Note the type of cross-bedding can rarely be determined in core.

A picture of cross-stratification, also called cross-bedding, is shown on the left.

Cross-bedding is especially evident in the eastern part of the park where Jurassic wind directions changed often.

Bedding may be irregular but is almost always present, and cross-bedding is common.

Evidence for this is in cross-bedding of the sediments and large numbers of fish fossils.

It is a form of cross-bedding usually formed by the action of large storms, such as hurricanes.

Cross-bedding can form in any environment in which a fluid flows over a bed with mobile material.

Composed of coarse sandstone, river cross-bedding indicates deposition in a stream environment.

These rather massive calcarenites can reach a thickness of 12-15 m in places and sometimes are affected by cross-bedding.

Curves for the determination of compaction using deformed cross-bedding.

Cross-bedding refers to inclined beds of sedimentary rock formed by deposition from wind or water.

The large-scale cross-bedding was generated by the migration of very large dunes moved by tides.

Scroll-bar sediments are characterized by cross-bedding and a pattern of fining upward.

Features associated with cross-bedding occur relatively frequently.

In some cases bioturbation is so pervasive that it completely obliterates sedimentary structures, such as cross-bedding.

Cross-bedding is widespread in many environments.

Cross-bedding can be subdivided according to the geometry of the sets and cross strata into subcategories.

Cross-bedding is formed by the downstream migration of bedforms such as ripples or dunes in a flowing fluid.

Tabular cross-bedding is formed mainly by migration of large-scale, straight-crested ripples and dunes.

The original direction of the strata can be established using the graded and cross-bedding of sedimentary structures.

In sedimentary rocks this may include sole markings, ripple marks, mudcracks and cross-bedding.

Lower: Medium-grained arkosic and kaolinitic sandstones with trough cross-bedding.

The opposite of cross-bedding is parallel lamination, where all sedimentary layering is parallel.

The most commonly described types are tabular cross-bedding and trough cross-bedding.

The exposures of Permian sands exhibit complex cross-bedding that is believed to represent ancient seif dune deposits.