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The geology of Sicily (a large island located at Italy's southwestern end) records the collision of the Eurasian and the African plates during westward-dipping retreating subduction of the African slab since late Oligocene. Major tectonic units consists of the Hyblean foreland, the Gela foredeep, the Apenninic-Maghrebian orogen, and the Calabrian Arc. The orogen represents a fold-thrust belt that folds Mesozoic carbonates, while a major volcanic unit (Mt Etna) is found in an eastern portion of the island. The collision of Africa and Eurasia is a retreating subduction system, such that the descending Africa is falling away from Eurasia, and Eurasia extends and fill the space as the African plate falls into the mantle, resulting in volcanic activity in Sicily and the Tyrrhenian slab to the north.

Tectonic History
The tectonic setting of Sicily is controlled by the rate of collision of the African plate and Eurasian plate and the rate of back rolling of the African plate. The tectonic history of Sicily can be divided into four main stages :

Late Triassic- Early Jurassic period
During Late Triassic, the ancient Neotethyan ocean was formed by a major continental rifting event and rapid tectonic subsidence. Traces of the tectonic event can be found at both the Hyblean plateau and western Sicily.

Early Jurassic-Late Cretaceous period
After the rapid subsidence during Triassic to Early Jurassic, there was a slow thermal subsidence at the Mediterranean basin from Jurassic to Late Cretaceous that formed the Neotethyan carbonate platform.

Late Cretaceous-Palaeogene period
During Late Cretaceous and Palaeogene, the collision of African and Eurasian plates generated compressive stress in the region. The Neotethyan ocean was closed by the collision and the continental margin became active.

Neogene-Quaternary period
Sicily has been undergoing a phase of uplifting and subduction since Neogene. The African slab retreats to the east as the collision of Eurasian and African plate continued. Since late Oligocene, the orogenic process started when sediments accreted onto the Calabrian block while flysch was deposited in the foreland basins. The Sardinia block then underwent counter-clockwise rotation and the Calabrian unit subsequently underwent clockwise rotation. During the Early–Middle Miocene, shallow seated thrusting occurred which formed the wedge-top basins. Since Late Miocene, thrusting occurred in the Sicilian orogen and Calabrian accretionary wedge. Extension and back-arc magmatism occurred in the Tyrrhenian slab due to the fast roll back of the Ionian slab, while Calabria migrated to the current position at northeast Sicily.

Hyblean Foreland
The foreland consists of exposures of the Hyblean Plateau and the offshore areas of Gela. The subduction forms a northward-dipping monocline in the foreland with a dip of 16-18°, which is a high angle compared to other regional monoclines. This is suggested to be caused by a higher subductibility of the African slab. Deformation in the foreland is dominated by normal faulting, which most of these faults are formed in Neogene by plate flexure. Some of the faults are identified to be much older and was formed in Mesozoic, which the faults are suggested to have separated high-standing platforms from deeper basins.

The simplified stratigraphy includes the following units :

The post-Paleogene geological events of the foreland can be divided into four main stages:

At early Miocene, thrusting and volcanic activity triggers a regional uplift at the foreland, which caused the emergence of a broad carbonate platform in the eastern Hyblean Plateau.

During the Messinian of late Miocene, the Messinian salinity crisis occurred as a result of sea-level fall and major uplift, causing deposition of evaporites over the Mediterranean basin. The dry climate resulted in extensive erosion in high-standing regions of the plateau.

At Early Pliocene, rapid subsidence occurred at the foreland. This subsidence event occurred simultaneously with a major rise in Mediterranean sea level which Plio-Pleistocene sediments were accumulated in the foreland basin.

During the Late Miocene-Early Pleistocene, a massive basaltic volcanic activity occurred. After the emission of alkali basalts during Late Miocene, major volcanic activity occurred during the Late Pliocene, which large volumes of tholeiitic basalts were emitted and the foredeep north of the Hyblean foreland collapsed.

Gela Foredeep
The Gela foredeep extends from the northern margin of Hyblean plateau onland to Gela basin, the offshore area of southwestern Sicily. Based on fossil analysis, the basin has been developing since Late Pliocene, and its formation is related to the bending of the carbonate platform due to loading at the front of the Gela nappe. The basin fill consists of Late Miocene-Pleistocene sediments, including marly limestonees, Messinian evaporites and sandy clays.

The Apenninic-Maghrebian orogen
The central to western part of Sicily is made of the Maghrebian-Apenninic orogen, represents the fold and thrust belt of the subduction system. A combination of frontal accretion and low-angle detachments formed the present geological structure. The orogen consists of a stack of detached nappes that involves mostly the Mesozoic carbonate, which had been folded subsequently into a syncline, underlying a broad anticline of the Caltanissetta area.

The stratigraphy of the wedge is composed of the following units :

Calabrian crystalline basement
The northeastern part of Sicily consists of the Calabrian Arc unit, the tectonic unit that connects the Apennines with the North African Maghrebide. Paleozoic igneous and metamorphic basement rocks are exposed at this part of the island, suggested to be exposed by exhumation process between mid-Oligocene and Middle Miocene. The rapid migration of the Calabrian Arc towards the southeast was driven by the retreat of the Ionian slab east of Sicily. In early Miocene, Calabria was still attached to Sardinia. In Middle Miocene, the trench rolled back to the east and normal faulting occurred between Calabria and Sardinia, causing Calabria to split eastward from Sardinia. By Early Pliocene, the retreat of Calabria consumed the oceanic slab of the Ionian sea while new oceanic crust is created in the Tyrrhenian sea by back-arc magmatism. Since Pleistocene, the eastern portion of the arc formed the Apennine mountain of Italy while the Calabrian block slide through right lateral strike-slip motion to Sicily to form the northeastern portion of the island. GPS measurements shows that the Calabrian Arc still advances to the southeast at 2-3mm per year at present days due to the roll back of the Ionian slab.

The simplified stratigraphy consists of the following units :

Mount Etna
See also: Mount Etna

Mount Etna is an active stratovolcano located at the eastern coast of Sicily which is composed mainly of basalt. Its formation began at about 0.5 Ma when submarine volcanism occurred at the Gela foredeep and formed tholeiitic pillow lava. At about 0.3 Ma, a tholeiitic lava plateau was formed on an ancient alluvial plane by fissure-type volcanism. From 0.22 Ma, volcanism mainly occurred at the Ionian coast which formed an alkaline shield volcano with length of 15 km at the N-S direction, until volcanism shifted westward to the current location of Mt. Etna at about 129 ka. Finally, central-vent type volcanism began with the formation of two small parasitic cones, which the eruption of these two cones ended at 106 and 102 ka. It is suggested that the formation of Mount Etna is closely related to the subduction system of Sicily. Although the magma does not originate from the subducted material, the retreat of African slab creates a low-pressure zone at the mantle wedge under Calabria, which pulls the asthenospheric material under the African plate laterally towards the northeast. This process produces a large volume of magma that caused upwelling under Mount Etna, as well as the regional uplift of the Calabrian unit.

Mining
Sicily is known for its history of sulphur production which sulphur mining was active until the 20th century. Abandoned sulphur mines includes those in Castelterminin, Enna and Caltanissetta. The major ores were sulphur-bearing sedimentary deposits, formed during the Messinian Salinity Crisis, which thick layers of evaporites including gypsum and other evaporitic sulphur were deposited in the central Sicilian basin when the area was above sea level. These native sulphurs are associated with secondary carbonates and are suggested to be formed by intense microbial sulphate reduction, which microorganisms 'breath in' sulfate instead of oxygen for anaerobic respiration.