It is generally subaphyric and contains clinopyroxene micro-phenocrysts (10–50 m), almost always sopra synneusis with magnetite and olivine micro-phenocrysts (Acquafredda et al., 1999).
3.2. Sardinia: Ammasso Arci
30 km 2 and located con the comprensorio of the gulf of Oristano. The volcanic activity developed during two distinct cycles sopra the Pliocene and Pleistocene, and therefore it belongs puro the latest volcanism mediante Sardinia. The magmatic products erupted during the second cycle, can be divided into four phases. The lavas erupted per the first phase were very rich durante silica, and consisted mainly of rhyolites, either massive or perlitic-obsidianaceous. Dacites and andesites, trachytes and trachyrhyolites followed per chronological succession, until the last stages of volcanic activity, which were characterized by quiet eruptions of basaltic magma flows (Piras, 2002; Bigazzi et al., 2005).
The obsidian outcrops were described for the first time con the 19 th century by De La Marmora (1839–40). Subsequently, mediante the 1980s, several independent studies contributed sicuro the characterization of the multiple Monte Arci obsidian outcrops. Unfortunately, the results of these studies are available only con brief conference papers (Francaviglia, 1986; Mackey and Warren 1983) or durante an unpublished dissertation (Herold, 1986).
More recently, considering the geochemical features the obsidian of Ammasso Arci, Tykot (2002) subdivided them into four groups, SA, SC https://datingranking.net/it/asiandate-review/, SB1 and SB2. The obsidian sampled near Acquaio Cannas and Uras are clustered within the SA group; those sampled near Pau, Perdas Urias and Sonnixeddu belong onesto the SC group; those sampled at Santa Maria Zuarbara and Marrubiu are mediante the SB1 and SB2 groups, respectively (Tykot, 2002; Barca et al., 2007; De Francesco et al., 2008). Coppia sicuro their geochemical similarity, SB1 and SB2 have been grouped under the name SB sopra the present study.
Monte Arci obsidian populations are characterized by large biotite micro-phenocrysts (50–200 ?m), abundant crystals of feldspar (plagioclase and alkali feldspar) 50 ?m in size, orthopyroxene, magnetite, monazite and ilmenite (Acquafredda et al., 1999).
3.3. Palmarola
Geochronological datazione, obtained by fission-track analyses, indicate an age of 1.7±0.3 Bensi for obsidian from Montagna Tramontana (Bigazzi et al., 1971; Bigazzi and Radi, 1981). Per per recent work Tykot et al. (2005) provided per detailed geochemical study of 80 samples, and were able puro distinguish three source localities: Vocabolario Vardella, the northern end of Pezzo Vardella and Mucchio Nord. However, given the small size of the island, this distinction can be considered irrelevant from an archaeological point of view.
Palmarola obsidian contains micro-phenocrysts of clinopyroxene (5–20 ?m) and biotite. It is generally black durante colour, glassy, poorly shiny and semi-opaque (Acquafredda et al., 1999). However, per small amount of highly transparent obsidian was found at Lingua Vardella by Tykot et al. (2005).
3.4 Pantelleria
90 km east of Cape Bon, Tunisia. Pantelleria is famous for its peralkaline rocks, and especially for its greenish obsidian enriched mediante sodium and iron, known as Pantellerite (Civetta et al., 1998; Acquafredda et al., 1999). Pantelleria has per bimodal distribution of magmatic products. Mafic lavas, exposed durante the NW spigolo of the island, include transitional basalt and hawaiite (from
62 to 72 wt.% SiO2), prevail in the SE sector (White et al., 2009). K–Ar determinations of mafic lavas done on different basaltic units give ages of 118 ± 9, 83 ± 5 and
29 ka BP (Civetta et al., 1984). Ages determined on felsic volcanic rocks range from 324 ka BP esatto 4 ka BP (Farfallina et al., 1984, 1988, 1998; Mahood and Hildreth, 1986). The volcanic history of the island is characterized by large explosive eruptions, some of which produced caldera collapses, alternating with periods dominated by less energetic eruptions (Fraschetta et al., 1998). The oldest caldera, named La Vecchia, is dated at 114 ka BP (Mahood and Hildreth, 1986); the youngest caldera, named the Camposanto caldera by Cornette et al. (1983) and the Cinque Sporgenze caldera by Mahood and Hildreth (1983), is related sicuro the eruption of the Green Tuff (50 ka BP; Orsi and Sheridan, 1984). The more recent (post-50 ka) history of the island has been subdivided by Farfallina et al. (1998) into six sialic eruptive cycles, intercalated with basaltic eruptions. The Green Tuff is considered the first of these six cycles. All the others are dated at around 35–29, 22, 20–15, 14–12 and 10–4 ka BP, respectively (Civetta et al., 1998).