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The stratigraphic position and lithology confirm their attribution to the 1631 primary and secondary (lahars) deposits. Figure C2Nola (Pollena) lahar deposits overlain by a cultivated paleosol and by the 1631 ash fallout and lahars. 17 and 18 represent minimum local values of the flow velocity and dynamic pressure, respectively, useful to assess some minimum impact of the lahars in the alluvial plain. According to Rodolfo (2000), Sulpizio et al. (2006), and Vallance and Iverson (2015), volcaniclastic mass flows can be generated at variably long time intervals, spanning from eruptive to post-eruptive phases of tens to hundreds of years. Usually, post-eruptive lahars are not accounted for in the assessment of volcanic hazard, although their study is important for hydrogeological hazard assessment and long-term territorial planning. It is possible to evaluate the effects of the lahars on building in the Roman Villa di Lauro, at Taurano, where a 70 cm thick fallout is overlain, without paleosol, by syn-eruptive lahars which engulfed and transported pieces of walls, bricks, and potteries.
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10 and 11 we show a significantly larger distribution area, particularly toward the north (Somma–Vesuvius ramps and plain) and east (Apennines valleys), and less toward the southeast. In particular, this distribution is well-explained by the wide distribution of the ash fallout deposit toward both north and northeast (Fig. 6), remobilized during the lahar generation from both the Mount Somma and Apennine slopes. On the other hand, looking at the average deposit thicknesses, they reach half a meter in the north and northeast, while they reach a couple of meters in some locations in the northeast (aligned with the dispersion axis of the primary fallout deposits and out of the Apennine valleys). Here we present distribution maps for the lahar deposits of the Pollena and 1631 eruptions (Figs. 8–11).
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We provide an array of services, encompassing educational courses in trading and investing, insightful trading research, and sophisticated risk management instruments. At Acerra, the Tdep interval is 120–140 °C, while for Nola Tdep is lower than 120 °C (Fig. 14). In the Nola case, a low-temperature magnetization component lower than 120 °C cannot be directly considered to be a thermal remanent magnetization (TRM). In fact, the low-Tb Earth field component of magnetization can also be produced by a viscous remanent magnetization (VRM), acquired during exposure to weak fields (Bardot and McClelland, 2000). For an age around that of the Pollena eruption, the minimum Tdep which can be distinguished is ca. The municipalities with the highest number of reports are Sarno (43), Salerno (32), Siano (26), Vietri sul Mare (22), Bracigliano (21), Nocera Inferiore (20), Maiori (19), and Quindici (17) (Fig. 1).
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