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Volume 23, Issue 6
  • E-ISSN: 1365-2117

Abstract

ABSTRACT

We present a new lithostratigraphy and chronology for the Miocene on central Crete, in the Aegean forearc. Continuous sedimentation started at ∼10.8 Ma in the E–W trending fluvio‐lacustrine Viannos Basin, formed on the hangingwall of the Cretan detachment, which separates high‐pressure (HP) metamorphic rocks from very low‐grade rocks in its hangingwall. Olistostromes including olistoliths deposited shortly before the Viannos Basin submerged into the marine Skinias Basin between 10.4 and 10.3 Ma testifies to significant nearby uplift. Uplift of the Skinias Basin between 9.7 and 9.6 Ma, followed by fragmentation along N–S and E–W striking normal faults, marks the onset of E–W arc‐parallel stretching superimposed on N–S regional Aegean extension. This process continued between 9.6 and 7.36 Ma, as manifested by tilting and subsidence of fault blocks with subsidence events centred at 9.6, 8.8, and 8.2 Ma. Wholesale subsidence of Crete occurred from 7.36 Ma until ∼5 Ma, followed by Pliocene uplift and emergence. Subsidence of the Viannos Basin from 10.8 to 10.4 Ma was governed by motion along the Cretan detachment. Regional uplift at ∼10.4 Ma, followed by the first reworking of HP rocks (10.4–10.3 Ma) is related to the opening and subsequent isostatic uplift of extensional windows exposing HP rocks. Activity of the Cretan detachment ceased sometime between formation of extensional windows around 10.4 Ma, and high‐angle normal faulting cross‐cutting the detachment at 9.6 Ma. The bulk of exhumation of the Cretan HP‐LT metamorphic rocks occurred between 24 and 12 Ma, before basin subsidence, and was associated with extreme thinning of the hangingwall (by factor ∼10), in line with earlier inferences that the Cretan detachment can only explain a minor part of total exhumation. Previously proposed models of buyoant rise of the Cretan HP rocks along the subducting African slab provide an explanation for extension without basin subsidence.

© 2011 The Authors. Basin Research © 2011 Blackwell Publishing Ltd, European Association of Geoscientists & Engineers and International Association of Sedimentologists
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Formation and fragmentation of a late Miocene supradetachment basin in central Crete: implications for exhumation mechanisms of high‐pressure rocks in the Aegean forearc
Basin Research 23, 678 (2011); https://doi.org/10.1111/j.1365-2117.2011.00507.x
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. Data file showing details on location, lithology, biostratigraphy and palaeobathymetry of the studied sections and outcrops in central Crete along with their lithostratigraphic and biozonal assignment. Sections and outcrops in this file are arranged from area I to V and from E to W per area.. Description and definition of the planktonic foraminiferal biozones defined in Gibliscemi (Sicily) and Metochia (Gavdos). The biozones are considered to be useful for correlating and dating upper middle to lower upper Miocene sediments in the Mediterranean region.. Location of sections and outcrops shown in Figure 2b plotted on a scanned version of the Tourist Map of Crete 1:100,000 (Harms‐ic‐Verlag, Germany). O=Kourtes; N=Agios Ioannis. (Semi) Quantitative distribution and coiling of selected planktonic foraminiferal taxa in section Gibliscemi (Sicily). This section combines subsections A to F described in Krijgsman . (1995) and Hilgen . (2000). The semiquantitative data for Gibliscemi A, B and C (extending from cycle G ‐3 up to top sapropel of cycle G 85 are based on 125‐595 micron fraction counts of all 620 samples (average sample resolution < 5 kyr) including the data‐set published in Krijgsman . (1995) which was based on only 40% of all samples from Gibliscemi A and B. This semi‐quantitative record is spliced with the published quantitative pattern in the older part of the Gibliscemi sequence, i.e. Gibliscemi E, D and F (Hilgen ., 2000; Turco ., 2001). The spliced record combines (small) and (large) into and stricto and N. 4‐chambered into . We further added percentages of per total neogloboquadrinids (with–10 values indicating samples where neogloboquadrinids are absent). The distribution and coiling pattern of the selected planktonic foraminiferal taxa allows a subdivision of the spliced record into nine planktonic foraminiferal biozones (numbered 1 to 9) and two subzones (numbered 7.1 and 7.2) up to the level of a significant hiatus at the top of the sapropel of cycle G 85 spanning ~200 kyr (Krijgsman et al., 1995).. Semi‐quantitative distribution and coiling of selected planktonic foraminiferal taxa in section Metochia (Gavdos). The data presented here replace the original presence‐absence data in Krijgsman . (1995) and are based on studying the 125‐595 micron fraction of all 560 samples providing a resolution of < 5 kyr. Note that specimens referred to as in Krijgsman . (1995) are re‐labeled (see also discussion in Hilgen ., 2000). Lithology, sample position and cycle numbers are from Krijgsman . (1995) with the mentioning that we extended the original cycle pattern downward with cycles M0 to M‐2. Biozones 6 to 9 and subzones 7.1 and 7.2 defined in Gibliscemi are present in Metochia as well and extended upwards by biozones 10 and 11.. Lithostratigraphic units for the Neogene basin fill in central Crete in this and earlier studies. Units are equally boxed using the base of Pliocene as reference line.. Photobook.. Ages of planktonic foraminiferal bioevents defining 11 biozones (described in Appendix S2) and their position in terms of sample and sedimentary cycle numbers in sections Gibliscemi (Sicily) and Metochia (Gavdos). Ages for defining bioevents in Metochia are derived from retuning of sedimentary cycles (M‐cycles) to the Laskar 2003(1,1) solution by Lourens et al. (2004). Updated ages for bioevents in Gibliscemi A and B are based on retuning G‐cycles to La2003(1,1) by Lourens et al. (2004) and for bioevents in Gibliscemi F‐C by retuning correlative cycles in the Monte dei Corvi section (northern Italy) to La2004(1,1) by Hüsing et al. (2007). Ages in red are used in this paper. Also shown is position of bioevents in terms of sample number (as registered in the Utrecht collections) and sedimentary cycle number. Table also includes identified magnetic chron boundaries in Metochia (Krijgsman et a., 1995) and Monte dei Corvei (Hüsing et al., 2007) together with their position in terms of M‐cycles and correlative G‐cycles (from Hilgen et al., 2003). Updated ages for magnetic chron boundaries in Metochia are from Lourens et al. (2004) and in Monte dei Corvi from Hüsing et al. (2007).[Correction added after online publication 24 August 2011 ‐ in Location 8 in Appendix S1, the sentence ‘a correlation of the lower Kastellios Hill section to Chron 4Ar.2r is the most likely’ was changed to ‘a correlation of the lower Kastellios Hill section to Chron 4Ar.1r is the most likely’]Please note: Wiley‐Blackwell is not responsible for the content or functionality of any supporting materials supplied by the authors. Any queries (other than missing material) should be directed to the corresponding author for the article.

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  • Article Type: Research Article

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