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McCave (1979) has doubted both the secondary-flow model and Stride’s (1974) lag effect, on the basis of measurements of the profile of velocity at the North Hinder Lightship, 3 km to the west-northwest of the North Hinder Bank in the Southern Bight of the North Sea. According to him, the near-bed current deviates in direction from the velocity at 10m below the surface in a manner inconsistent with the presence of a secondary flow. This is correct only if, as McCave assumes, the measurements came from the cell characterized by a bottom-current directed toward the crest of the bank.
1-20. Air photograph (10 by 10 km) showing complex longitudinal dunes, Grand Erg Oriental, Sahara. Dominant wind from upper left toward right, but with evidence for reversals. longitudinal dunes consist of sand of a finer texture than the debris in the corridors between, where bed-rock or clay layers, gravel, or bimodallydistributed relatively coarse sands abound. No finer material is permitted by the wind to linger in the interdune corridors. It is no surprise that the internal structure of these large dunes should be ill-known.
Longitudinal grooves are not uncommon in water-depths of several tens of metres. Those reported by Donovan and Stride (1961) are extremely large but, because they are generally ungrouped and depend closely on outcropping hard and soft strata, are unlikely to be controlled by secondary currents. The latter explanation seems most appropriate to the systems of large grooves and ridges described by Dyer (1970), Stride et al. (1972), Newton et a]. (1973), Bouma et al. (1978), and Reinson (1979), eroded into respectively mud, gravel, fine sand over gravel, bed rock and, possibly, gravel.