Abstract The basins in the Eastern Mediterranean can be divided into those that were formed mainly in post-Miocene time and those that were formed during the rifting episodes that led to the formation of the Neotethys. The younger basins can be further divided into those that were formed mainly in post-Miocene time and those that were formed in post-Pliocene time. The separation is not only one of convenience but also corresponds to major adjustments in the plate tectonic situation in the Eastern Mediterranean. The late Miocene deposition of thick evaporites throughout the Mediterranean region, or, where evaporites are missing, the creation of an important erosional unconformity during the extreme lowstand of the Mediterranean, makes the Miocene-Pliocene boundary relatively easy to identify, especially on seismic reflection records. At about the same time, following the collision of the Arabian plate with Eurasia, the Anatolian and Aegean microplates came into existence between the convergent African and Eurasian plates to accommodate tectonic escape between them. The general configuration of the Eastern Mediterranean basins reflects the tectonic and structural gradients between the collisional domain of southeastern Turkey and Iran, and the continuing but increasingly limited subduction along the Calabrian and Hellenic arcs, with the Cyprus and Levantine zones between them. Several distinct zones can be identified in the Eastern Mediterranean. The Dead Sea Fault system marks the edge between the collisional and pre-collisional zones to the east and west, respectively. The meridian through the Anaximander Mountains (30°E) forms a rough boundary between the zone of incipient collision to the east and the zone of continuing but late-stage subduction to the west. The Malta Escarpment forms the Eastern boundary of the Eastern Mediterranean basins. The series of basins along the northern margin of the Eastern Mediterranean and the Aegean Sea share this progressive evolution, with those containing Messinian evaporites to the east and those without to the west. The Sicily Channel with its associated basins is an extensional zone between the Eastern and Western Mediterranean. The basins discussed in this paper are divided into two groups, the larger and older basins and the smaller and younger basins. In the first group are the Ionian Basin and the Levantine Basin, and in the second group the Cilicia Basin, Antalya Basin, Finike Basin, Rhodes Basin, Aegean basins, Sicily Channel basins, Latakia Basin and Larnaca Basin. The Eastern Mediterranean represents the last stage in the evolution of an ocean basin. Given the current motion between Africa and Eurasia, the Eastern Mediterranean will cease to exist in about 6–8 Ma from now. As a result, the larger and older basins are shrinking, whereas the younger and smaller basins are growing. Eventually the smaller basins will also disappear.

Abstract Information concerning the glacio-eustatic controls on Quaternary cool-water carbonates is dominated by data contained within the Holocene to Recent marine shelf record. However, this information represents only part of a full eustatic cycle. Much of the data comes from Southern Ocean-based biofacies studies associated with seafloor sediments. Geophysical studies provide further information on earlier Quaternary seafloor deposits and yield valuable data on sediment geometries; however, these works yield little direct information that can be applied to carbonates at outcrop scale. In contrast, Quaternary cool-water carbonates in the Mediterranean region offer outcrops with continuous exposure along which facies changes are readily accessible for study. In southern Italy and Sicily in particular, post-depositional uplift permits outcrop-based studies of large tracts of Quaternary microtidal cool-water carbonates, containing complete interglacial eustatic cycles. This study examines the carbonates associated with the Emilian sub-stage of the early Quaternary Calabrian Stage.