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A package of impure fine sandstone with poorly developed bedding follows in the succession.
As a result, joints that traverse impermeable deformation band shear zones may provide the primary pathways for fluid flow in sandstones compartmentalized by these zones.
Numerous thin sandstone beds (in general about 10 cm thick) are separated by thicker units of flaser-bedded siltstones and mudstones.
Incubation vessels inside the chamber were filled with sterile sand, inoculated with crushed sandstone-based biofilms and allowed to incubate for 5.5 months.
The c. 25 m of purple, fine-grained sandstones below include quartz-arenitic intercalations and have an essentially calcareous matrix.
In the channel casts, the sandstone packages are separated by oscillation wave ripples and microbial structures.
The sharp-based sandstones with traction-generated internal sedimentary structures represent storm eventbeds emplaced by episodic storm-generated currents.
Some conglomerates contain thin (< 10 cm) lenses of sandstone.
These conglomerates are composed of clasts of basalt, volcaniclastic sandstone, alkaline lava and sub-rounded chert.
This consists of coarse-grained sandstones with frequent pebbles or thin interbeds of small pebble conglomerates.
This second phase of electron microscopy was carried out to determine accurate percentages of each mineral phase present in the different sandstones.
This facies occurs as beds of coarse or medium to fine, normally graded sandstone between 0.3 and 1.0 m thick.
Interbedded thin fine-grained sandstone and siltstone layers are laminated and wavy in nature.
The siltstones commonly contain detrital white mica flakes that are generally lacking in the sandstones, and are possibly of distal continental origin.
The sandstones are the more reliable indicators of the state of evolution of arcs of this type, as they represent near-source deposition.
