By David M. Rubin
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Extra resources for Cross-Bedding, Bedforms, and Paleocurrents (Concepts in Sedimentology & Paleontology 1)
First, upcurrent migration of superimposed bedforms occurs locally in the 52 COMPUTER IMAGES-VARIABLE 2-0 upslope-migrating bedform that deposited a relatively thick set of foresets (B). The main bedform continued to migrate to the left after the superimposed bedforms disappeared (C). If found in the geologic record, these beds might be incorrectly identified as tidal deposits (Figs. 29 and 30), because of the flow reversals indicated by the reversals in ripplemigration direction. The real cause of the flow reversals was probably the formation and decay of eddies at the depositional site.
The resulting structures have gently undulating lower bounding surfaces, as shown here, or have scalloped bounding surfaces, as shown in Figures 16 and 17. ORIGIN: Fluctuations in bedform height can be random changes undergone by individual bedforms or, as illustrated here, can be systematic changes undergone by entire populations of bedforms. Systematic fluctuations in height of such bedforms as sand waves can arise from changes in flow velocity or flow depth (Rubin and McCulloch, 1980) and can probably arise from fluctuations in flow direction.
Oscillation ripples that occur in an area undergoing erosion can also produce this structure (Fig. 11). FIG. - Structure formed by a stoss-erosional and lee-erosional angle of climb. RECOGNITION: This structure is purely erosional, and consequently is probably extremely rare. Preservation can occur when the rate of deposition increases, a similar situation to that shown in Figures 13 and 14. Bedform spacing is indicated by the spacing of undulations on the bounding surface. ORIGIN: Where the rate of erosion approaches the rate of bedform migration, bedforms scour downward into the underlying substrate without accumulating sediment, even on their lee sides.