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198 A. Slootman et al. / Earth and Planetary Science Letters 444 (2016) 192–204

Fig. 5. Palaeohydraulic reconstruction of the studied section of the examined backset-bedded clinoform unit. (A) Line drawing of internal stratification. See also Fig. 4. (B–G)
Time-progressive morphodynamic reconstructions of flow and bed. Note that only the basal flow is depicted and not the overriding low-density flow nor the ambient sea
water. Note preservation of the downstream lee side deposits (arrow in (B)). Time span (B–G) is of the order of a few hours (Table 1).

4.3. Dune cross-bedded clinoform units                              of southeastward currents that underwent an apparent deflection
                                                                    to the right due to the Coriolis force (cf. Puga-Bernabéu et al.,
4.3.1. Sedimentary features                                         2010; Massari and D’Alessandro, 2012). A single high-angle cross-
    Backset-bedded clinoform units are enveloped by stacks of       bed (up to 10 cm thick, dipping up to 30 degrees) is bounded by
                                                                    the highest-order surface in a clinoform unit and is deposited from
high-angle cross-bedded sets, comprising ca. 50% of the studied     an individual grainflow down the lee-side of a small- to medium-
carbonate ramp succession (Fig. 2). Such dune cross-bedded clino-   scale dune (sensu Ashley, 1990). Such dunes encompassed parasitic
form units were formed by the action of subaqueous dunes, which     bedforms that migrated over the stoss-side of a large-scale (sensu
migrated slightly oblique down the ramp slope (Fig. 1) as a result
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