Mar Geophys Res DOI 10.1007/s11001-011-9130-4
ORIGINAL RESEARCH PAPER
Geomorphic setting and geohazard-related features along the Ionian Calabrian margin between Capo Spartivento and Capo Rizzuto (Italy) Danilo Morelli • Angela Cuppari • Ester Colizza Francesco Fanucci
•
Received: 10 April 2010 / Accepted: 31 March 2011 Ó Springer Science+Business Media B.V. 2011
Abstract The aim of this work is to describe the morphodynamic processes of coastal and submarine areas based on morpho-bathymetric data and sub-bottom acoustic profiles from the Calabrian Ionian margin (from Capo Spartivento to Capo Rizzuto). We describe some of the most significant geo-hazard features and show some examples of their complex interactions and related potential risk. The relationship between these geo-hazard features and the active tectonics and some severe historical earthquakes and tsunamis is also discussed. The studied area is characterized by several well developed canyon systems. The retrogressive erosion of the canyon heads affects the continental shelf and interacts with the coastal morpho-sedimentary processes, evidencing the intense geomorphic activity of this sector of Ionian margin. The widespread evidence of mass wasting processes and slope instability, together with the historical seismicity, makes this area also an ideal case study for investigating on the possible relationship between earthquakes and landslide-triggered tsunamis and assessing the potential risk. Keywords Marine geo-hazard Submarine landslide Submarine canyon Active tectonics Marine morphology Marine cartography Ionian Calabrian margin D. Morelli (&) A. Cuppari E. Colizza F. Fanucci Department of Geosciences, University of Trieste, Via Weiss 2, 34128 Trieste, Italy e-mail:
[email protected] A. Cuppari e-mail:
[email protected] E. Colizza e-mail:
[email protected] F. Fanucci e-mail:
[email protected]
Introduction During the last decade most research programs in marine geology focused on the analysis of seafloor features and shallow sediments packages, aiming at defining seafloor instability and sediment mass wasting processes that may represent hazard for coastal areas and infrastructures. In this view, a number of national and international research projects have involved the Italian continental margins (COSTA Project, Canals et al. 2004; MALISAR Project, Migeon et al. 2007, MAGIC Project, Chiocci and Ridente, this volume), where the interests for geo-hazard investigation and risk analysis are rooted in the well-known high concentrations of historical and recent natural disasters (Italian Catalogue of Tsunami, Tinti et al. 2004; Lorito et al. 2008). These events are often connected to the intense seismicity (e.g. Ligurian, Calabrian and Sicilian margins) which may influence both the long- and short-term morphodynamic evolution. Moreover, such catastrophic events may be amplified by human activity (e.g. the 1977 Gioia Tauro harbour landslide, Colantoni et al. 1992; the 1979 Nizza harbour landslides, Cochonat et al. 1993). The geographical distribution and frequency of geohazard features indicative of intense erosion and sediment failure along the Italian margins, such as canyons and widespread submarine landslides, have been better constrained with the recent increase of Multibeam swath bathymetry acquisition combined with high resolution seismic data. Detailed 3D reconstructions of surficial and deep-seated morpho-structural settings have improved the identification of marine geo-hazard features, allowing a better comprehension of geomorphic processes resulting in the rapid morpho-dynamic evolution of continental margins. This rapid geomorphic shaping of the seafloor is often related to
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sediment erosion and mass wasting; where these processes cluster and focus, they may lead to the development of canyon systems deeply and diffusely incising the shelf and slope region. Mass wasting processes are often the effect of multiple factors which can variably interplay, making sediment instability one of the most difficult geo-hazard to be evaluated. In many cases the difficulty of predicting geo-hazard related to the complex processes like sediment failure depends also on the scarce availability of spatial and temporal information relative to their occurrence. However, the likelihood of geo-hazards and their possible effects can be inferred from specific geomorphic features (e.g. horseshoe scar, migrating bedforms, accumulation or dispersion of giant blocks) as well as from the stratigraphic record (e.g. debris deposits, hummocky deposits), properly evaluated within the context of known recent and historical events (e.g. earthquakes, inundations, and tsunamis). The Ionian Calabrian margin is one of the most interesting areas for applying the above investigative criteria in order to define the main geomorphic features, their relationship with stratigraphy and seismotectonic setting and, finally, the resulting geo-hazard potential. The Ionian Calabrian margin has been the object of the MESC-05 research Project (Morphology and Evolution of the Submarine Canyons in the Ionian Margin of Calabria- University of Trieste, Italy). In the framework of the MESC-05 project, a survey has been performed on board of the R/V OGS EXPLORA (summer 2005) during which Multi-beam and CHIRP data were acquired, covering the Ionian shelf area and slope up to 1,600 m depth from Capo Spartivento to Capo Rizzuto (Figs. 1, 2).
The collected high resolution swath bathymetry data allowed us to define in detail the main morphological features of the area, confirming the prevalence of the erosional and mass wasting processes, particularly along canyon systems in the slope and within the shelf area. The deeply incised canyon headscarps and channels suggest that erosion and sediment mass wasting may have been accompanied by landslides. These features have been evaluated in terms of geo-hazard potential in the framework of the MaGIC project (Marine Geohazard along the Italian Coasts). The regional seismotectonic setting (Fig. 1) is dominated by the Calabrian arc subduction zone, and is responsible for large historical earthquakes and tsunamis events, as well as for the high uplift rates of 0.8–0.9 mm/ year during the Plio-Quaternary (Ghisetti 1979; Canu and Trincardi 1989; Westaway 1990; Dai Pra et al. 1993; Bordoni and Valensise 1998; Ferranti et al. 2007). Locally, regional uplift was accompanied by extensional and strikeslip tectonics, by which formed ridges and basins also within the offshore, including the study area (e.g. Spartivento and Catanzaro basins; Ambrosetti et al. 1987; Del Ben et al. 2008). This process is one of the main causes for the intense erosion and mass wasting processes in the study area, where the margin is characterized by a very narrow continental shelf and steep slope, frequently incised by canyon systems that backstep landward very close to the modern coast and affect coastal sediment dispersal (Fig. 2; Cuppari et al. 2007; Morelli 2008; Colizza et al. 2008). In particular, sediment is intercepted by canyon headscarps and channels and is directly conveyed into the slope, determining, on one hand, coastal erosion and shoreline
Fig. 1 Structural setting and active tectonics of the Calabrian Arc and surronding area (Ferranti et al. 2007, modified). In a solid black line: Front of the contractional orogen in the Apennines and Sicily; dotted black lines: Depth (km) of the Ionian slab; gray patches bounded by thick dashed lines: Moho Depth (km) in the Tyrrhenian Sea; thin, solid gray lines: Uplift and subsidence rates (mm/year) in
the Late Pleistocene. In b structural setting (Del Ben et al. 2008, modified) seismicity and active tectonics of the Calabrian Arc and of the Ionian margin. The double-arrowed line shows extension direction (Monaco and Tortorici 2000). Focal mechanisms of moderate to large earthquakes (M [ 4) are shown (Ferranti et al. 2007 and references therein)
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Fig. 2 3D view of the surveyed Ionian Calabrian Margin showing the main morphological features of the three sectors of BovalinoSidenno, Squillace Gulf and Stilo Rise. The relationship between the main erosional-gravitational features and the active tectonics of the Cabrian Arc is shown. The red lines indicate the main faults (by
Ambrosetti et al. 1987; Cuppari et al. 2004; Del Ben et al. 2008, modified). The red circles and blue dots show the seismicity (by Italian Seismicity Catalogue, 1981–2002—CSI 1.1, Castello et al. 2007, modified)
retreat, and promoting on the other hand sediment mass wasting (debris and turbidity flows). The regional geomorphic setting is characterized by areas of different concentrations and intensity of these processes, coinciding with different seismo-tectonic activity within three distinct areas: the Squillace Gulf, the Siderno-Bovalino Gulf and the Stilo rise area.
stack of basement nappe and the Meso-Cenozoic sedimentary cover. The accretionary prism, during its SE migration, has involved the Oligocene–Quaternary terrigenous succession deposited in migrating foreland and piggyback basins (Monaco et al. 1996; Patacca et al. 1990; Van Dijk et al. 2000). Since the Late Miocene, the structural evolution and sedimentary succession of the Ionian area are comparable to the typical development and migration of thin-skinned thrust front fore-arc basins, with alternation of compressional and extensional process, often accompanied by strike-slip deformation. The Quaternary extensional phase affecting the Calabrian Arc and the Ionian margin is testified by regional NE–SW normal fault systems and E–W to NW–SE strike-slip fault systems segmenting the Calabrian Arc; these fault systems extend through the Ionian shelf and slope (Figs. 1, 2; Sibari, Squillace Bovalino and Spartivento faults in Del Ben et al. 2008; Van Dijk et al. 2000; Cuppari et al. 2004; Tansi et al. 2007). During the Middle and Upper Pleistocene, the Calabrian coast underwent significant tectonic uplift (Fig. 1; Westaway 1990; Bordoni and Valensise 1998; Ferranti et al. 2007). The regional uplift determined topographic steepness, in turn enhancing erosion and large volume sediment discharge by which mass movements and geomorphic shaping of the margin significantly accelerated. The surficial effects of these processes include topographic steepness with seismogenic normal and strike-slip
Geological setting The study area is located in the Ionian Sea margin of southern Calabria, whose Neogene geological evolution is connected to the growth and SE migration of the Calabrian Arc orogen and accretionary prism (Fig. 1). The prominent arc-shaped orocline connecting the NW–SE trending southern Apennines with the WSW striking Maghrebian trusts belt, is rimmed by the Tyrrhenian and Ionian basins characterized by thinned continental and oceanic crust. According to several Authors, these physiographic and geological units are the result of the Neogene north-westerly subduction and easterly roll-back of the Adriatic– Ionian slab (Malinverno and Ryan 1986; Doglioni et al. 1994; Gueguen et al. 1998; Faccenna et al. 2001; Ferranti et al. 2009 and references therein). Since the Late Oligocene to Early Pleistocene the process has led to the development of a complex contractional belt (Casero et al. 1992; Patacca and Scandone 2001) including a
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Mar Geophys Res Fig. 3 Detailed 3D view of the Bovalino-Siderno area which shows the morphodynamic characters of the canyons and of the slope area (above). Sidescan sonar records show the proximity of the Bovalino Canyon head to the shoreline and to the urban areas (below)
faulting, high persistence of erosion, large volume of sediment discharge and related mass movements. These are the major factors responsible for the rapidly evolving morpho-dynamic features and geo-hazard elements detected in the surveyed area.
Methods Multibeam bathymetry and Chirp sonar seismic data were acquired in the frame of MESC-05 Project, over an area of approximately 6,000 km2, including the continental shelf and slope between Capo Spartivento and Capo Rizzuto (Fig. 2) to a depth of 1,500 m. In addition, multi-channel seismic sections acquired for hydrocarbon exploration have
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been used for investigating the deep-seated tectono-sedimentary structures. Multi-beam data have been collected using Reson 8110 and 8150 devices and then processed with PDS2000; the DTM spatial resolution obtained was of 50 m (Fig. 2). When possible, the interpretation and mapping of geo-hazard features on the multi-beam dataset has been supported by high-resolution (Benthos Chirp II) seismic data. The most proximal reach of canyon heads, which is very close to the coast, could not be covered by multi-beam data; this coastal area, however, has been mapped using side-scan sonar data (Italian Department of the Environment and of the Territory Management. –SI.DI.MAR). Earthquake and tsunami events reported in historical catalogues (Tinti et al. 2004) have been also considered in order to better evaluate the geo-hazard
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potential of the geomorphic features investigated in the study area.
Results Based on seafloor morphology, three different areas can be distinguished on the Ionian Calabrian margin: the Squillace Gulf and the Siderno-Bovalino basin, separated by the Stilo rise (Fig. 2). The former two are characterized by the maximum concentration of erosional and mass wasting features (Figs. 3, 4) and by a narrow shelf (1–5 km) rimmed by a steep (5°–18°) slope, which is incised by canyons, gullies, and landslide scars. Gullies on the upper slope alternate with canyon heads deeply incising the shelf; the lower slope is dominated by fan-shaped deposits. The canyon thalwegs are straight or meandering, locally with sharp deviations, and are formed downslope by the confluence of numerous tributary channels. The frequent occurrence of landslide scars testifies recurrent sediment mass transport and failure, particularly in the canyon heads and along their steep flanks (up to 20°; Figs. 3, 4). Despite the evidence of the frequency and high diffusion of these processes, landslide accumulation bodies at the base of the slope are scarce or absent. In the Stilo rise area the shelf is wider (5–8 km) and the slope is less steep (2°–5°) than in the two former areas. Evidence of sediment erosion and instability is less
frequent and limited to the flanks of the Assi Channel and the surrounding slope area (Fig. 2). The Assi Channel head affects the outermost continental shelf and forms a small valley on the slope with a meandering, locally sharply deviating course (Fig. 4). Based on a more detailed analysis, the narrow shelf (1–2 km; Fig. 3) of the Bovalino-Siderno sector between the canyon heads is characterized by a shelf-break area completely carved by small channel heads responsible for its progressive retreat. The entire slope area is very steep and characterized by small channels and gullies that indicate frequent erosion and large mass transport of sediment. These are also responsible for the deep incisions of the canyons and for occurrence of landslide scars along their flanks. The thalwegs are mostly straight along the steep upper slope and meandering at the base of the Bovalino Canyon, continuing their course across the deep-sea fan area. The Bovalino, Siderno and Caulonia canyon heads are particularly developed and retreated within the shelf, reaching a short distance from the shoreline (20–500 m). Clusters of instrumental seismic epicentres with maximum magnitude 3–4 (Tinti et al. 2007) appear located within the areas of the canyons development, and might testify the recent activity of NW–SE trending regional fault systems (Figs. 2, 3; Ambrosetti et al. 1987; Cuppari et al. 2004; Del Ben et al. 2008). Recent fault activity is confirmed by historical large earthquakes whose devastating effects have also led to major flooding events along the coast a short
Fig. 4 Seafloor morphology of the Squillace Gulf and Stilo rise sectors which shows the main erosional and gravitational processes and geohazard sites of the area (red line) detected
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distance from the canyon heads (e.g. 1784 Roccella event and 1907 Bovalino event; Tinti et al. 2007). In the Gulf of Squillace, one of the most significant geohazard features is represented by the upper portion of the Botricello Canyon (Fig. 4). The canyon head of the main channel is close to the coast, while the secondary channel head is intersecting a forward shelf edge sector. The western flank of this canyon is affected by retrogressive gravitational-erosive processes testified by well evident landslide scars that are progressively reducing the slope area which delimits the canyon from the Serre Channel. The rapidly evolving mass-wasting processes are supported by multi-channel seismic profiles which show deep-seated landslide slip planes and their correspondence with a deep compressive structure (Fig. 5). This finding is consistent with the regional tectonic evolution, which is characterized by the presence of a blind Plio-Quaternary and still active
Fig. 5 3D view of the Serre Channel b and its surficial (Chirp profile; in a) and deep seated structural setting (multichannel seismic section; in c)
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arc-shape compressive front (Fig. 2; Ambrosetti et al. 1987; Del Ben et al. 2008). The historical data of this area show a tsunami event on 8th March 1832 which struck the coastal area from Catanzaro Lido to Steccato village with maximum flooding at Magliacane village for about 900 m, corresponding to the canyon head. The tsunami wave of 20 m height 2 km offshore was triggered by an earthquake with epicentre on land, about 20 km from the coast (Tinti et al. 2007). The Serre Channel presents a fan-shaped head characterized by minor channel with shell-shaped erosion scars which flow in the Catanzaro Canyon (Fig. 4). Chirp and multi-channel seismic profiles suggest a channel head development linked to surficial and deep-seated mass movement which may be favoured by the presence of gas charged sediments (Fig. 5). In the area where the gravitational processes are concentrated, a deep compressive structure, as described for the Botricello Canyon, is present (Fig. 5) and its recent activity is confirmed by a cluster of instrumental seismic epicentres with maximum magnitude 3.4 (Tinti et al. 2007). Moreover the fault planes have likely controlled the upward migration of gas into the younger sedimentary covers (Fig. 5). The Sellia Canyon head is located at depth of 40 m at a distance of 1 km from the shoreline (Fig. 6). The concave-shaped axial profile and the meandering morphology of the thalweg suggest a smaller persistence of the erosional and mass wasting processes than on the other canyons of this area. However, at the confluence with the Squillace Canyon, the canyon thalweg is more straight and carved with very steep flanks (Fig. 4). In this sector the Chirp profiles show evidence of incipient destabilization of significant thickness of sedimentary cover. The Catanzaro Canyon head is subject to evident retrogressive erosion (Fig. 6). The canyon is narrow, straight, directly connected to the mouth of the Corace River, and drains coastal deposits and flood supply (Fig. 7). Its northern flank is marked by many landslide scars and an incipient secondary channel. In this area, where small earthquake epicentres cluster, high resolution seismic profiles show how slope instability may be related to active faults and gas leakage (Fig. 6). Near the coast, the fan-shaped canyon head is at a distance of 50 m from the shoreline along a frontal area of about 3.5 km. The coastal area affected by the head canyon is strongly urbanized, with the presence of the Catanzaro Lido tourist harbour (Fig. 7). The head of Copanello and Soverato Canyons can be described as a single zone of landslide and erosional geohazard (Fig. 4). The head of the canyons reaches the shoreline near Soverato at a distance of 100–200 m, where coastal indentations are conditioned by a master fault outcropping on land. In this area the morpho-dynamic
Mar Geophys Res Fig. 6 Chirp profile (b) of the northern side of the Catanzaro Canyon (a). The area is characterized by mass wasting conditioned by active faults and fluid escape (disruption of the layering). The Chirp profile and 3D view (in c) show an inferred mud volcano feature
processes are amplified and the area is characterized by both potential submarine landslides and destabilization of the coastal zone. In this situation gravitational processes can simultaneously affect the coast and the seabed. The Assi Channel head is strongly conditioned by scars that characterize the southern side of the Stilo Rise. This situation can be classified as a slow gravity mass flow (Fig. 8). The channel head interests only the outermost shelf edge at a distance of 4–5 km from the Assi river mouth. In the shelf area the seabed morphology shows scarce morpho-dynamic evidence of direct and recent
interaction between the Fiumara Assi river sediment discharge events and the channel head erosional processes. Nevertheless the two areas are linked by a gentle seabed scarp coinciding with a WNW–ESE trending and NNE dipping normal fault which displaces the Holocene deposits (Fig. 8). The head morpho-dynamic characters and the location suggest that its main development is attributable to the Last Glacial Maximum (*25–16 ka). The recent erosional and mass-wasting features are likely induced by the flank channel steepness.
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Fig. 7 Side-scan sonar records of the head of Catanzaro Canyon which show its proximity to the coastal area and to the tourist harbour
Discussion The different morphological character of the three sectors described above reflect, to some extent, the effect of the regional uplift and active tectonics on the morphodynamic
evolution of the Ionian Sea margin of Calabria. Distribution of mass wasting and erosional features, as well as the main canyon heads, coincide with fault systems and tectonic lineaments dissecting the Calabrian Arc (Fig. 2), and are located near the coastal infrastructures. In terms of potential geo-hazard, these coastal areas are exposed to retrogressive erosion of the canyon headscarps yielding sediment mass-wasting and failure, both on the shelf edge, where sediment loading is significant, and on the steep slope and canyon flanks; slope failure is also associated with gas-charged sediment and shallow faults dissecting Pleistocene and Holocene deposits. The absence of significant landslide accumulations at the base of the slopes suggests that the sediment failure mainly occurred as small-scale processes in form of frequent and diffused debris flows (grain/mud flows) evolving downslope into turbidity flows, rather than as large-scale landslides (debris avalanches). Nevertheless, it is also possible that larger landslide deposits may have been reworked and/or transported at greater distance (McAdoo et al. 2000; De Blasio et al. 2006). An example of very large slope failure is recorded in the area between the two canyons of Bovalino and Siderno, where the widespread retrogressive erosional and gravitational processes have reduced the shelf to a narrow sublittoral zone (Fig. 3). Relative to such events, it is still a matter of debate whether seismicity may have contributed to slope instability and whether instability progressed
Fig. 8 3D view of the head of Assi Channel which affects the shelf edge. In the shelf area Chirp profiles show the presence of active faults that displace the base of the Holocene section
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Fig. 9 3D view diagram of the Ionian Calabrian Margin showing the relationship between its seismotectonic setting, the main erosionalgravitational features (canyon heads), historical tsunami (red star) and related earthquake epicentres (Tinti et al. 2004)
through frequent and small events or less frequent but larger submarine landslides. The hypothesis that large landslides are responsible for the collapse of a shelf area portion must be better evaluated. In particular, further investigation is required in order to constrain the cause-and-effect relationship between historical earthquakes, large submarine landslides, and historical tsunamis which affected the coastal areas (e.g. 1784 Roccella event and 1907 Bovalino event; Fig. 9). Defining such relationships would significantly increase the evaluation of the potential geo-hazard and related risk along the studied margin. Nonetheless, the most critical geo-hazard situation is represented by the active retrogressive development of the Bovalino, Siderno and Caulonia canyon heads. Their proximity to the coastline (20–500 m) causes the instability and capture of coastal sediments (Fig. 3). Analogous situations have been recognized in other areas of the Gulf of Squillace at the heads of the canyons of Botricello, Serre, Sellia, Copanello, Soverato and in the most extreme conditions, near the Catanzaro Lido Harbour (Catanzaro Canyon; Figs. 4, 5, 6, 7). In the same areas, based on the available data, the presence of active faults may allow us to hypothesize a possible relationship between recent fault activity and the focussing of erosional and gravitational processes responsible for the channels and canyons’ development. Despite this evident correlation only further investigations, specifically regarding the individual most critical geo-hazard situations, will verify the consistency of this hypothesis. Based on the small development of the head and its great distance from the coast, the Assi channel area can be
classified as a low geo-hazard feature. However, the area must be better analyzed by further investigation focused on the recent fault activity (Holocene; Fig. 8). A detailed evaluation should be carried out to estimate the faults capability of producing significant earthquakes or triggering tsunami events like those reported to be present in the local historical record (Fig. 9; Sea rise at Stilo in 1783; Tinti et al. 2007).
Conclusions The interpretation of detailed swath bathymetry, Chirp sonar and side-scan sonar data shows that the Calabrian Ionian margin between Capo Spartivento and Capo Rizzuto can be divided into the following three sectors undergoing rapid though different geomorphic evolution: the BovalinoSiderno, the Stilo rise and the Gulf of Squillace sectors. These sectors are characterized by a different morphostructural setting, but all evidence several geo-hazard features. In particular, several canyon systems characterized by well developed heads provide evidence of retrogressive erosion and sediment failure. The vicinity of the canyon heads to the shoreline causes the coastal transport to be intercepted and sediment supplied by rivers is in greater part conveyed directly to the slope, with the consequence of enhancing shoreline erosion in areas settled by infrastructures. Mass-wasting processes also affect the steep flanks of canyons and of their tributary channels. The absence of landslide deposits along the canyon thalwegs and at the base of the slope indicates the persistence of erosional processes strongly controlled by frequent
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turbidity flows, or dynamic processes as disintegrative mass failure associated with large submarine landslides. The focusing and development of these processes could be mostly conditioned by the margin structural setting and influenced by the activity of the offshore extent of fault systems known on land. The offshore extent of these systems frequently coincides with the main canyon heads and small channels (Assi Channel) on the margin. In many cases, mass-wasting processes may be favoured by the presence of gas charged sediment, along the flanks of canyons, as evidenced by seismic data. An interesting aspect put in evidence by the correlation between the known historical tsunami events and the described marine geo-hazard features, is the reduced distance of the latter from the coastal zones that were damaged (Fig. 9). This distance in many cases turns out to be less than the distance of the related earthquake epicentre. Based on this evidence one can surmise that the tsunamis have been generated by large submarine landslides triggered by repeated earthquake loading. This hypothesis is only partially supported by the frequency of landslide scars and widespread mass movements described, and requires further investigation aimed at defining the volume and velocity of the failed deposit, as well as their age in order to verify the consistency with the occurrence of known historical earthquakes. A similar, more complete analysis would allow to better address geo-hazard evaluation and risk assessment relative to earthquake triggering of landslides and landslide-generated tsunamis in the studied area. Acknowledgments This work was supported by University of Trieste (Department of GeoSciences; Resp. F. Fanucci and E. Colizza). We are grateful to the support of Project MaGIC (Marine Geohazard along the Italian Coasts; Resp. F.L. Chiocci) funded by the Italian Civil Protection Department and coordinated by the Institute of Environmental Geology and Geoengineering of the Italian National Research Council (IGAG-CNR). The marine geophysical data were acquired in the framework of the MESC-05 project (Morphology and Evolution of the Submarine Canyons in the Ionian Margin of Calabria; Resp. E. Colizza), on board of the R/V OGS-EXPLORA and supported by the Department for the Development of Marine Technology and Research of the Osservatorio Geofisico Sperimentale (Trieste; Resp. R. Ramella). The Side-Scan Sonar data were collected by the Italian Department of the Environment and of the Territory Management. (SI.DI.MAR). L. Ferranti (University of Naples— FedericoII) is thanked for his helpful suggestions. We are also grateful to D. Ridente (IGAG-CNR) and of an anonymous reviewer for their careful review and to F.L. Chiocci for editorial guidance.
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