Continental Rifted Margins 2. Gwenn Peron-Pinvidic
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Название: Continental Rifted Margins 2

Автор: Gwenn Peron-Pinvidic

Издательство: John Wiley & Sons Limited

Жанр: Физика

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isbn: 9781119986942

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СКАЧАТЬ granulites, all interpreted as lower crustal rocks, while Site 1068 drilled serpentinized peridotites, which were interpreted as serpentinized mantle (Whitmarsh et al. 1998). Underlying rotated blocks between Sites 1065 and 1067, the H detachment is warped up and separates Site 900 from Site 1068 (Figure 1.4), so similarly to S, H likely represents a serpentine detachment delineating the CMB (Chian et al. 1999). Cutting across and rotating the H detachment, the fault bounding the western side of Site 1068 has been interpreted as marking the development of a newly formed detachment, which has been variously termed F detachment (Krawczyk et al. 1996) and HHD detachment (Manatschal et al. 2001, pp. 405–428). F/HHD defines the top of seismic basement from this high down to a fault block drilled at Site 1069. This rider block appears to be an allochthonous continental slice (based on the recovered sediment) resting on the same peridotitic basement as the one sampled at Site 1068. Site 899 recovered serpentinite breccias intercalated with sediments, indicating the presence of a nearby serpentinized high (Whitmarsh et al. 1998), and Site 897 recovered highly sheared, partially serpentinized mantle peridotites (Sawyer et al. 1994). Finally, Site 1070, located 15 km east of the M0 magnetic anomaly (Figure 1.1), recovered serpentinized mantle rocks and gabbro.

      1.2.3. Conjugated West Iberian and Newfoundland Margins

      The DGM faces the southeast flank of the Flemish Cap at the Newfoundland Margin (Figure 1.1a and sections SCREECH 1/ISE1 on Figure 1.2), whereas the SIAP faces the North Newfoundland Basin (Figure 1.1a and sections SCREECH 2/LG12-TGS on Figure 1.2). Palaeographic reconstructions have proposed that both the Western Iberian and the Newfoundland margins represented a pair of conjugated margins before continental breakup (e.g. Sutra et al. 2013). The final root of S observed at the DGM is incidentally believed to be currently located on the Flemish Cap (Reston et al. 2007).

      A key finding of the drilling at the SIAP was the demonstration of the presence of a wide-zone of unroofed mantle (from Site 900 to 1070 and oceanward, Figure 1.4) that extends between the hyper-thinned continental crust and the first clear magnetic polarity reversals (Figure 1.1, M0), outlining the areas where seafloor spreading occurred. This observation west of Iberia has underpinned the concept of mantle unroofing on a large-scale at other rifted margins (Whitmarsh et al. 1998; Manatschal et al. 2001). It has also led to the concept of margin pair asymmetry (e.g. Pérez-Gussinyé and Reston 2001), as comparison of sections across both margin segments (Figure 1.2) clearly shows the asymmetry of the unroofed mantle (e.g. Reston 2009). The mantle extends across ~250 km within the SIAP (sections LG12-TSG, IAM-9, Figure 1.2), versus ~50 km west of the COT offshore the Northern Newfoundland Basin (section SCREECH2, Figure 1.2). Asymmetry between the margin pair also exists when considering the thickness of the continental crust: comparison between the two margins still shows a “normal” crustal thickness of ~30 km at the Flemish Cap, whereas at the Galicia Margin, the GIB and the GB are characterized by relatively thin crust, of about ~10 km (e.g. Druet et al. 2018). This asymmetry between the WIM and its Newfoundland conjugate margin has been interpreted as having developed once the crust had become completely brittle (e.g. Pérez-Gussinyé and Reston 2001; Reston 2009).

Schematic illustration of the extension discrepancy across the Iberian margin.