The Coastal Areas of the Bay of Naples: The Sedimentary Dynamics and Geological Evolution of the Naples Canyons

Abstract

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.

Marine Geohazards of the Bay of Naples (Southern Tyrrhenian Sea, Italy): A Review Integrating Morpho-Bathymetric and Seismo-Stratigraphic Analysis

“…During the late Quaternary, submarine slides mainly involved both the canyon's heads, being double regressive (Dohrn) and triple regressive (Magnaghi). In this area, the geological evolution of submarine slides has been explained according to the three-stage model of Pratson and Coakley [42] for submarine canyon evolution [43]. This approach is centered on the modification of the slope failures in a canyon with a retreating head, receding upward on the slope along the pre-canyon channels, as dictated by the retrogressive slides modulated by strong volcaniclastic input.…”

“…The second phase, corresponding to the canyon development through slope failures, happened later than 15 ky B.P. (eruption of the Neapolitan Yellow Tuff) [43]. The third stage, corresponding to the individuation of the canyon retrogressive heads, is older than the growth of the Nisida volcanic bank (Naples offshore), physically interrupting the Dohrn western branch (4.8-3.8 ky B.P.)…”

“…The third stage, corresponding to the individuation of the canyon retrogressive heads, is older than the growth of the Nisida volcanic bank (Naples offshore), physically interrupting the Dohrn western branch (4.8-3.8 ky B.P.) [43]. Figure 4 shows the high-slope map of Naples Bay, which was previously constructed [24], identifying the areas prone to slide, which are those having gradients greater than 10 • .…”

“…In the proximal areas, the tephra deposits consist of coarse-to-medium-grained sands and gravels. In the distal areas, it consists of sandy silts with fine-grained lithic and bioclastic components [43,[51][52][53] (Figure 6). In the Bay of Naples, marine tephra deposits have constrained the eruption magnitude and frequency in the area, as well as the distribution of pyroclastic deposits associated with the most recent activity of Vesuvius [51][52][53], thereby improving the knowledge on marine hazards.…”

“…In the proximal areas, the tephra deposits consist of coarse-to-medium-grained sands and gravels. In the distal areas, it consists of sandy silts with fine-grained lithic and bioclastic components [43,[51][52][53] (Figure 6). [43].…”