The Field Classification Of Niger Delta Basin

In 1956, oil was discovered in the Nigerian state of Bayelsa, less than 50 miles south of the Delta state line. In 1958, the Delta started producing oil at around

Rodinia started to rift around 750 to 600 million years ago and the Iapetus Ocean opening up as seen in Figure 1, the Swift Run Formation with Grenville, volcanic debris and ash material produced the Catoctin Formation that contains flood basalts supporting Shenandoah. With modern day East Africa rift and Red Sea curst stretched, this allowed flood basalts and rhyolite seep through the ocean floor and eventually made its way to the surface.

The Waucoba Wash Quadrangle, California cross section begins with the deposition of the Cambrian layers such as the Campito Formation, Poleta Formation (upper and middle members and undivided), Harkless Formation, Saline Valley Formation (lower and upper members), Mule Spring Limestone, Monola Formation (lower and upper members), and the Bonanaza King dolomite (dominantly limestone and undivided). These Cambrian rocks are followed by rock layers from the Devonian period, thus meaning that an unconformity occurred between the layers. The Devonian dolomite rock layers include the Hidden Valley dolomite and the Lost Burro Formation (cherty dolomite). These are followed by the Mississippian

Devonian until the Cretaceous. Hildebrand (2009, 2013) cast doubt the back thrust interpretation of the western US Cordillera.

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

Another rifting phase started in the early Jurassic around Pliensbachian or Toarcian (Chongzhi et al., 2013; Geoscience, 2014; Tindale, Newell, Keall, & Smith, 1998). Exmouth, Barrow, Dampier and Beagle Sub-basins were created until Middle Jurassic (He, 2002; Tortopoglu, 2015) and oceanic crust was laid down to form the Argo Abyssal Plain in Late Jurassic around 164-160 Ma during the Callovian to Oxfordian then followed by the Gascoyne and Cuvier Abyssal Plain in Early Cretaceous around 125 Ma (Fullerton, Sager, & Handschumacher, 1989; Müller, Mihut, & Baldwin, 1998). Passive margin was established in North West Shelf. Rifting phase of the basin transformed into sagging phase post breakup thermal subsidence when Gondwana breakup took place during Valanginian early Cretaceous around 134Ma. During the Campanian late Cretaceous, rifting along the Australian southern margin triggered the basin inversions and wrench reactivation of basin structures on NW Shelf. These movements arose the Barrow Island above sea level and formed Novara, Resolution and Exmouth Plateau Arch in Barrow, Dampier Sub-Basins and Investigator Sub-Basin (Figure 1) (Longley et al., 2002; Sinhabaedya,

The Crato Formation lithologies were most likely deposited when there was a marine transgression; which is what the Cretaceous period is renowned for (Hu et al. 2012). The build-up of laminated limestones and different lithologies in the stratigraphic column could suggest that it was a lagoon depositional environment (Martill and Frey, 1998).

Deposition of sediments began in the basin during the Cambrian era, but subsidence and basin filling occurred the most during the Ordovician,

This document describes in detail the organic petrology and maturation of the Bakken Formation located in the Williston Basin. This report is organized into five sections. Section I will introduce the Bakken Formation in reference with the Williston Basin. It will also address sedimentary and structural aspects of the Bakken Formation. Section II outlines the processes that formed the Bakken Formation that occurred during the Devonian/Mississippian age. Section III will summarize organic components and influence within the Bakken Formation. Furthermore Section IV will address the nature of inorganic constinuents that influence the Bakken Formation. Section V will discuss production history and current production of oil and gas found within

Literature suggests that the Wandagee Formation conformably overlies the Quinnanie Shale (Mory & Backhouse, 1997). These two sections were most likely deposited within a marine shelf, perhaps below the storm water wave base (notebook page 33). The Quinnanie, displaying no trace fossils or bioturbation and generally massive in structure may suggest that it was deposited at greater depths than the Wandagee Formation or it may suggest a cycle of shallowing and deepening waters, due to tidal influences. The Quinnanie representing deepened waters. Its more organic make-up may also indicate that it was deposited at greater depths than the Wandagee. The Wandagee Formation contains a vast number of structures that indicate a shallower environment than the Quinnanie. Whilst still being deposited below the storm water wave base, it may be possible that it was deposited during a shallowing oscillation. Trace fossils that were burrowing indicate shallower waters, the stratigraphic log demonstrates these relationships, figure 22).

Glaciation that are widespread can be identified based on the subglacial tillite, which is a thick layer of sediments that settle down beneath glaciers or ice caps. On top of this subglacial tillite layer is deposited marine carbonate, also known as cap carbonate. Based on their paleolatitude designated by glacial sediments’ paleomagnetism, it can be determined that these deposits are from equator region. The interaction between two types of sediments, marine (like carbonate) and subgacially deposited sediments, indicate that the glaciers had approached marine coastlines.

The structure of a basin is important for subsidence as well as accumulation of sediments that influence coal deposition within the basin. The Raton Basin is a foreland basin which formed during the Laramide Orogeny (Rooper et al., 2006). The Raton Basin as a whole covers approximately 4,000 square miles in southeastern Colorado and northwestern New Mexico (Flores and Bader, 1999). The Raton Basin is an elongate asymmetrical basin, where the sedimentary rocks are very steep, overturned, as well as faulted, on the east of the Sangre de Cristo Mountains (Keighin, 1994). The basin is bounded on the west side by the Sangre de Cristo Mountains, on the northeast side by the Apishapa arch, and on the southeast side by the Sierra Grande-Las Animas arch (Flores and Bader, 1999). The Raton Basin

Burchfield and Royden (1991) cast doubted the island arc-collision hypothesis because: 1. the arc west of the North American continent and its structures seem more to face west rather than east. 2. The Havallah basin sediments deposited before and after the emplacement of the Roberts mountains allochthon. 3. Deposition occurred in a paleogeographic location that should have been occupied

As previously mentioned the project is expected to cost more than $3.7 billion and will be funded by the World Bank and the International Financial Corporation. The total costs have two major sections i.e. the Field System of more than $1.5 billion and the Export System at approximately $2.2 billion. The Field System is geared towards the development of Chad's Doba oil fields that includes the construction of related infrastructure and facilities and drilling of around 300 wells. The Export System incorporates the construction of a 670-mile, 30-inch pipeline from Chad's Doba oil fields to Kribi's Atlantic coast in

Drilled by the Transocean Leader, the 6705/10-1 well reached a vertical depth of 3,775 meters below sea. The reservoir is located in Upper Cretaceous reservoir rocks, and found gas in rocks with good reservoir properties.