Callytharra Formation Essay

Sedimentary rocks interpret dinosaur habitats through encased environmental structures of the past. Through sedimentary rocks, paleoecologists’ can examine the arranged formation of sedimentary structures to specify what type of environment the dinosaurs’ lived in. An example of a specific sedimentary rock structure can be seen through formed weathering and ripple marks by how wind and sand formed distinct patterns in the past layered sediment. These arrangements provide interpretations on the structure of the sediment and the habitat of encased fossils, through modern day comparisons

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

Oil and Gas exploration has been an ongoing project in the Raton Basin, but a quite unsuccessful one at best. The Raton Basin is primarily a flood plain paludal deposit which is not ordinarily an ideal unit to recover oil or gas from (Speer, 1976). The sandstones within the Raton are predominantly coarse grained, poorly sorted, fluvial sandstones which have been shown

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 440 million year old Georgian Bay Formation is largely composed of fossiliferous grey-black shale (L1R). It also consists grey fine-grained limestone, sandstone and green/grey siltstone interbedded with green/grey and blue/grey shales (Bond et. al. 1976). The frequency of hard rock units increases toward the top of the formation. Recurrent tropical storms across the Ordovician seas caused the formation of shady, thin limestone with wave ripples on top. Numerous fossils can be found in the siltstones and limestone including molluscs, crinoids and gastropods

These Paleozoic rocks are steeply plunging sandstones and siltstones, with a little event of limestone at Lilydale - the Early Devonian Lilydale Limestone. The Silurian rocks were stored in profound water, while the Devonian rocks, which are exceptionally fossiliferous, appear to have been stored in shallower water. These Silurian and Devonian rocks were folded into a progression of anticlines

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,

What is Marcellus Shale? It is a marine sedimentary rock buried thousands of feet beneath the earths surfaces. Sedimentary rock is one of the three main rock groups and is formed in four main ways: by the deposition of the weathered remains of other rocks; by the accumulation and the consolidation of sediments; by the deposition of the results of biogenic activity; and by precipitation from solution. Marcellus Shale is found throughout the Allegheny Plateau region of the northern Appalachian basin of North America. It stretches from upstate New York south through Pennsylvania to West Virginia and west to parts of Ohio. Marcellus shale was named after a town in upstate New York, the rock itself is millions of years old, formed from mud and other natural materials. Its made up of the formation of black shale that may contain lime stone beds and concentrations of iron pyrite and siderite. The Sedimentary beds and structure is very well developed. Lighter colored shales in the upper portion of the formation tend to split into small thin edged fragments after exposure. The fragments may have and leave rust stains from exposure of pyrite to air, and tiny gypsum crystals from the reaction between both of the fragments pyrite and the limestone particles. Fresh exposures of the pyriteiferous shale may develop the secondary mineralization of orange limonite and the pale yellow efflorescence or bloom of sulfur, associated with acid

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).

At the intersection of Neva Road and U.S. 36 we examined three different members, the Smoky Hill, Fort Hayes, and Codell, which belong to two different formations, Niobrara and Benton. The Smoky Hill and Fort Hayes belong to the Niobrara formation while Codell belongs to the Benton Formation. In the Niobrara’s Smoky Hill and Benton, Inoceramid clam (giant clam) fossils were found. These three formations are of Late Cretaceous.

The central idea of this article is the study of the Storr Lochs Monster and how its study can be applied to more fossils being found and studied in Scotland and in the Middle Jurassic Period. The author states that very few fossils can hunted down and studied in Scotland, and in the rest of the world fossils from the Middle Jurassic Period, when this creature lived, are very rare. Steve Brusatte, the Paleontologist from Scotland, said "We know that quite a lot was happening during the Middle Jurassic Period" he also said "It's frustrating because it seems like an active period in evolution but one with very few fossils" and also inputted that he hopes after the study of the Storr Lochs monster that an increase in Scottish paleontology can

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,

1. The author chose to focus on 375 million year old rock because the transition from fins to necks and limbs occurred then. The scientists knew that any time later than this and they would find lots of animals with limbs. But if they searched earlier than this time then there are only fish without necks. When the fish were evolving they evolved necks before they evolved limbs so this was a good sign in chronology. Sedimentary rocks are the best types of rocks for fossil due to their gradual pressure and low amounts of heat. Sedimentary rock is also found in lake beds and streams, where fish and aquatic wildlife are most likely to live.

Cape Lieper and Cape Ingersoll formations: They are part of Ryder Gletscher Group. They are mainly composed of dolomites and other carbonates rocks and they overlie Dallas Bugt Formation with thicknesses of up to 40m (Higgins et al, 1991). Other smaller formations within the Ryder Gletscher Group include Lower-Middle Cambrian wulff River and Cape Wood formations and they are mainly dominated by irregular bedded micritic limestone with thickness of up to 150m (Higgins et al, 1991). Cape Kent Formation of Lower Cambrian which was probably formed in a high-energy depositional environment in shallow water contains oolitic limestone with thickness of up to 10m

By testing sediment and recording whether it was deposited under conditions of normal polarity and then measuring successive layers, we can build a time chart. By matching different charts from different areas with similar fossils, a more global correlation can be made.