Supersequences Of Discussion And Interpretance Of Hydrocarbons

Approximately 17 meters thick, Unit A defines the lowest third of the Juniata Formation. Fragments of marine fossils, including bryozoans, brachiopods, and gastropods, are commonly found in the bottom-most portion of this unit of structureless mudstone and quartz arenite. Quartz grains in the sandstone beds of Unit A are typically immature and fine-grained, though the sandstone packages tend to coarsen upwards. Though typically structureless, intermittent bedding of the sandstone and shale packages is observed in this unit, and some areas display

Next, we can see that the rock displays a subtle porphyritic texture with plagioclase comprising the phenocrysts. The overall texture of the surrounding groundmass is granoblastic equigranular. Under thin section we also see a weakly defined foliation evidenced in the preferential alignment of actinolite grains and to a lesser extent chlorite grains. Undulose extinction is also observed in quartz indicating the rock was subject to deformation. The normalized quartz, alkali-feldspar, and plagioclase (QAP) values of this rock indicate that it is classified as a grano-diorite according to the IUGS QAPF classification system which is consistent with the hand sample interpretation.

The Lynne deposit lies within the early Proterozoic Penokean fold belt of the southern province of the Precambrian Shield. The fold belt is divided into two major terranes in Wisconsin (Sims 1989). The first is the northern Penokean terrane, which contains major oxide facies iron formations and granitic intrusions (DeMatties 1989). The second major terrane, separated from the Penokean terrane by the Niagara fault zone, is the Wisconsin magmatic terrane, characterized by a volcanic island arc-basin assemblage (Sims 1989). This southern terrane lacks major oxide facies iron formations, but contains abundant tonalite-granite intrusions (DeMatties 1989). The Wisconsin magmatic terrane is further subdivided into the northern Pembine-Wausau terrane and the southern Marshfield terrane, which are separated by the Eau Pleine shear zone, a north-dipping subduction zone (Sims 1989).

First, we must examine the sedimentary formations; when they were formed, how they were formed, and what materials they consist of. About ninety-three to one hundred million years ago, the Western Interior Seaway rolled through the North American continent, eventually reaching the geographical area of today’s Mesa Verde National Park (National Park Service 2005). This sea deposited a thick, hard sandstone base that is called Dakota Sandstone, although this layer is not exposed in the park

Around the world our water supply is depleting. Our water is becoming contaminated making it harmful for both mammals and aquatic life. Today over one billion people go without adequate water supply and every fifteen seconds a child dies of waterborne illness. Sources of water that once supplied water to millions can no longer meet the supply and demand of the water need. Scientist predict that the amount of useful water will keep depleting greatly in the years to come. In the next couple of pages it will talk about both the geological and human reasons as to why are water supply is depleting.

This formation is a very fine grain Mississippian limestone. To test to see if this was the Bangor formation we used HCL and because there was a reaction we know its limestone. This formation could also be described as gray in color as well as an average thickness of 700 feet. We see the Bangor until stop eight, where we see a very different vertical bedding. Also different at stop eight is the outcrop no longer reacts with HCL. From this we gathered that we had moved into the Hartselle formation. In the Hartselle Formation, Mississippian aged sandstones are dominant. This particular stop had a large amount of jointing. After the Hartselle, we figured the Pride Mountain Formation would be next, however at stop nine we see the Maury Formation present. This stop focused on the rock located inside the creek. Because we were unable to go into the creek to get the strike and dips, we once again had to do a projected orientation. Also found on this stop were natural sulfur springs, easy to notice with the smell that it gives off. The Maury formation consist of Mississippian- Silurian aged shale. At the next stop, stop 10, we encounter the Ft. Payne formation. Although this area location was thickly vegetated, we were able to conduct the acid test and saw that the HCL reacts in some places but not all. From this we concluded that this was the cherty limestone of the Ft. Payne formation. The following stop, 12, we went up section and arrived at the Maury Formation once again. At the final stop, location 13, we see Ft. Payne Formation. All of the metamorphism and deformation in the southernmost Appalachians can be related to the movement of the thrust sheets and stacks (Higgins,

This Lower Keg River member was initiated by a rapid increase in sea level elevation flooding the salt plains of the Contact Rapids. Campbell (1987) described the Lower member of a dark micritic limestone, in a somewhat “euxinic” environment, containing bitumen and fauna such as brachiopods, crinoids, corals, stromatoporoids and gastropods. The unit can be locally dolomitized with a maximum thickness of approximately 50m. The Upper Keg River member was deposited during the restriction of marine waters by the Presqu’ile Barrier reef into the Elk Point Basin (Campbell, 1987). The interior of the basin contains Upper Keg River pinnacle reefs, banks and platforms. Campbell (1987) noted the spatial differences in the type of carbonate deposition within sub-basins; areas from the Peace River Arch to southern Alberta show a fringing carbonate platform, while the Rainbow, Zama and Shekelie basins contained the majority of the

The South Brae oilfield is mainly Kimmeridgian to mid-Volgian in age, however on some accounts it may possibly be of Oxfordian (Turner et al, 1987). The oilfield is heavily developed along the western, fault-bounded margin of the South Viking Graben approximately 161 miles NE of Aberdeen flanking Fladen Ground Spur (see Fig.1). The Upper Jurassic rifting of the South Viking Graben encountered, pronounced movement along the western bounding fault as syn-rift extension proceeded (Harris & Fowler, 1987, Gregory et al, 2007). Syn‐tectonic deposition throughout the Jurassic ensued the formation of a distinct sediment wedge thinning eastwards into the basin, outlining the main phase of fault movement down the boundary fault (Roberts, 1991). As a result, the Brae oilfields are a series of

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

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,

Main oil deposits are in Neuquén Basin, Gulf of San Jorge, Northeast, Austral and Cuyana basins. Vaca Muerta, which is located in Neuquén Basin, accounts for 60% of 27 billion barrels of shale oil and it is in preliminary stage of development and remains vastly untapped. 7 Analysts estimate that YPF is expected to need up to $200 billion to fully exploit the formation. XTO plans to invest up to USD13.8bn more to drill 556 horizontal wells in Vaca Muerta.

This review is on the scientific paper ‘Architecture of an active mud-rich turbidite system: The Zaire Fan’ by Droz et al [2] published in 2003. The main purpose of this article was to take the seismic results from the ZaïAngo program, acoustic imagery and bathymetry information and present the architecture of the Zaire Fan.

The Sarir “C” field is a higly prolific hydrocarbon producing field in North Africa (figure1) with an estimated ultimate recovery of about 6.5bbl of oil in place (Carmalt et. al; 1986) It was discovered in Southern Cyrenaica in 1961, forms part of three complex fields(fig3), and has other significant fields like the Amal, Defa, Augila, Hateiba, Messla, Bu Atifel, lying in the same Sirte basin.

Absract: The Miocene carbonate – siliciclastic deposits are widely exposed along the stretch of Qabilt Ash Shurfah to Wadi Zaqlum sections, Sirte Basin, NW Libya. These deposits overlies unconformably the Late Cretaceous Sidi As Sid Formation and overlain unconformably by Quaternary clastic deposits. Three stratigraphic sections were investigated namely, from north to south: Qabilat Ash Shurfah, Ras Al Shaqqah and Wadi Zaqlum sections. Lithostrtigraphically, the Miocene sequence could be differentiated into two main rock units representing shallow deposits with relatively intermittent deep marine incursions. These are from base to top as follows: 1- Al Faidiyah Formation and 2- Al Khums Formation (represented at lower part by An Naggazah Member followed upwards with Ras Al Mannubiyah Member. Detailed foraminiferal investigations led to the recognition of three foraminiferal zones from base to top: Elphidium macellum / Miogypsina intermedia and Globigerinoieds trilobus zones covering Al Faidiyah Formation and assigned it to early Miocene (Burdigalian) age and the Borelis melo melo zone which includes Al Khums Formation and dated it to Middle Miocene (Langhian to Early Serravallian) age. Detailed microfacies analysis of the rock units led to the recognition of eleven microfacies types indicating that the Miocene sequence was deposited in transgressive – regressive cycles ranged from near shore, warm shallow inner to middle shelf marine environments with development of reefal

A seismic section shows the appearance of the SGA-A across (Figure 23) that goes across a salt dome inducing faults (Figure 23b) that go through the Chalk group and segments the accumulation of gas within the shallow sub-section below Quaternary incised Tunnel Valleys. There seems to be a seismic indication of a vertical migration of hydrocarbons along faults reaching the SGA - A accumulation that may indicate migration pathways for fluids above a salt diapir – C.