy), which is affected by several slow-moving landslides. Furthermore, an analysis of costs and benefits derived by using DInSAR technique has been provided. As result, the use such technology can be recommended for large areas studies, for which conventional punctual measurements can be highly expensive.
... Location of "P.R. 264" linear infrastructure in Campania Region (a), in the geological sketch Location of "P.R. 264" linear infrastructure in Campania Region (a), in the geological sketch map of the Cilento area (b) (modified from[52]) and its reference on the orthophoto map (c) and on a Digital Terrain Model (DTM) (d). ...
The occurrence of geological events such as landslides is one of the main causes of damage along linear infrastructures: Damage to transport infrastructures, as roads, bridges, and railways, can restrict their optimal functions and contribute to traffic accidents. The frequent and accurate monitoring of slope instability phenomena and of their interaction with existing man-made infrastructures plays a key role in risk prevention and mitigation activities. In this way, the use of high-resolution X-band synthetic aperture radar (SAR) data, characterized by short revisiting times, has demonstrated to be a powerful tool for a periodical noninvasive monitoring of ground motion and superstructure stability, aimed at improving the efficiency of inspection, repairing, and rehabilitation efforts. In the present work, we suggest a semiautomatic GIS approach, which, by using satellite radar interferometry data and results of geomorphological field survey integrated in a qualitative vulnerability matrix, allows to identify sections with different levels of damage susceptibility, where detailed conventional in situ measurements are required for further analysis. The procedure has been tested to investigate landslide-induced effects on a linear infrastructure in Campania Region (Italy), the Provincial Road “P.R. 264”, which is affected, along its linear development, by several slope instabilities. COSMO-SkyMed interferometric products, as indicator of ground kinematics, and results of in situ damage survey, as indicator of consequences, have been merged in a qualitative 4 × 4 matrix, thus obtaining a vulnerability zoning map along a linear infrastructure in January 2015. Furthermore, an updating of landslide inventory map is provided: In addition to 24 official landslides pre-mapped in 2012, 30 new events have been identified, and corresponding intensity and state of activity has been detected.
... The allochthonous units are composed of deep marine units consisting of the Sicilide complex, in this area represented by the Argille Varicolori, and Liguride units, and carbonate deposits of the Apennine platform. Together these domains are interpreted as the record of an accretionary wedge related to the subduction of Neotethys oceanic crust during the Late Cretaceous-Paleogene (Casero et al., 1988;Vitale et al., 2011;Ciarcia et al., 2012). The lower structural level is characterized by highly allochthonous Mesozoic-Paleogene platform carbonates (Apennine Platform) and pelagic basin (Lagonegro) units tectonically overlying a buried, deep-seated (Apulian) carbonate inversion belt (Butler et al., 2004;Mazzoli et al., 2008Mazzoli et al., , 2014. ...
The Plio-Pleistocene Calvello-Anzi Basin (CAB) represents a synorogenic shallow marine to alluvial succession deposited during the late phase of the Apennine Orogenic event. While the stratigraphy and sedimentary cycles are well known, the precise role and timing of the tectonic phases affecting this area are unclear. In this paper we report the major findings from a study aimed at unraveling the signatures of the Plio-Quaternary tectonic events affecting the CAB and this portion of the Southern Apennines by using a field integrated approach characterized by facies analysis, structural surveying, and basin architecture. The CAB is located in the axial portion of the Southern Apennine chain and has a roughly E-W orientation which is at a high angle with respect the main NW-SE striking regional tectonic structures controlling the foreland-directed migration of the compression. In the study area, an approximately 1,200-meter-thick package of Zanclean (early-middle Pliocene) to Santernian (middle Pleistocene) shelf, shallow marine, and alluvial deposits accumulated during the late stages of the Apennine orogenic evolution. Within the CAB deposits we recognize two main depositional motifs which roughly correspond to previously established regional cycles that are genetically linked to two corresponding tectonic phases of the Southern Apennine chain. Our results reveal how these two main tectonic phases played a primary role in controlling the depositional architecture, facies, depocenter distribution, and the basin shape throughout the CAB's lifespan. In the proposed model, during the first depositional stage (Zanclean), the CAB formed as a wedge-top basin, controlled by the subsurface propagation of NW-SE-trending thrusts related to the main NE-SW directed shortening of the Apennines. This stage is recorded in the basal units of the CAB infill by progressive unconformities, the development of syn-tectonic shallow marine sedimentary wedges along a high gradient tectonically controlled depositional surface, and a marked SE migration of the main depocenter. During the second depositional stage (upper Piacenzian to Santernian), the CAB was controlled by a series of roughly E-W-trending normal faults which crosscut the preexisting compressional structural fabric. Syndepositional activity along these faults played a direct role in creating an E-W oriented tectonic depression and controlling the accommodation space for the upper portion of the CAB infill. This second stage is marked by two points of evidence. The first point is revealed by a southwestward migration of the CAB depocenter driven by ~90-degree rotation from a roughly NW-SE elongated pattern to roughly elongated W-E transverse to the Pliocene regional structural fabric. This depocenter drift also coincides with an abrupt change in depositional regime from shallow marine to continental sedimentation. The second and most important point of evidence is the presence of several basin-bounding extensional fault zones which cut the lower Pliocene basin-fill units. We relate these features to the middle upper Pleistocene transition to along-strike extension, widely reported in the Southern Apennines, which is related to the overall extensional regime that is acting on the chain also at present. Data from this study provide additional insight into the evolution of the Southern Apennine chain, the formation of the Plio-Pleistocene CAB, and the debated role of Quaternary tectonics on the basin's development during the post-collision orogenic phases. Given the proximity of the study area with several oil fields and considering that hydrocarbon traps in Southern Apennines are Plio-Quaternary in age, the constraints provided on the timing and the style of the regional deformation may improve the definitions of hydrocarbon traps in the buried Apulian platform.
... In contrast, the external units consist of carbonate platform sequences partly from the Apulian margin (Bonardi et al., 2009;. The Apennine tectonostratigraphic wedge is therefore consistent with a classical collision complex that evolved from an earlier subduction phase into a thrust-emplacement phase (Vitale et al., 2011). ...
The Pollino Massif is the most southeastern outcrop of the Apennine core. It marks the transition between Apenninic shortening and extension, respectively, SE and NW of the massif and is also the cusp of a southeastward plunge that characterizes the submerged Apennines. The SE limit of NE‐SW extension merges with the east limit of Tyrrhenian extension in Calabria. This strategic position is expected to transition southeastward in the progressive oblique collision of the Calabrian forearc and Apulia. We test this hypothesis using published results and new field data. The time‐transgressive emergence of basins on the Apennine thrust wedge is quantitatively consistent with the ESE rollback of the Calabrian arc. Specifically, a thrust‐normal slip reversal on a SW dipping fault is responsible for the tectonic collapse that lead to the Mercure Basin along strike NW of the Pollino Massif and to an east‐to‐west reversal of drainage. This reversal is timed by an intermediate stage of trapped internal drainage with Mid-Pleistocene lacustrine sedimentation, but it may young to SE as the normal displacement on the border fault decreases gradually to
SE and vanishes near the apex of the massif. On the SE side of the massif, contractional tectonics persists at least into the Mid‐Pleistocene and likely later, while NE‐SW extension is absent. Prominent normal faults in that area accommodate range‐parallel extension and are coupled with the thrust faults. The combination of longitudinal extension with a counterclockwise rotation of hanging‐wall units and thrust directivity can account for the final setting in the Apennines.
... Early orogenic normal faulting in the Central and Northern Apennines has been interpreted by several authors as the response to flexural bending of the lithosphere (e.g., peripheral bulge; Bradley and Kidd; (C) Doglioni, 1995;Tavani et al., 2015, and reference therein) and has been highlighted by field evidence and imaged in seismic cross sections (Tavarnelli and Peacock, 1999;Scisciani et al., 2002;Mirabella et al., 2004;De Paola et al., 2006;Carminati et al., 2014). These faults differ from similar extensional structures that triggered exhumation in the adjacent Southern Apennines part of the same orogen (Corrado et al., 2005;Mazzoli et al., 2006Mazzoli et al., , 2008 and also controlled the development of early wedgetop basins (Vitale et al., 2011;Ciarcia et al., 2012;Corrado et al., 2019). In fact, these latter faults were induced at shallow crustal levels by gravitational readjustment within the tectonic wedge associated with thick-skinned shortening at depth during orogen building (e.g., Mazzoli et al., 2008). ...
Temperature-dependent clay mineral assemblages, vitrinite reflectance and 1D thermal and 3D geological modelling of a Neogene wedge-top basin in the Sicilian fold-and-thrust belt and its pre-orogenic substratum allowed us to: (i) define the burial history of the sedimentary succession filling the wedge-top basin and its substratum, (ii) reconstruct the wedge-top basin geometry, depocenter migration and sediments provenance through time in the framework of a source to sink system and (iii) shed new light into the kinematic evolution of the Apennine-Maghrebian fold-and-thrust belt.
The pre-orogenic substratum of the Scillato basin shows an increase of levels of thermal maturity as function of stratigraphic age that is consistent with a maximum burial of 3.5 km in deep diagenetic conditions. In detail, Ro% values range from 0.40 to 0.94% and random ordered illite-smectite (I-S) firstly convert to short-range ordered structures and then evolve to long-range ordered structures at the base of the Imerese unit.
The wedge-top basin fill experienced shallow burial (~2 km) and levels of thermal maturity in the immature stage of hydrocarbon generation and early diagenesis.
Vitrinite reflectance and mixed layers I-S show two populations of authigenic and inherited phases. The indigenous population corresponds to macerals with Ro% values of 0.33-0.45% and I-S with no preferred sequence in stacking of layers whereas the reworked group corresponds to macerals with Ro% values of 0.42-0.47% and short-range ordered I-S with no correlation as function of depth.
Authigenic and reworked components of the Scillato basin fill allowed us to unravel sediments provenance during the Neogene, identifying two main source areas feeding the wedge-top basin (crystalline units of the European domain and sedimentary units of the African domain) and to detect an early phase of exhumation driven by low-angle extensional faults that predates Neogene compression.
