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![Structural map of the Bay of Naples displaying fault geometry, fault kinematics and folds [see also the location of the presumed Campi Flegrei calderas (dashed lines): the smaller one as supposed by Rosi and Sbrana (1987); the larger one as suggested by Orsi et al. (1996)]. The enlargement shows details of volcanoes and faults in the northern Naples Bay. T1-T6 indicate the relative chronology of volcanism (from older to younger): T1-Gaia Bank, Pia Bank and southern part of Penta Palummo volcanoes; T2-Miseno Bank and northern Penta Palummo volcanoes; T3-magmatic intrusion north of Penta Palummo; T4-Neapolitan Yellow Tuff; T5Nisida Complex volcanoes; T6-Monte Dolce Bank volcano and tuff cones off Capo Miseno](profile/Alfonsa-Milia/publication/227292973/figure/fig3/AS:651500023975937@1532341118135/Structural-map-of-the-Bay-of-Naples-displaying-fault-geometry-fault-kinematics-and-folds.png)
Structural map of the Bay of Naples displaying fault geometry, fault kinematics and folds [see also the location of the presumed Campi Flegrei calderas (dashed lines): the smaller one as supposed by Rosi and Sbrana (1987); the larger one as suggested by Orsi et al. (1996)]. The enlargement shows details of volcanoes and faults in the northern Naples Bay. T1-T6 indicate the relative chronology of volcanism (from older to younger): T1-Gaia Bank, Pia Bank and southern part of Penta Palummo volcanoes; T2-Miseno Bank and northern Penta Palummo volcanoes; T3-magmatic intrusion north of Penta Palummo; T4-Neapolitan Yellow Tuff; T5Nisida Complex volcanoes; T6-Monte Dolce Bank volcano and tuff cones off Capo Miseno
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The Campanian continental margin is characterised by asymmetric half grabens and large-volume volcanic deposits. Vesuvius and Campi Flegrei are active volcanoes located along the coast of Naples Bay along one of these half grabens. The interpretation of an extensive set of seismic reflection data allowed to reconstruct the stratigraphy and structur...
Contexts in source publication
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... southern sector of Naples Bay west of Capri has a narrow continental shelf and an upper slope dipping towards the north-west. In the central sector the con- tinental shelf is about 20 km wide (Fig. 3A), the upper slope has an average gra- dient of 3 and dips towards the west-northwest. In the middle of the Bay of Naples between Capri and Ischia a NE-trending structural high, known as Banco di Fuori, is present. This asymmetrical ridge is bounded at the south-eastern slope by normal faults (Fig. ...
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... main structural features of the Bay of Naples are NE-SW normal faults, NW- SE oblique faults, E-W left-lateral faults and folds (Fig. 3). The detailed strati- graphic analysis and the inferred age of the stratigraphic units displaced by the faults allowed the evaluation of fault slip ...
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... NW-SE fault bounds the north-eastern side of the Ammontatura depression (Fig. 3) and an igneous dike is present close to this fault (Fig. 6). Another NW- SE fault located south of Nisida down-throws a volcanic mound by 13 m (Fig. 6). As the fault scarp affects the volcanic unit corresponding to the 10-8 Ka old Nisida Complex, the resulting vertical slip rate ranges between 1.6 and 1.3 mm=yr. The above mentioned ...
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... affects the volcanic unit corresponding to the 10-8 Ka old Nisida Complex, the resulting vertical slip rate ranges between 1.6 and 1.3 mm=yr. The above mentioned fault ends in the Monte Dolce Bank formed by recent lava extrusions ). The NW-trending faults of Ammontatura and Nisida Bank continue north-westward into Pozzuoli Bay (dashed-lines in Fig. 3) as evidenced by right-lateral fault segments mapped near Pozzuoli ( ) and NW-trending self-potential isolines (Di Maio et al., 2000). Although faults are in the Pozzuoli Bay locally buried by younger marine deposits, they must be considered as active structures because they dis- place the sea floors offshore ...
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... mentioned above, folds and uplift zone are also present in Naples Bay. The erosional surface on the margin of the continental shelf (Fig. 3) marks a NW-SE uplift area during the emplacement of the Campanian Ignimbrite (Milia, 2000). In Pozzuoli Bay two anticlines and an intervening syncline have been identified: the syncline controls the physiography of the deepest part of the bay, the northern anticline extends along the coast of Pozzuoli (Fig. 3). The folding began 8 Ka ...
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... the margin of the continental shelf (Fig. 3) marks a NW-SE uplift area during the emplacement of the Campanian Ignimbrite (Milia, 2000). In Pozzuoli Bay two anticlines and an intervening syncline have been identified: the syncline controls the physiography of the deepest part of the bay, the northern anticline extends along the coast of Pozzuoli (Fig. 3). The folding began 8 Ka ago and calculated uplift rates are up to 20 mm=yr ...
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... ''the Central shelf block'', ''the Campi Flegrei block'', ''the Procida block'' and ''the Slope block''. The central basin, located in the northern part of the bay, was the site of intense extension and volcanism; it corresponds to the Ammontatura depression and to a triangle-shaped zone in the Penta Palummo area. Notably, in Penta Palummo area (Fig. 3), volca- nism started in the southern banks and corresponds to the Gaia Bank and Pia Bank volcanoes (T1). With time the volcanic center migrated northwards reaching Pozzuoli Bay when the Neapolitan Yellow Tuff (T4) was erupted. Dikes (T3 in Fig. 3) are aligned along NE-SW and NW-SE trending faults. Sites of intense volcanism related to ...
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... depression and to a triangle-shaped zone in the Penta Palummo area. Notably, in Penta Palummo area (Fig. 3), volca- nism started in the southern banks and corresponds to the Gaia Bank and Pia Bank volcanoes (T1). With time the volcanic center migrated northwards reaching Pozzuoli Bay when the Neapolitan Yellow Tuff (T4) was erupted. Dikes (T3 in Fig. 3) are aligned along NE-SW and NW-SE trending faults. Sites of intense volcanism related to local extension are located at the southwestern to southern margin of ''the Campi Flegrei block'' where vents of the Neapolitan Yellow Tuff are aligned and at the boundary to the ''Central shelf block'' that corresponds to the NW-trending fault ...
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Citations
... On the other hand, [29] showed that an additional NE trending normal fault system and a WNW-ESE directed fold system were active in the Late Qua ternary. ...
Vesuvio is likely the most if not one of the most dangerous volcanoes in the world. It is an active volcano, quiescent since 1944. The activity of the Monte Somma and Vesuvio volcanic complex is commonly referred to as two central volcanic edifices, namely Monte Somma and Vesuvio. Nevertheless, the opening of numerous eruptive fissures and related vents have characterized Monte Somma and Vesuvio throughout their lives. Spatter cones, spatter ramparts, and related eruptive fissures are disseminated downslope of Vesuvio’s main cone and on the southern slopes of the volcano. Similarly, cinder cones, spatter cones, and welded spatters are distributed in the sequence cropping out on the Monte Somma cliff and on the northern slopes of Monte Somma. In this work, a total of 168 eruptive vents have been identified and characterized in a GIS environment in which field data have been merged with relevant information from historical maps and documents. These vents have been arranged into units bounded by unconformities (Unconformity Bounded Stratigraphic Units) defining the eruptive history of the volcano. Alignments of vents and eruptive fissures within each unit have been compared with regional tectonic elements and the volcano-tectonic features affecting Monte Somma and Vesuvio during the last 5600 years, thus inferring that different structural trends were active in the different stratigraphic units. In particular, we show that the N300°–320° regional, Apennine, left-lateral, strike-slip fault system, the N040°–055° Torre del Greco direct fault system, the N70° and the EW fault system, and the generally NS oriented group of local brittle elements, all analyzed here, were differently active during the investigated time span. These tectonic trends might control the position of the eruptive fissures and vents in case of future unrest of the volcano.
... In western Naples Bay, the volcanic districts of the Procida, Vivara, and Ischia islands pertain to the Campi Flegrei volcanic district, including a number of submerged volcanoes [32,36,[82][83][84][85]. This volcanic activity has controlled the formation and activity of the western branch of the Dohrn canyon and of the Magnaghi canyon, which drained the volcaniclastic input of the continental slope during the major eruptive phases. ...
... The coastal plain of the Sebeto river, on which the eastern part of the town of Naples lies, is located at the boundary of the Somma-Vesuvius volcanic complex and towards the Tyrrhenian coastline. The individuation of this plain has been triggered by a NE-SWtrending (counter Apenninic) normal fault, corresponding to the Acerra-Dohrn canyon fault (Figure 1), active after the eruption of the Campanian Ignimbrite and of the Neapolitan Yellow Tuff at 39 and 15 ky B.P., respectively [5,6,[83][84][85][86][87][88]. ...
The sedimentary dynamics and geological evolution of the Naples canyons during the Late Quaternary have been studied based on sedimentological and seismo-stratigraphic data. Several factors, including the sedimentary environments, tectonic setting, and volcanic eruptions, have controlled the geological evolution of the coastal and marine areas of the Bay of Naples. The main data and methods include the sedimentological data analysis, the seismo-stratigraphic techniques
applied in the geological interpretation of seismic profiles, and the integrated analysis of core data that were previously published. The formation of the Dohrn canyon is controlled by fluvial processes, active in correspondence with the palaeo-Schiazzano River system and by the main eruptive events involving the submarine portion of Naples Bay, including the Campanian Ignimbrite (CI; 39 ky B.P.) and the Neapolitan Yellow Tuff (NYT; 15 ky B.P.). The formation of the Magnaghi
canyon is controlled by erosional processes on the continental slope of Procida Island, which was active during the last eruptive phases of the island (Solchiaro Formation; 18 ky B.P.), triggering high rates of volcaniclastic supply.
... In western Naples Bay, the volcanic districts of the Procida, Vivara, and Ischia islands pertain to the Campi Flegrei volcanic district, including a number of submerged volcanoes [32,36,[82][83][84][85]. This volcanic activity has controlled the formation and activity of the western branch of the Dohrn canyon and of the Magnaghi canyon, which drained the volcaniclastic input of the continental slope during the major eruptive phases. ...
... The coastal plain of the Sebeto river, on which the eastern part of the town of Naples lies, is located at the boundary of the Somma-Vesuvius volcanic complex and towards the Tyrrhenian coastline. The individuation of this plain has been triggered by a NE-SWtrending (counter Apenninic) normal fault, corresponding to the Acerra-Dohrn canyon fault (Figure 1), active after the eruption of the Campanian Ignimbrite and of the Neapolitan Yellow Tuff at 39 and 15 ky B.P., respectively [5,6,[83][84][85][86][87][88]. ...
The sedimentary dynamics and geological evolution of the Naples canyons during the Late Quaternary have been studied based on sedimentological and seismo-stratigraphic data. Several factors, including the sedimentary environments, tectonic setting, and volcanic eruptions, have controlled the geological evolution of the coastal and marine areas of the Bay of Naples. The main data and methods include the sedimentological data analysis, the seismo-stratigraphic techniques applied in the geological interpretation of seismic profiles, and the integrated analysis of core data that were previously published. The formation of the Dohrn canyon is controlled by fluvial processes, active in correspondence with the palaeo-Schiazzano River system and by the main eruptive events involving the submarine portion of Naples Bay, including the Campanian Ignimbrite (CI; 39 ky B.P.) and the Neapolitan Yellow Tuff (NYT; 15 ky B.P.). The formation of the Magnaghi canyon is controlled by erosional processes on the continental slope of Procida Island, which was active during the last eruptive phases of the island (Solchiaro Formation; 18 ky B.P.), triggering high rates of volcaniclastic supply.
... The CF depression is widely interpreted as that of a caldera, although a few authors deny the existence of the caldera (e.g., Milia and Torrente 2003;Milia et al. 2006). Various hypotheses have been proposed on the genesis and architecture of the CFc. ...
... The deeper part of the anomaly (beneath 700 m, with Vp > 3,500 m/s) correlates with rock sequences made up of agglomerate tuffs and interbedded lavas (AGIP 1987), which form the southern edge of the caldera (Barberi et al. 1991;. The shallower part of the anomaly that tends to split into two parallel arcs is correlated with dikes, volcanic mounds and hydrothermal alteration zones (De Bonitatibus et al. 1970;Pescatore et al. 1984;Milia and Torrente 2003). The presence of these structures suggests the existence of a highly fractured area, through which fluids (mainly gases) may have been able to rise towards the surface. ...
We present a comprehensive review of seismic and gravity observations and tomographic models produced over the past four decades in order to understand the structure of the crust beneath the Campi Flegrei caldera. We describe the main lithological and structural discontinuities defined through these observations, illustrate their geophysical responses, and discuss the constraints they give to the understanding of magmatic and volcanic processes. Micro-seismic crises related to caldera unrest, and ambient seismic noise measurements provide comprehensive seismic data to local earthquake and ambient noise tomography. In combination with reflection data from onshore and offshore active seismic experiments, velocity tomography reconstructs the elastic properties of the caldera between surface and ~4 km depth. Active experiments also define the depth of lithological interfaces and deep (~7.5 km) partially molten bodies. Seismic attenuation tomography provides information complementary to velocity tomography, defining lateral lithological changes and the geometry of onshore and offshore fluid and magma bodies down to 4 km depth. Once compared with seismic analyses, gravity data highlight lateral changes in the offshore caldera structures. During the deformation and seismo-geochemical unrest (1982–1984), they permitted to reconstruct a minor (<1 km lateral extent) melt volume related to the point of maximum uplift measured at the caldera. Seismic coda-wave amplitude inversions depict the caldera rim limits in analogy to velocity tomography and map the lateral extension of ~4-km-deep deformation source. Once combined with the results from velocity tomography and gravity inversions, they reconstruct the feeding systems that connect deep deformation source and shallow vents across the eastern caldera, capped by a seismic horizon around a depth of 2 km.
... This procedure, coupled with the high-precision marine weather forecasting, provided by the network in the Gulf of Naples belonging to the University of Naples "Parthenope", might be intended as a tool for civil protection and coastal damage prevention purposes. The approach proposed in this study can be efficiently used to define the level of sensitivity of urbanized coasts to storms (Williams et al., 2018;Molina et al., 2019Molina et al., , 2020. ...
... The structure of the Gulf of Naples is controlled by numerous Quaternary fault systems, NE-SW trending and SE-dipping, and NW-SE trending and SW dipping, linked to the last stages of the opening of the Tyrrhenian Sea (Fedele et al., 2015;Milia, 2010). Between the Middle and Upper Pleistocene, the fault systems were responsible for the development of the half-graben of the Gulf of Naples and Sorrento Peninsula fault block ridge (Milia and Torrente, 2003). The landscape of this area is strongly influenced by the presence of two active volcanos: the Campi Flegrei poly-caldera in the west and the Vesuvius stratovolcano in the east ( Fig. 1), which interfered with its Late Pleistocene-Holocene evolution (Iannace et al., 2015;Isaia et al., 2018;Santacroce et al., 2003). ...
Destructive marine storms bring large waves and unusually high surges of water to coastal areas, resulting in significant damages and economic loss. This study analyses the characteristics of a destructive marine storm on the strongly inhabited coastal area of Gulf of Naples, along the Italian coasts of the Tyrrhenian Sea. This is highly vulnerable to marine storms due to the accelerated relative sea level rise trend and the increased anthropogenic impact on the coastal area. The marine storm, which occurred on 28 December 2020, was analyzed through an unstructured wind–wave coupled model that takes into account the main marine weather components of the coastal setup. The model, validated with in situ data, allowed the establishment of threshold values for the most significant marine and atmospheric parameters (i.e., wind intensity and duration) beyond which an event can produce destructive effects. Finally, a first assessment of the return period of this event was evaluated using local press reports on damage to urban furniture and port infrastructures.
... The internal part of the Adriatic plate has been affected by a longitudinal compression, as suggested by the main features of the Middle Adriatic Ridge (e.g., [8,228,230]); -Quaternary magmatic activity in the Apennine belt involved two major volcanic episodes (Roman and Campanian provinces, [208,231]), associated with transtensional faulting ( [232,233]). - ...
Tectonic activity in the Mediterranean area (involving migrations of old orogenic belts, formation of basins and building of orogenic systems) has been determined by the convergence of the confining plates (Nubia, Arabia and Eurasia). Such convergence has been mainly accommodated by the consumption of oceanic and thinned continental domains, triggered by the lateral escapes of orogenic wedges. Here, we argue that the implications of the above basic concepts can allow plausible explanations for the very complex time-space distribution of tectonic processes in the study area, with particular regard to the development of Trench-Arc-Back Arc systems. In the late Oligocene and lower–middle Miocene, the consumption of the eastern Alpine Tethys oceanic domain was caused by the eastward to SE ward migration/bending of the Alpine–Iberian belt, driven by the Nubia–Eurasia convergence. The crustal stretching that developed in the wake of that migrating Arc led to formation of the Balearic basin, whereas accretionary activity along the trench zone formed the Apennine belt. Since the collision of the Anatolian–Aegean–Pelagonian system (extruding westward in response to the indentation of the Arabian promontory) with the Nubia-Adriatic continental domain, around the late Miocene–early Pliocene, the tectonic setting in the central Mediterranean area underwent a major reorganization, aimed at activating a less rested shortening pattern, which led to the consumption of the remnant oceanic and thinned continental domains in the central Mediterranean area.
... On the Campania-Latium continental margin, sedimentary basins perpendicular to the chain occur in correspondence with NE-SW trending normal faults [43][44][45][46][47][48][49]. Their tectonostratigraphic setting has been investigated based on both field geological survey [48][49][50] and onshore and offshore seismic data [43,47,[51][52][53][54]. ...
This study discusses the siliciclastic to bioclastic deposits (in particular, the rhodolith
deposits) in the Gulf of Naples based on sedimentological and seismo-stratigraphic data. The selected areas are offshore Ischia Island (offshore Casamicciola, Ischia Channel), where a dense network of sea-bottom samples has been collected, coupled with Sparker Multi-tip seismic lines, and offshore Procida–Pozzuoli (Procida Channel), where sea-bottom samples are available, in addition to Sparker seismic profiles. The basic methods applied in this research include sedimentological analysis, processing sedimentological data, and assessing seismo-stratigraphic criteria and techniques.
In the Gulf of Naples, and particularly offshore Ischia, bioclastic sedimentation has been controlled by seafloor topography coupled with the oceanographic setting. Wide seismo-stratigraphic units include the bioclastic deposits in their uppermost part. Offshore Procida–Pozzuoli, siliciclastic deposits appear to prevail, coupled with pyroclastic units, and no significant bioclastic or rhodolith deposits have been outlined based on sedimentological and seismo-stratigraphic data. The occurrence of mixed siliciclastic–carbonate depositional systems is highlighted in this section of the Gulf of Naples
based on the obtained results, which can be compared with similar systems recognized in the central Tyrrhenian Sea (Pontine Islands).
... Inflation events are accompanied by seismic crises that define a spatially fixed seismogenic volume during unrest with a circular shape (radius~6 km) around the town of Pozzuoli, where the greatest uplift is observed. The magnitude of the uplift and seismicity both decrease in intensity toward the margins of the circular uplift region [5][6][7][8][9][10][11]. [17]; Milia and Torrente [18]). (c) Structural sketch map of CF caldera: (1) sector deformed during caldera collapse; (2) undeformed to subsiding portion of the caldera floor; (3) eastern sector of the resurgent portion of the caldera floor; (4) western sector of the resurgent portion of the caldera floor; red lines = regional faults activated during caldera collapse; yellow lines = regional faults reactivated during resurgence of a portion of the caldera floor; white lines = regional faults reactivated during subsidence of a portion of the caldera floor (modified from Capuano et al. [96]). ...
... In the CF caldera area, a compressional tectonic regime is active, with an anticline culminating near the town of Pozzuoli and a syncline located beneath Pozzuoli Bay (Figure 1(b)). The rate of fold uplift ranges from 1 to 20 mm/yr [15][16][17][18][19]. Other studies (e.g., [20]) generally report an extensional tectonic regime without going into much detail in the area within the caldera. ...
Several recent models that have been put forth to explain bradyseism at Campi Flegrei (CF), Italy, are discussed. Data obtained during long-term monitoring of the CF volcanic district has led to the development of a model based on lithological-structural and stratigraphic features that produce anisotropic and heterogeneous permeability features showing large variations both horizontally and vertically; these data are inconsistent with a model in which bradyseism is driven exclusively by shallow magmatic intrusions. CF bradyseism events are driven by cyclical magmatic-hydrothermal activity. Bradyseism events are characterized by cyclical, constant invariant signals repeating over time, such as area deformation along with a spatially well-defined seismogenic volume. These similarities have been defined as “bradyseism signatures” that allow us to relate the bradyseism with impending eruption precursors. Bradyseism is governed by an impermeable shallow layer (B-layer), which is the cap of an anticlinal geological structure culminating at Pozzuoli, where maximum uplift is recorded. This B-layer acts as a throttling valve between the upper aquifer and the deeper hydrothermal system that experiences short (1-10² yr) timescale fluctuations between lithostatic/hydrostatic pressure. The hydrothermal system also communicates episodically with a cooling and quasi-steady-state long timescale (10³-10⁴ yr) magmatic system enclosed by an impermeable carapace (A layer). Connectivity between hydrostatic and lithostatic reservoirs is episodically turned on and off causing alternatively subsidence (when the systems are connected) or uplift (when the systems are disconnected), depending on whether permeability by fractures is established or not. Earthquake swarms are the manifestation of hydrofracturing which allows fluid expansion; this same process promotes silica precipitation that seals cracks and serves to isolate the two reservoirs. Faults and fractures promote outgassing and reduce the vertical uplift rate depending on fluid pressure gradients and spatial and temporal variations in the permeability field. The miniuplift episodes also show “bradyseism signatures” and are well explained in the context of the short timescale process.
1. Introduction
About a billion people, roughly 15% of the world population, live in areas of volcanic risk because many population centers developed around dormant volcanoes that have not erupted in recent years. The Neapolitan volcanic area is one such high volcanic risk area [1], with about three million people living within an area with a radius of ~25 km in a volcanic province that includes active volcanoes such as Vesuvius, Campi Flegrei (CF), and Ischia [2] (Figure 1(a)).
(a)
... In this paper, the marine geological maps have allowed to show the depositional environments occurring offshore of the Cilento Promontory and to interpret these environments in terms of system tracts of the Late Quaternary depositional sequence [41][42][43]. Moreover, the sedimentological data of sea bottom samples have been analyzed in order to show the main grain sizes occurring at the sea bottom in this portion of the Cilento offshore. ...
The depositional environments offshore of the Cilento Promontory have been reconstructed based on the geological studies performed in the frame of the marine geological mapping of the geological sheet n. 502 "Agropoli". The littoral environment (toe-of-coastal cliff deposits and submerged beach deposits), the inner continental shelf environment (inner shelf deposits and bio-clastic deposits), the outer continental shelf environment (outer shelf deposits and bioclastic deposits), the lowstand system tract and the Pleistocene relict marine units have been singled out. The littoral, inner shelf and outer shelf environments have been interpreted as the highstand system tract of the Late Quaternary depositional sequence. This sequence overlies the Cenozoic substra-tum (ssi unit), composed of Cenozoic siliciclastic rocks, genetically related with the Cilento Flysch. On the inner shelf four main seismo-stratigraphic units, overlying the undifferentiated acoustic basement have been recognized based on the geological interpretation of seismic profiles. On the outer shelf, palimpsest deposits of emerged to submerged beach and forming elongated dunes have been recognized on sub-bottom profiles and calibrated with gravity core data collected in previous papers. The sedimentological analysis of sea bottom samples has shown the occurrence of several grain sizes occurring in this portion of the Cilento offshore.
... Volcanic rocks of Ischia have mainly trachytic-phonolytic compositions, whereas trachybasalts and shoshonites characterize only a few deposits (Poli et al., 1987;Civetta et al., 1991;Vezzoli, 1988;Sbrana and Toccacelli, 2011). Rolandi (1976), Milia and Torrente (2003, 2020), De Alteris et al. (2006, Milia et al. (2006), Milia (2010) and Torrente et al. (2010). B. Geological map of Ischia Island (http://www.napoliunplugged.com/ ...
The correlation between onshore and offshore of the volcanic features in a complex volcanic field area is a difficult
task, however, it is a fundamental step in order to better understand the geological evolution of such a complex
area and for an assessment of geologic hazards.
Ischia is a well exposed and densely populated volcanic field located in the Campania volcanic province of Italy. In
order to improve our understanding of the recent volcanic history of Ischia Island, high-resolution seismic reflection
profiles were used to identify volcanic and sedimentary features in the northern offshore.
The volcano stratigraphy interpretation permitted us to recognize seismic units with a reflection-free/chaotic facies.
These latter units have been associated with volcanic deposits and correlated to the main volcanic units outcropping
on the northern coast of Ischia Island. They are limited in extent and interlayered with eight seismic
units with continuous reflectors corresponding to clastic sedimentary units that were deposited during intereruptive
phases. The main result of this work is the documentation of volcanic activity during the Holocene in
the area offshore between Castello d'Ischia, Ischia Porto (mainly effusive products) and Punta della Scrofa
(mainly shallow lava domes and dykes). The key volcanic units were mapped and 3D geological models were reconstructed.
The reconstruction of the stratigraphic framework offshore a volcanic coast provides a pathway to
the investigation of the stratigraphic relationships between inter-eruptive sedimentary deposits and volcanic
units, and permits the assessment of a wide and continuous chronostratigraphic framework in a complex area.
Furthermore, the onshore-offshore correlation of the main Holocene volcanic units allows us to better estimate
their areal distribution, a critical factor in the hazard evaluation of a coastal volcanic area. The application of seismic
volcano stratigraphy illustrates the remarkable possibilities that the study of submarine volcanic fields offers.
