Figure 13 5 Close-up of Fig. 13.4 for the central Adriatic Sea.
Related Figures (27)
Fig. 13.1 On the left, a digital elevation model of Italy and surrounding seas (data from www.gebco.net/); note the change from light blue to dark blue marks the approximate limit of the continental shelf. On the right, a simplified tectonic map of Italy and surrounding regions, modified from Scrocca et al. (2003) with permission. (1) foreland areas; (2) foredeep deposits (delimited by the -1000-m isobath); (3) domains characterized by a compressional tectonic regime in the Apennines; (4) thrust belt units accreted during the Alpine orogenesis; (5) areas affected by extensional tectonics in response to the eastward roll-back of the west-directed Apennine subduction; (6) outcrops of crystalline basement (including metamorphic alpine units); (7) regions characterized by oceanic crust; (8) Apennine watershed; (9) thrust; (10) faults. Fig. 13.1 On the left, a digital elevation model of Italy and surrounding seas (data from www.gebco.net/); note the change from light blue Fig. 13.2 Map of the main tectono-stratigraphic units of Italy from the geological map of Italy at 1:1,250,000 scale (www.isprambiente.gov.it en/projects/soil-and-territory/the-geological-map-of-italy-1-250000-scale/default). Reproduced with permission from ISPRA. In Sicily, the natural morpho-dynamic processes of the coastal sectors of Trapani and the Catania Plain have been compromised by land use and global changes. However, increasingly, erosion is affecting all the sandy beaches of the Italian littoral, where the dune systems have been strongly compromised or definitively destroyed. bathymetry_data/). This database provides a bathymetric grid at 30 arcsecond intervals, with reference to geograph- ical coordinates, latitude and longitude in the WGS84 datum. Bathymetry and topography were processed using the software Global Mapper 11 (www.globalmapper.com) in order to produce maps at different levels of detail (Fig. 13.5 and 13.6). Fig. 13.4 The bathymetric data used in this map were derived from GEBCO. Isobaths between -130m and -10 m are well defined in the Adriatic Sea. Fig. 13.6 Close-up of Fig. 13.4 for the Tyrrhenian Sea. Fig. 13.7 Rates of vertical movement along the Italian coastlines for MIS 5.5 (125 ka) and the Holocene. Modified from Lambeck et al. 2011 Fig. 13.8 Vertical displacement rates (mm/year) computed from the elevation of (A) Late Pleistocene and (B) Holocene markers plotted with main structures on a DEM of Calabria and eastern Sicily. Modified from Ferranti et al. 2010. Fig. 13.8 Vertical displacement rates (mm/year) computed from the elevation of (A) Late Pleistocene and (B) Holocene markers plotted wit Fig. 13.11 DTM of the Panarea and Stromboli volcanoes. The DTMs are at 2.5-m and 5-m grid size at Panarea and Stromboli respectively. Local bathymetry in the area surrounding the Panarea archipelago (the islets of Panarelli, Dattilo, Lisca Nera, Bottaro, and Lisca Bianca) is at 0.5-m grid size, while regional bathymetry is at 10-m grid size. Fig. 13.12 Plio-Quaternary sediment thickness around the Italian coasts (data from IBCM charts, adapted with permission), displaying three main depocenters (see text for detail). Fig. 13.12 Plio-Quaternary sediment thickness around the Italian coasts (data from IBCM charts, adapted with permission), displaying three g. 13.13 (A) Thickness and depocenter distribution of the Late Holocene highstand mud-wedge in the Adriatic Sea. Modified from Cattan al. (2003) and reproduced with permission from Elsevier; on the right (B, C, D), thickness of highstand, transgressive and Quaternary posits. Data from 1:50.000 geological map of Italian sea ‘Venezia sheet’ (www.isprambiente.gov.it/ Media/carg/index_marine.html). 2produced with permission from ISPRA. Fig. 13.13 (A) Thickness and depocenter distribution of the Late Holocene highstand mud-wedge in the Adriatic Sea. Modified from Cattaneo Fig. 13.14 Map of Holocene sediment thickness in the southern Latium shelf. Modified from Chiocci and La Monica (1996) with permission; note the main depocenters are located offshore of the main rivers draining this sector (the Tiber to the north and the Garigliano to the south). ocean. The hydrodynamics of the basin are controlled by the North Atlantic water inflow, wind regime, and climate of the surrounding lands (Pinardi & Masetti 2000). Climate variability is related to the geographic position of the region located on the transition between high- and low-latitude influences. Paleoceanographic research demonstrates that during the Last Glacial interval, the Mediterranean Sea became a sensitive region, respond- ing to North Atlantic rapid climatic changes, includ- ing Dansgaard-Oeschger (D-O) and Heinrich events (Rohling et al. 1998; Cacho et al. 1999; Sangiorgi et al. 2003; Sierro et al 2005). In addition, it seems that the African monsoon extended at certain times over the Mediterranean basin and has been responsible for an increase in precipitation leading to increased freshwater input, reduced deepwater ventilation and deposition of sapropel layers (Tzedakis 2007). Various efforts have been made to estimate Quaternary SSTs in the Mediterranean Sea but most of these studies have considered single- core rather than multi-core analysis on a basin-wide scale (Kallel et al. 1997; Sangiorgi et al. 2003; Geraga et al. 2005; Di Donato et al. 2008). Additional problems are related to the different adopted methods (e.g. size fraction of faunal counting, use of different proxies) and TABLE 13.2 PRINCIPAL RECONSTRUCTION OF SST PERFORMED IN THE CENTRAL MEDITERRANEAN SEA. Central Mediterranean wave climate reconstructions for the central Mediterranean Sea at different epochs. These predictions were then extended to the whole Mediterranean (Lambeck & Purcell 2005). A complete review of the Holocene data, including the files of the predicted sea-level data for 40 Italian sites, has recently been published (see supplementary material in Lambeck et a/. 2011). Significant differences can be observed in stable coastal areas if different sites are considered: as an example, sea level at 10 ka cal BP varies along the Italian coasts between —48 m and —35 m, whereas at about 8ka cal BP it ranges between -19m and —11 m. The Mesolithic and Neolithic paleoshorelines predicted from Lambeck et a/. (2011) for Sardinia and the central Mediterranean are drawn in Figs. 13.17 and 13.18, and other examples using the same method and model are published for the islands of Pianosa and Elba (Tuscany) in Antonioli e¢ a/. (2011). An example of temporal and spatial evolution of land/sea extension and paleoshoreline evolution since the LGM is reported in Furlani eg al. (2013) for the area between southern Sicily and northern Africa. The survival of prehistoric sites in shallow seas depends partly upon the prevailing local wave climate. Enclosed between the storm belt of northern Europe and the tropical area of northern Africa, the Mediterranean Sea has a relatively mild climate on average, but substantial storms are possible, usually in the six-month winter (Cavaleri et al. 1991). The maximum measured significant wave height (H,) can reach 10m, but model estimates for some non-documented storms suggest larger values. For instance, even in the relatively small Adriatic Sea, an oceanographic tower, located 15 km offshore in 16m water depth, suffered heavy damage up to 9 m above sea level (Cavaleri 2000). Fig. 13.15 Mean April-May sea-surface temperatures (SST) during the LGM at 22 ka cal BP Figures are obtained by solving the Fig. 13.16 Mean April-May sea-surface temperatures (SST) during the Holocene Climatic Optimum at 8 ka cal BP Figures are obtained by the same methods as for those presented in Fig. 13.15. Fig. 13.17 Sardinia, Tyrrhenian Sea. DEM from GEBCO with “ig. 13.18 Coast of southern Latium, Tyrrhenian Sea. DEM from Fig. 13.20 Modified from Alvisi et al. (1994) and reproduced with permission from Istituto Italiano di Speleologia; black represents Fig. 13.21 Alghero, Sardinia. A partially submerged cave containing biased by selective pollen accumulation and preservation, resulting in an over-representation of the saccate pollen of conifers and in reduced floristic richness. The distance from the coast, and the water depth of the coring sites, clearly affect the vegetation reconstruction. The deep- sea records of the Adriatic Sea (-300m; Fig. 13.23) mostly represent the development of regional vegetation, as indicated by the high amounts of pollen from montane vegetation, corresponding to pollen inputs from far inland. In particular, both core KET 8216 and MD 90- 917 (Rossignol-Strick et al. 1992; Combourieu-Nebout et al. 1998) show significant percentages of Picea, most probably from the mountain ranges of the Balkan Peninsula. The vegetational landscape of the Italian coasts was herb-dominated, as also indicated by the coeval lacustrine records from inland regions (Follieri et al. 1998; Allen et al. 2000). Excluding Pinus, the most important trees were deciduous Quercus, which could populate areas both at middle elevations and along the coasts. By contrast, modest frequencies of evergreen Quercus were probably from low elevation sites. Marine cores from above 300 m depth in the Adriatic Sea, which were relatively close to the ancient coast, show high percentages of Juniperus, together with abundant steppe and grassland elements, while deciduous trees were less abundant than in the coeval deep-sea records (Lowe et al. 1996). Fig. 13.22 The Cala dell’Alabastro cave (San Felice Circeo, Italy, black line). The arrow indicates a Mesolithic site (Riparo Blanc) containing the shell mounds of limpets (Patella ferruginea) dated by radiocarbon; the submerged cave is of interest for future research. Modified from Antonioli and Ferranti (1994). Fig. 13.22 The Cala dell’Alabastro cave (San Felice Circeo, Italy, black line). The arrow indicates a Mesolithic site (Riparo Blanc) containing in the coeval deep-sea records (Lowe et al. 1996). Fig. 13.23 Location of coastal and marine pollen records in Italy for the time interval 22 ka cal BP to 5ka cal BP (dot = land site; triangle Fig. 13.23 Location of coastal and marine pollen records in Italy for the time interval 22 ka cal BP to 5ka cal BP (dot = land site; triangle = marine site above 300 m; star = marine site below 300 m). The gray area represents the modern distribution of evergreen vegetation. (1) Mistras: Di Rita and Melis (2013); (2) Le Fango: Reille (1992); (3) Saleccia: Reille (1992); (4) Rapallo: Bellini et al. (2009); (5) Sestri Levante Bellini et al. (2009); (6) Lago di Massaciuccoli: Colombaroli et al. (2007); (7) Versilian Plain: Bellini et al. (2009); (8) Arno S1: Amorosi et al. (2009); (9) Pisa Plain: Bellini et al. (2009); (10) Arno M1: Aguzzi et al. (2007); (11) Ombrone: Biserni and van Geel (2005); (12) Lingua d’Oca-Interporto: Di Rita et al. (2010); (13) Pesce Luna: Milli et a/. (2013); (14) Vendicio: Aiello et al. (2007); (15) C106: Russo Ermolli and ¢ Pasquale (2002); Di Rita and Magri (2009); (16) KET 8003: Rossignol-Strick and Planchais (1989); (17) Lago Preola: Magny et al. (2011); (1: Gorgo Basso: Tinner et al. (2009); (19) Biviere di Gela: Noti et a/. (2009); (20) Burmarrad: Djamali et al. (2013); (21) Lago Alimini Piccolo: Di Rita and Magri (2009); (22) MD 90-917: Combourieu-Nebout et al. (1998); (23) KET 8216: Rossignol-Strick et al. (1992); (24) IN9: Zonnevelc (1996); (25) SAO3-1: Favaretto et al. (2008); (26) Lago Salso: Di Rita et al. (2011); Di Rita (2013); (27) Lago Battaglia: Caroli and Caldara (2007); Caldara et al. (2008); (28) RF93-30: Oldfield et al. (2003); (29) RF93-77: Lowe et al. (1996); (30) PAL94-8: Lowe et al. (1996); (31) CM92-43: Asioli et al. (2001); (32) Ca’ Fornera: Miola et al. (2010); (33) Concordia Sagittaria: Miola et al. (2010); (34) Lake Vrana: Schmidt et al. (2000); (35) Malo Jezero: Jahns and van den Bogaard (1998); (36) Lake Voulkaria: Jahns (2005); (37) Alikes Lagoon: Avramidis et al. (2012). Fig. 13.24 Simplified map of the Italian continental shelf (in gray) Fig. 13.25 The Grotta Verde (Sardinia, Italy) section of a Neolithic necropolis containing ceramics and skeletons at -9m and anthropic Fig. 13.26 Emerged caves on land, on or close to the modern Fig. 13.26 Emerged caves on land, on or close to the modern coastline in northern Sicily containing prehistoric remains. Modified caves, some of which have been shown in recent studies to contain dated prehistoric sites, especially in central and southern Italy. At the moment the only prehistoric site that has published data is the Grotta Verde in northwest Sardinia (Alghero), containing Neolithic-age burials with Cardial pottery (6.7—7.2 ka cal BP, Antonioli et al. 1997 Fig. 13.25) and the site of Pakostane in Croatia (Radic Rossi & Antonioli 2008), where some hand-made wooden remains were found in situ at -5 m and dated to the Neolithic, although this research is still a work in progress. Finally, we illustrate some interesting caves (Fig. 13.26) located in northern Sicily close to the coast and above sea level containing prehistoric remains, while there are unstudied sea-flooded caves between —40 m and —15 m located in the surrounding cliffs. from Mannino and Thomas (2007) with permission from UCL.
