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This section highlights the map units (i.e., rocks and unconsolidated deposits) that occur in Timpanogos Cave National Monument and puts them in a geologic context in terms of the environment in which they were deposited and the timing of geologic events that created the present landscape.
The rocks and geologic structures and features present in Timpanogos Cave National Monument record a vast span of Utah’s geologic history from the time before plants or animals existed, through episodes of mountain building and extension of the earth’s crust, to formation of the caves, and excavation of American Fork Canyon (figure 9).
The oldest rocks provide a rare glimpse into the tectonic
setting of the Proterozoic Eon (figure 10 - below). The earliest
event preserved and recorded by rocks exposed in the
Timpanogos Cave quadrangle was the deposition of the
layers of sand and mud from nearby highlands. These
deposits now form the uppermost part of the Big
Cottonwood Formation. This deposition was
interrupted by a prolonged period of glaciation during
which massive tongues of ice extended into the area and
deposited great bodies of poorly sorted glacial till (now
tillite, the lithified equivalent of a jumbled assortment of
rock sizes and types, Mineral Fork Tillite). This ancient
glaciation was followed by local tectonic uplift and
subsequent extreme erosion. These eroded surfaces were
Late Proterozoic rifting created a new continental margin along western North America. During the Late Precambrian through the Cambrian, thousands of feet of shallow- water, marine sediments accumulated along a passive plate- tectonic margin on the western side of the Transcontinental Arch, an upland that stretched from northern Minnesota southwestward across Nebraska, Colorado and northwestern New Mexico (Speed 1983; Sloss 1988; Graham et al. 2002). The area that is now Timpanogos Cave was approximately located along the shoreline in this paleoenvironment.
Throughout the Paleozoic Era, Europe, Africa, and South America were approaching North America as the two great landmasses, Laurasia and Gondwana, collided. The ancient continent of Gondwana included Australia, Antarctica, Africa, South America, and India south of the Ganges River, plus smaller islands. Laurasia, located in the northern hemisphere, contained the present northern continents (Graham et al. 2002).
In the early Cambrian Era, the region again underwent an uplift and erosional event. Following the uplift, the region subsided and an ancient sea advanced bringingwith it the depositional environments necessary to capture vast amounts of sediments including the sand for the Tintic Quartzite, the mud for the Ophir Formation, and as the sea deepened, the limy ooze that lithified into the Maxfield Limestone.
This progression of units records the deepening of the sea during progradation in the area. During this time, prior to the evolution of land plants, loose sediment was continually reworked by wind and fluvial processes. Late Precambrian, shallow- water sediments thicken across Utah, from east to west, until they reach a thickness of 3,000- 6,000 m (10,000 to 20,000 ft) in western Utah (Hintze 1988; Graham et al. 2002).
In Utah, Cambrian strata are more widely distributed
than deposits of any other time (Hintze 1988). Thinly
laminated stromatolitic dolomites and mottled muddy
limestones in the Middle and Upper Cambrian of Utah
were deposited in very shallow marine waters that
deepened westward. A wedge of Cambrian Period
sediments thickened from eastern to western Utah
approaching a total thickness of 3,700 m (12,000 ft) near
the Utah/Nevada state line (Hintze 1988). The lateral and
vertical distribution of marine fossils, primarily trilobites,
paints a picture of the Utah area in Cambrian times with
a shoreline slowly migrating eastward from Nevada to
central Utah during the Early and Middle Cambrian. By
Late Cambrian time, marine waters covered virtually the
Whether similar deposition continued into the Ordovician, Silurian, and Devonian periods is not known because no sedimentary rocks representing any of those periods have been found in this part of the Wasatch Mountains. If any were deposited, they have since been removed, together with much of the Cambrian age rocks in some places, during the long erosion interval that is recorded in the profound unconformity at the base of the Mississippian age rocks (Baker and Crittenden 1961).
From elsewhere in Utah, rocks recording broad
carbonate shelves evolving into open and restricted
marine environments and later near- shore marine
In the Middle Devonian Period (about 401 Ma), the first compressive pulses of the Antler Orogeny in the west and the Acadian Orogeny in the east (part of the Appalachian Orogeny) began, as landmasses accreted onto both the western and eastern borders of North America.
To the west of Utah, a subduction zone formed and lithospheric plates collided against one another and their rocks were bent, buckled, folded, and faulted into a north- south trending pre- Rocky Mountains mountain range stretching from Nevada to Canada. The Roberts Mountains Thrust marks the easternmost thrust sheets generated by the Antler Orogeny.
During orogenic events, great sheets of rocks measuring tens to hundreds of kilometers in width and length are stacked on top of one another. The weight depresses the land in front of the thrust sheets, or foreland, and causes the foreland to subside into a foreland basin. As the highlands to the west were thrust above sea level at the beginning of the Mississippian, warm shallow marine water flooded the foreland basin and spread over eastern Utah giving rise to an extensive carbonate platform.
Found in the thick Mississippian marine limestones are fossils of animals that lived in normal marine salinity such as brachiopods, trilobites, corals, bryozoans, crinoids, fish, foraminifera, and conodonts (microscopic structures of an extinct animal that are excellent relative- age indicators). The sea became shallower during the regression that followed the Antler Orogeny, however, and habitats dwindled so that marine life became more restricted. Eastern Utah became a broad karst plain of shallow- marine sandstone and micrite (carbonate mudstone), and by the end of the Mississippian, the area was again exposed to subaerial erosion (Poole and Sandberg 1991; Graham et al. 2002).
During Early Mississippian and much of Late
Mississippian time, layers of carbonates, intermittently
alternating with sandy sediments, accumulated at
As the sea became shallower during the regression that followed the Antler Orogeny and the Kaskaskia Sequence came to an end, the shoreline again receded from the Transcontinental Arch and by early Pennsylvanian time, soils were beginning to form in low lands and the higher areas were being worn down by erosion. Much of the Oquirrh, Park City Formations, and possibly all of the Great Blue Limestone and Manning Canyon Shale may be missing to the north of the Timpanogos Cave quadrangle due to this erosion.
Coincident with Pennsylvanian tectonics (figure 12) was a global climate shift from the warm humid environment of the Late Mississippian to a much more arid environment in the region of Utah during the Early Pennsylvanian (Rueger 1996).
As the Ancestral Rocky Mountains formed, the Ouachita-Marathon thrustbelt, the Anadarko Basin, and other Permian basins developed to the southeast and the Oquirrh Basin subsided to the northwest (Jordon and Douglas 1980; Peterson 1980; Kluth 1986; Gregson 1992). Vertical relief in some of these basins relative to sea level (i.e., the Oquirrh and Central basins) was greater than the emergent mountains, and the Ancestral Rockies may have reached as much as 3,000 m (10,000 ft) of relief.
The thick sedimentary sequence of the Oquirrh Group in the Timpanogos Cave area represents the variety of shallow marine and arid near shore environments present in the Oquirrh basin area throughout the Pennsylvanian, including eolian dunes, marine shelf, open coastal area, intermittent fluvial systems/channels, and protected waters (Konopka 1982). The Oquirrh Basin along with all of these paleotectonic structures probably reflect a similar tectonic stress field controlled by Precambrian structural weaknesses and the compressional stress- field that evolved with the assembly of Pangaea (Tweto 1977; Kluth 1986; Ross and Ross 1986; Gregson 1992).
Continuing from the Pennsylvanian, during the middle part of the phase of the Park City Formation deposition, in Permian time, shallow stagnant seas persisted over most of the Timpanogos Cave region. These seas provided the arid/evaporitic conditions required for deposition of phosphate and other salts (Baker and Crittenden 1961). Across the globe, the Permian Period was a time of dramatic environmental change. The Permian equator was oriented southwest- northeast through Wyoming and eastern Utah. An arid climate prevailed in this western part of the supercontinent Pangaea and resulted in restricted marine evaporitic conditions over much of the cratonic shelf seaway (Peterson 1980; Graham et al. 2002). These shallow seas filled basins such as the Oquirrh and Paradox Basins, with incredible accumulations of sediments and salts.
From rock deposits around the globe, geologists have
documented the third, and most severe, major mass
extinction of geologic time at the close of the Permian.
Geologists think a comet, about 6- 13 km (4 to 8 mi) in
diameter, collided with the Earth (Becker et. al. 2001). The heat and shock waves generated from such an
impact may have triggered vast volcanic eruptions that
spread lava over an area two- thirds the size of the
United States. Imagine, for example, basalt flows
covering the area from San Francisco to St. Louis and
Seattle to New Orleans. The amount of ejecta, volcanic
ash, and toxic gases from such an event would have been
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