The Arkoma Basin

For the first paragraph we shall have a quick focus on the geological history of the area of Kalamazoo. The main deposits and formations of the Kalamazoo area where formed during the Wisconsin glaciation period. Now the deposits are actually due to two lobes during this period, the lobes are the Lake Michigan and Saginaw lobe. Kalamazoo is actually know as a “reentrant district” due to the presence of two different lobes materials. During the middle of the Wisconsin Ice Age the Lake Michigan lobe was extending southeastward, while the Saginaw lobe was extending southwest. With the meeting of the two lobes an interlobate developed between the terminals of the lobes. It is also thought that the two lobes overlapped each other. With the Saginaw lobe covering the Kalamazoo area first and then retreating while the Lake Michigan lobe then covered the area. There are also some bedrock formations in the area as well, these formations were established during

Found in the Appalachian Region, the Juniata Formation extends from central-southern Pennsylvania to Tennessee (Davies 2010). Though the thickness of the Juniata Formation is far from constant across its lateral extent, it is approximately 2000 feet thick in northern Pennsylvannia and thins towards the southwest (Crowder 1980). Named for the Juniata River running through southern Pennsylvania, this formation consists of sediments from the Taconic Orogeny in the late Ordovician period (Crowder 1980). Figure one displays the characteristic layers of alternating red sandstones and shales, which are divided into three distinct units (Darton

The Slate Belt bioregion is nested within the Great Valley Section of the Valley and Ridge Province that was formed by thrust and fault folding during the Late Ordovician period through and Late Paleozoic era.(Bailey,1992; Geyer, 1979;Van Diver, 1990). During this time Taconian

Starved rock and St. Peter Sandstone are an erosional remnant of Ordovician period. These remnants contain Pennsylvanian clastics that survived the washing out of the Illinois River at the end of the Ice Age. Evidence for swift, turbulent, and deep water includes gravel bars and erosional features as high as 160 feet above the current level of the river, massive cross bedded sand, and gravel deposits along the river course.

The Colorado River Basin starts in the Rocky Mountains and cuts through 1500 miles of canyon lands and deserts of seven US states and two Mexican states to supply a collection of dams and reservoirs with water to help irrigate cropland, support 40 million people, and provide hydroelectric power for the inland western United States [1,2]. From early settlement, rights over the river have been debated and reassigned to different states in the upper and lower basin; however, all the distribution patterns lead to excessive consumption of the resource. In 1922, the seven US states signed into the Colorado River Compact, which outlined the policy for the distribution rights to the water [3], however, this compact was written during an exceptionally

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).

When the Ouachita Mountains were created, the sediment carried by rivers was sent downward and eroded again. Swamps overfilled with clay and plant remains ended up buried. These remains become valuable products of the valley today- coal and natural gas. This region varies between narrow ridges and flat-topped mountains with rolling or hilly plains split by the river. The Arkansas River was an important means of transportation between the mountains. Present day Batesville, Fort Smith, Clarksville, Russellville, Morrilton, and part of Conway are within this

The basin begins near Simmesport, La., and stretches 140 miles southward to the Gulf of Mexico. Currently, the Atchafalaya Basin is bound by natural ridges formed by levee building along active and abandoned courses of the Mississippi River.

The book RISING FROM THE PLAINS (1986) talks about how the Rocky Mountains had developed in Wyoming, McPhee was accompanied by David Love during this book. It was the first of the books “Annals of the Formal World” that talked about the effects of human beings, and how it complicates science. The book concentrates on how different parts of geology directly affects

The Copper Basin of southeastern Tennessee is an area that is climatically unique with a rich history rooted in copper mining. It is thought that man is responsible for the total destruction of the environment over this large area, but it is mostly contributed to the exclusive location. The Copper Basin was susceptible to negative environmental effects due to its topographical, geological, climatic, edaphic, and meteorological location. However, the copper mining had a transformative effect on the surrounding lands that of which are still recovering.

The Southeastern Native Americans lived in the area of the United States imperfectly defined by being below Kentucky and Virginia and east of Arkansas’s and Louisiana’s border with Texas. This is imperfect because the Caddo, Atakapans, and the Tutelo crossed these borders. The environment was composed of Coastal Plain, Piedmont, and the South Appalachian Mountains. The coastal plains were comprised of pine forests, rivers, bayous, swamps, and floodplains. Piedmont had rolling hills, hardwood forest, many rivers, and fertile valleys. Lastly, at the South Appalachian Mountains there existed narrow, silty valleys, forests, and many deposits of stone (Sutton, 2012). The Southeast provides a decidedly beneficial climate and environment to sustain

Analyses from 7,300 years ago at the Hawken site in northeast Wyoming do not match with the hypothesis of a dry Altithermal, though this may be limited to the site from which the data was collected, and not representative of the entire High Plains area (Lovvorn, Frison, and Teiszen 2001).

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,

Stratigraphy: The Augustine-Seldovia arch, which is oriented east-west, transverse to the main structural trend of the basin, separates the forearc basin into two depocenters. (ADNR 2006). The northern depocenter in upper Cook Inlet is dominated by roughly 25,000 feet of Cenezoic strata. The southern depocenter in lower Cook Inlet and Shelikof Strait contains a thinner Cenezoic section superimposed on top of 36,000 feet of Mesozoic strata.

The Wells Creek structure was formed by a meteorite impact in Cumberland, Tennessee (36°〖23〗^ ' N,87°40 'W) which is the northern part of Middle Tennessee. This region is known as the highland rim. The younger and older strata is exposed in two areas in the highland rim which means the older sediment has been eroded and much of the younger sediment remains. The impact produced a variety of structural features. The circular central block contains a circular core of megabreccia about 1520 meters (Ford, 2012). The impacted breccia is monomitic breccia, which is the result of rock deformation from the impact event. The breccia from Wells Creek is homogenous breccia that has been under intense movement and very high confining pressures. The angular Horst is an upthrown block between the two fault blocks and the inner Graben is a downthrown block near the central block (Ford, 2012). The larger impact structure is an anticline which is boarded by a second ring Syncline of the wells creek basin structure (Ford, 2012). The shock wave releases are large amounts of energy from the central point of impact moving outward forming ring anticlines and synclines. The impacted breccia matrix consists of angular fragmented chert, limestone, and dolomite. The wells creek