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Local remnants of blueschist parageneses from the earlier Eocene subduction-related HP-LT episode (Wijbrans & McDougall, 1988) are preserved in the southern part of the dome (Avigad, 1998; Jansen, 1977) despite the overprint of the high-temperature Oligo-Miocene event. Later, during the formation of the Aegean Sea in back-arc context, the dome underwent a MP-MT/HT event, dated between 20.7 and 16.8 Ma by sensitive high-resolution ion microprobe U-Pb on zircons, Wijbrans & McDougall, 1988) and the overlying UCU that consists in Miocene sandstones, conglomerates, and remnants of ophiolitic rocks, 1977. ,
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To document the overall geometry of the intrusion and then to study the internal distribution of strain, we first complemented the geological map of Naxos (Jansen, 1973; Siebenaller, 2008) and described finite strain markers over the whole intrusion. The resulting new structural map of the intrusion is proposed in Figure 2. Results from the measurements of finite strain markers are presented in two synthetic maps showing either the foliation or the lineation and, Large-Scale Geometry and Internal Architecture of the Intrusion 3.1. Finite Strain Markers Only few field studies focused on the geometry of the monzogranite intrusion of Naxos, 1993. ,
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