A Survey On The Creek Geological History

deposit is the Marcellus Shale, located in the northeastern part of the US, centering on the state

The cataclysmic eruption which caused the collapse of the caldera and the deposition of the Bishop Tuff was an explosive, fast event. It ejected coarsely porphyritic biotite rhyolitic ash and viscous lava with an approximate silica content of 76 percent. The total ejecta came to about 600

A period of volcanism resulted in igneous intrusions within the Raton Basin-Sierra Grande Uplift Province that was sourced from the upper mantle about 26. 6 billion years ago and is associated with parallel dikes and sills (Higley, 2007). Igneous rocks are common within the Raton Basin and include Tertiary dikes and sills that range in age from 6.7 to 29 5 million years ago (Flores and Bader, 1999). One of the main differences between dikes and sills is that dikes are longer lived magma conduits and sills are features that form when magma is in neutral buoyancy with the surrounding rock (Rooper et al., 2006). These volcanic events are associated with hydrothermal alteration of coal within the basin (Higley, 2007).

At both Cienega Amarilla and Cottonwood Canyon, stratum VI consists of a 0.2–1.3-m-thick surface layer of bedded, fluvial sand locally with a very weak soil profile (Figures 3 and 4; Table 3). No radiocarbon dates or plant macrofossils are associated with stratum VI, but radiocarbon dating of underlying stratum V alluvium indicates that stratum VI post-dates ~300 cal BP. Stratum VI alluvium appears to represent arroyo fan deposits associated with historic period arroyo cutting. Accounts from ranchers indicate that arroyo-cutting in this area occurred in the late 1800s or early 1900s, consistent with widespread arroyo formation across the southwest U.S. at this time (Waters and Haynes, 2001).

Many millions of years ago the Sierra Nevada was filled with ocean water until sediments began collecting and formed mountain ranges. Over a large period of time, the mountains began to wear out and became immersed in the ocean once again. Many different particles and materials began to make layers and created the first mountain system. After the Jurassic era, “…new strata were folded and crumpled and invaded by molten granite from below” (Beatty, 1943). A large

In addition, per my knowledge none of the western US geologists have documented passive margin deposits as young as of upper Paleozoic age or younger. Therefore, Hildebrand (2009, 2013) hypothesis faces deficiency to explain the thrusting of Roberts Mountain and the emplacement of the Proterozoic rocks over the rocks of Lower Paleozoic age.

These rocks grade abruptly northward into a marine geo-synclinal facies up to as much as 6,000 feet thick in the Las Vegas sub-basin. The Magdalena Group is missing from the Cimarron arch, but it most likely present in the western part of the northern Raton Basin. Orogenic debris of the Sangre de Cristo Formation of Pennsylvanian and Early Permian age was derived mainly from the San Luis uplift, filled the Rowe-Mora and Central Colorado basins, and lapped onto Precambrian rocks of the other bounding uplifts. The Sangre de Cristo Formation is 700-3,500 feet thick at the south, and 6,000-9,500 feet thick at the north (Baltz 1965).

The Tuscarora formation is in the Silurian age, located in Pennsylvania, mostly composed of quartzite, and is secondarily composed of sandstone. Its thickness is 150-200 feet and is in the lower part of the Silurian age. The Tuscarora formation is in the Clinton group. One member would be Castanea located at the top of the Tuscarora Formation. The depositional environment is, as we know it, a continental shelf of some sort of marine zone because of sediment structures like fossils and cross-bedding. The Tuscarora formation is mainly non-porous and neither

The third and topmost layer of geological deposits is the Pleistocene sediment, from the Quaternary Period, which can date up to 1.7 million years old (L). This layer contains sediments of Holocene from ten thousand years ago as well as Pleistocene from 1.7MY to 10KY(L). Continent wide ice sheets deposited the glacial sediments during numerous ice ages (DVLR) and can be seen at Don Valley Brickyard. The York Till is above the bedrock, and was left 135,00 years ago by an Illinoian ice sheet. Above the till is the 80,000-year-old Don Formation that was caused by the Sangamon Interglacial, and indicates climate change by the alternation of sand and mud. Above the Don Formation, all other deposits are from the Wisconsin Glaciation. The Scarborough Formation consists of clay and then sands, and was formed 60,000 years ago. Above this is the Sunnybrook Drift and the Thorncliffe Formation from 45,000 years ago consisting of seminary

“Sedimentary Rocks.” Living with Volcanic Past. http://vulcan.wr.usgs.gov/LivingWith/VolcanicPast/Notes/sedimentary_rocks.html (accessed May 23, 2012). Stafford, Orin Fletcher. The Mineral Resources and Mineral Industry of Oregon for 1903.

is characterized by increased sediment yield from hillslopes destabilized by vegetation change resulting from climatic warming and drying (Bull, 1991; McFadden and McAuliffe, 1997). In the Zuni Salt Lake piedmont area, vegetation change and hillslope runoff-sediment yield during this transition would have been further disrupted by pyroclastic airfall and wildfires associated with eruptions at Zuni Salt Lake maar and Cerro Pomo cinder cone during the ~13.5¬–11.5 ka interval (Appendix A). Rates of fan deposition immediately after the eruptions were probably quite accelerated; however, by ~10.3 ka (the age of the oldest piedmont fan deposits exposed), fan aggradation was not particularly high (~2 m/ka). Early Holocene valley floodplains in the Carrizo Wash watershed, at least after ~9 ka, are characterized by slow aggradation of clay-rich alluvium. This suggests that most sediment eroded from the upland slopes during the early Holocene was stored on piedmonts as alluvial fan deposits, with a relatively minor amount of fine sediment reaching the valley floors. Early Holocene floodplains were therefore probably relatively stable, slowly aggrading, and densely vegetated

This geologic data has shown that the basin contains sedimentary rocks of Late Cambrian to the Tertiary age, and is more than 15,000 feet thick. The depo-center of the Williston Basin started its development during the early Paleozoic era in the northwestern part of North Dakota. The sedimentary rock thickness decreases to less than 10,000 feet in eastern Montana and to less than 5000 feet along the basin margin (Peterson & MacCary, 2009). Carbonate deposition occurred throughout the area during the early to middle Paleozoic era and changed to clastic deposition in the late Paleozoic era. During the Paleozoic era, more than 8000 feet of marine sediments accumulated at the basin center, but the shape of the basin remained the same. The basin depo-center has however shifted slightly over time. The Williston Basin sedimentation in the lower and middle Paleozoic is dominated by carbonates and evaporates, whereas upper Paleozoic and younger rocks are largely siliciclastic with small admixtures of carbonate (Anderson & Gerhard,

Permin Land Formation: It is dominated by medium-to fine-grained well-sorted and rounded sandstone (Higgins et al, 1991). There are also dolomite and siltstone interbed and features like wave-ripple lamination, flat and low-angle lamination as well as shallow trough & tabular crossbedding are also present indicating a shallow marine depositional environment. The thickness of Permin Land Formation is up to 50m (Higgins et al, 1991).

shallow marine sandstones. The Rannoch and Etive consist of V.fine to coarse grained sand which was deposited in shore face and marginal marine settings. Within the Ness dominance of shoreface and fluvial channel facies is attributed to the delta plain setting during this period. The Ness has a lower net to gross than the other formations and is composed of fine to coarse grained sand, mudstone and coals. The Tarbert was deposited in a shallow marine environment and is composed of fine to coarse sand.

The Tumalo tuff was formed by one episode of flow and has a well developed basal 2a layer. Variations in the distal character of layer 2a are thought to represent complex flow conditions in the head of the Tumalo tuff ash flow. Mixed pumices also are found in proximal Tumalo tuff deposits. The Bend pumice and Tumalo tuff are peraluminous and rhyodacitic. Within analytical uncertainties, they have identical major, minor, and trace element abundances. Both contain fresh hornblende in the mineral assemblage Plg + Opx + Mgt + Zr + Ap. The hornblende appears to have been a liquidus phase and indicates that the rhyodacite evolved under high pressure, hydrous conditions. A hight La to Ce ratio and a strong negative Eu anomaly in the B-T rhyodacite further indicates that the Bend pumice and Tumalo tuff evolved under physical conditions quite distinct from other rhyodacites in the central Oregon High Cascades analysed by Hughes (1982). Mixed pumices in the Tumalo tuff represent the incomplete mixing between Bend-Tumalo rhyodacite and a dacitic