- Geology of the Canyonlands area
The exposed geology of the Canyonlands area is complex and diverse; 12 formations are exposed in
Canyonlands National Parkthat range in age from Pennsylvanianto Cretaceous. The oldest and perhaps most interesting was created from evaporites deposited from evaporating seawater. Various fossil-rich limestones, sandstones, and shales were deposited by advancing and retreating warm shallow seas through much of the remaining Paleozoic.
Eroded sediment from a nearby
mountain rangelater mixed with coastal dune and sand bar deposits. The end of the Paleozoic and the start of the Mesozoicsaw the last seas start to leave the region for good. A subdued topography was dominated by flood plains and tidal flats. Now much further inland, the Triassicclimate in the region was dry. Vast deserts covered much of that part of North America, except for one period when streams for a time fought the sand dunes. Wetter times returned.
The uplift of the
Rocky Mountainsstarting in late Cretaceous greatly affected the Canyonlands region. Erosion rates increased and further quickened upon the onset of the ice ages in the Pleistocene. Modern erosion occurs at a slower rate.
Deposition of sediments
A vast sea covered the region in early
Pennsylvaniantime. A basin in the area called Paradox Basinsubsided and a mountain rangecalled the Uncompahgre Mountainswas uplifted to the east. Great quantities of seawaterwere trapped in the subsiding basin and water became increasingly saline in the hot and dry climate. Thousands of feet of evaporites ( anhydriteand gypsumthen halite) started to build up in the Mid Pennsylvanian and storms occasionally washed sediment from the nearby mountains. Fresh seawater periodically refilled the basin but was never able to flush out the very salty water there (the new water in fact floated on top of the brine). These beds were later lithified to become the Paradox Formation, which in turn is part of the Hermosa Group. Compressed salt beds from the Paradox started to flow plastically later in the Pennsylvanian and probably continued to move from then until the end of the Jurassic. Satellite-based measurements indicate that flow of salt and gypsum continues today to cause flexing and faulting of overlying sedimentary layers.
The Paradox is up to 5000 feet (1520 m) thick in places and in the park is exposed at the bottom of
Cataract Canyonas rock gypsuminter-bedded with black shale. Upward movement of the Paradox is also a possible theory for the creation of Upheaval Dome, although none of the Paradox is exposed on the dome, the predominant theory being a meteor crater.
A warm shallow sea again flooded the region near the end of the Pennsylvanian. Limey oozes, sand, and mud were deposited on top of the salt-filled basin. These sediments became the
fossil-rich limestones, sandstones, and shales of the gray-colored Honaker Trail Formation. Outcrops of the Honaker Trail can be seen near the bottom of deep canyons in the park, most notably along the Colorado River.
A period of
erosionthen ensued, creating a break in the geologic record called an unconformity.
Early in the
Permiana transgressing (advancing) sea laid down the Halgaito Shale. Coastal lowlands returned to the area after the sea regressed (retreated), forming the Elephant Canyon Formation. These formations can now be seen in Cataract and Elephant canyons.
The Uncompahgre Mountains were undergoing extensive erosion during this time. Large
alluvial fans filled the basin where it met the range. The resulting Cutler red beds are made of iron-rich arkose sandstone. Underwater sand bars and sand dunes on the coast inter-fingered with the red beds and later became the white-colored cliff-forming Cedar Mesa Sandstone. Today these two competing rock units are exposed in a 4 to 5 mile (6.4 to 8 km) wide belt across the park, stretching from south of the Needles through the Maze and to the Elaterite Basin.
Brightly-colored oxidized muds were deposited on top the Cedar Mesa and ranged in color from red to brown. These sediments eventually became the slope-forming
Organ Rock Shaleformation and can be seen in the Land of Standing Rocks part of the park.
Coastal sand dunes and marine sand bars once again became dominate, creating the cross-bedded cliff-forming White Rim Sandstone. It is exposed as a topographic bench 1200 feet (365 m) below the top of Island in the Sky (thus earning its name) and along the White Rim Trail. A fossilized offshore sand bar made of the White Cliff Sandstone is also exposed in the Elaterite Basin. A tarry dark-brown oil called
elateriteseeps out of the structure, giving the basin its name.
The Permian sea retreated, which exposed the land to a long period of erosion and thus created a second unconformity.
Moenkopi and Chinle formations
Clastic red beds were laid down in shallow-water on top of the eroded
Paleozoicsurface early in the Triassic. These sediments were deposited on flood plains by streams on an expansive lowland that was slightly slopped in the direction of an oceanto the west. Mud built up in tidal flats to become the mudstoneof Moenkopi Formation. Examples of this formation, some that still show fossilized ripple marks and mudcracks, can be seen in the northern and western parts of the park.
Another period of erosion returned, creating a third unconformity. The brightly-colored shales of the slope-forming
Chinle Formationwere laid down on top of this eroded surface. Petrified woodfrom the Petrified Forrest Member of the Chinle is sometimes found at the base of Chinle slopes.
Glen Canyon Group
Glen Canyon Groupof formations includes (from oldest - lowest - to youngest) the
Kayenta Formation, and the
Navajo SandstoneThese formations are most prominently exposed in the western and northern sections of the park.
Triassic climates progressively became dryer, prompting the formation of sand dunes that buried dry stream beds and their flood plain. This sand became the cliff-forming several hundred feet (many tens of meters) high and red-colored Windgate Sandstone. Outcrops tend to run for hundreds of miles (hundreds of kilometers) with few breaks, creating an impediment to human travel.
For a time climatic conditions became wetter and streams cut channels through the sand dunes. Reddish-brown to lavender-colored sandstones interbedded with
siltstones and shales constitute the resulting ledgy slope-forming Kayenta Formation.
The youngest and therefore topmost formation in the Glen Canyon Group was formed after arid conditions returned to the region. A vast and very dry
desert, not unlike the modern Sahara, covered 150,000 square miles (388,000 km²) of western North America. Cross bedded sand dunes accumulated to great thickness, especially in the nearby Zion and Kolob canyons area (see geology of the Zion and Kolob canyons area), forming the buff to pale orange Navajo Sandstone. Navajo outcrops form cliffs, temples, and under certain conditions natural arches (such as Millard Canyon Arch) in the area.
A fourth unconformity was created by a period of erosion.
an Rafael Group
Mud flats developed on top of the eroded surface of the Glen Canyon Group, forming the
Carmel Formation. The massive cliff-forming Entrada Sandstonein turn was created on top of the Carmel. A long period of erosion stripped away most of the San Rafael Groupin the area along with any formations that may have been laid down in the Cretaceousperiod,
Starting 70 million years ago and extending well into the
Tertiary, a mountain-building event called the Laramide orogenyuplifted the Rocky Mountainsand with it the Canyonlands region. Even though the strata were uplifted thousands of feet (hundreds of meters) they were left at more-or-less the same horizontally. Uplift associated jointing did occur and has since influenced erosional patterns.
ground waterseeped into the salt beds of the Paradox Formation it carried away the topmost and more soluble salts, leaving gypsum. This process was so pronounced in The Grabens that the overlying rock collapsed into voids left by escaping salt.
Increased precipitation during the
ice ages of the Pleistocenequickened the rate of canyon excavation. Canyon widening and deepening was especially rapid for the gorges of the Green and Colorado Rivers, which were in part fed by glaciermelt from the Rocky Mountains. Alluvial fancreation landslides and sand dunemigration were also accelerated in the Pleistocene. These processes continue to shape the Canyonlands landscape in the Holocene(the current epoch) but at a slower rate due to a significant increase in aridity.
* "Geology of National Parks: Fifth Edition", Ann G. Harris, Esther Tuttle, Sherwood D., Tuttle (Iowa, Kendall/Hunt Publishing; 1997) ISBN 0-7872-5353-7
* Furuya, M., Mueller, K., and Wahr, J., 2007, "Active salt tectonics in the Needles District, Canyonlands (Utah) as detected by interferometric synthetic aperture radar and point target analysis: 1992-2002." Journal of Geophysical Research v. 112, B06418, doi:10.1029/2006JB004302
* [http://3dparks.wr.usgs.gov/canyonlands2/ USGS: Canyonlands National Park, A Photographic Featuring Park Geology]
* [http://www.americanparknetwork.com/parkinfo/ca/geology/ American Park Network: THE CREATION OF CANYONLANDS]
* [http://www.4corners.net/ccyc/text2.html 4corners.net: Geology of the Arches and Canyonlands National Parks]
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