The Taconic Orogeny In The Hudson Valley

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.

Cenozoic sedimentary rocks predominated to the west and east of the central mountain while plutonic rocks predominated in the peninsular ranges. The irregular contact between these geologic regions reflects the ancient topography of the area. The ancient oceanic crustal plate created an archipelago of a volcanic island. The former's subduction created immense volumes of magma. This resulted to the congealation of plutonic rock in the crust. The local rocks that existed before the tectonic forces uplifted, and erosion capped the deeply buried plutonic rocks that formed a steep and rugged mountains coastline, similar to that present one, which in the west coast of south America.

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).

The Ozark Mountains are characterized by eroded plateaus caused by the collision of the super continent of Gondwana, which compressed the present continents of South America, Africa, Antarctica and other land masses. These forces uplifted Arkansas with limestone and calcareous rocks such as sandstone and chert. Erosion lowered the surface creating a level plateaus which included: The Boston Plateau, the Springfield Plateau, and the Salem Plateaus. Rivers, over time, cut valleys into the plateaus. Present day Fayetteville-Springdale-Rodgers, Harrison, Mountain Home, Batesville, and Clinton are all cities which are within the Ozark Mountains boundaries.

Regional history, lithology and structural geology of the Flin Flon greenstone belt and the broader Trans-Hudson Orogen, with special emphasis on University of Saskatchewan Flin Flon Field School map area 4

Florida and Shenandoah National Park have many commonalities as well as differences that makes each of these geologic setting unique. Though North America looks like Florida and Shenandoah National Park never seemed to collide with one another, Shenandoah has a rock record of being about 1 billion years old that constructed the North American continent and a building block that formed the Appalachians through orogenies. Florida falls about 300 million years old with the North American plate, however findings that were part of Gondwana provides evidence of the origin of Florida. With a vast time difference of these rock records, what can be furthered analyzed of what the

The Niagara Escarpment AVA is a relatively new viticulture designated area. The area received the designation in 2005 and is now one of the fastest growing wine regions in New York State. This AVA is comprised of a portion of the Niagara Escarpment landform that runs from New York State through Canada into Wisconsin. (Fig. A) The escarpment has formed over time due to erosion of the rock layers. The top rock layer, dolomitic limestone, is more weather resistant causing it to erode slower and creating the escarpment landform.

One of the major things noticeable from the cross section is that quite a few of the rock layers are over turned, where the older rock layers are above the newer rock layers. This is seen in the contact between the Quartz Monzonite of Papoose Flat and the Campito Formation which is also a disconformity. Next there is some fault zones separating the Camptio, Poleta, and Harkless formations. We then see some more overturned layers with the contacts between Saline Spring Valley Formation (lower and upper members) above the Mule Spring Formation along with some inferred folding. With a normal fault separating the inferred folding event, we see where the overturning occurs. In between the Cambrian layers we see Tertiary Basalt nonconformities also being folded, thus with that we know that the folding event was more recent than the formation of the Basalt. Next there is a large Basalt field with a spot of the Harkless formation. Again we see over tuning as the Basalt field ends there are the Devonian and Mississippian rock Layers on top of the basalt. Separating these overturned layers from the Harkless Formation and the Saline valley Formation (upper member), which are not overturned, is a thrust fault. From this information, there was a major stress event sometime after the Tertiary period causing the rock layers to fold and overturn. And from this stress event and from the folding, normal and thrust faults are formed. Finally we see that there were alluvial and landslide deposits from the Quaternary after the folding, faulting, and over

The Earth's crust has been undergoing complex chemical, physical, and biological reactions over more than 4 billion years now. In this relentless tardiness of geologic instance, the convection of the Earth's mantle gave form to the planet (Cronon, 1993). The Middle Atlantic region of North American was shaped by the tectonic plate movements and climatic changes shaping the ancient oceans into lands. Water streams gave form to hills and deep valleys and rainwater broke big rocks into fine soil. It is interesting to note that while all this was taking place, Maryland's mountains were comparable to the size of the Himalayas (Flannery, 2001). Their rock gradually created the mountain that we see in Maryland in the present day. Eventually, Maryland's rock layer turned into fertile soils, mineral deposits, and composite water elements.

Connecticut's landscape and surface change from 3 elements named tectonic plates, Glaciation, and Weathering and erosion.

The Appalachian Region stretches from the northern part of New York, through Pennsylvanyia, all of West Virginia, the West side of Kentucky, Mississippi, and the southern parts of Maryland, S.Carolina, N. Carolina, and Alabama. The immigrants who settled in the Appalachian Region were made-up of three main ethinic backgrounds; Scot-Irish, English, and German. “Appalachian people are considered a separate culture, made up of many unique backgrounds—Native Americans, Irish, English and Scotch, and then a third descendants of German and Polish immigrants—all blended together across the region”(“Appalachian Culture”, 2015). The immigrants came to the Appalachian Region either in search of land at cheaper prices or to get away from the Quacker Leaders. The Appalachian Region has proven to create a hard way of life for those who settled the region. “The people who settled in the Appalachian region were known as hearty people who lived in an often difficult environment”(“What is Unique”, 2015). Those who live in the Appalachian Region today may not face the same challenges as his or her ancestors who settled the region, but there is no doubt the Appalachians still brings a set of challenges. However, no matter the challenges there is one thing those who live in Appalachia share, tradition. It is these traditions that assisted the first settlers, our ancestors, in living life and are still getting present day Appalachians through.

It consists of the state’s most unique landscapes – strangely long, tapered and almost parallel ridges and valleys, all mingling over water gap formations. The province extends from the center towards New Jersey (north-eastward) and into Maryland (south-westward). The province’s ridges and valleys are made up of Sedimentary rocks from the Paleozoic Era. Metamorphosed Proterozoic volcanic rock (~575 million years old) is also found in some ridges of the South Mountain sector of the province. The sediments were originally deposited in a horizontal manner, but then these rocks were subjected to a high amount of heat and pressure during the Alleghanian orogeny, which resulted in them being folded and angular. The erosion of sediments over the years have formed a very distinct landform – valleys have been formed over areas of shale and limestone (softer rocks) and ridges have been formed in the areas of sandstone (harder rock). This Province is divided into 7 sectors: South Mountain, Great Valley, Blue Mountain, Anthracite Upland, Anthracite Valley, Susquehanna Lowland and Appalachian

We started in North America at the Rocky Mountains. The mountain stretches from Alberta, Canada to New Mexico in the U.S. Appalachian Mountains is a system of mountains in eastern North America.

Clastic rocks are most common in the central part of the study area and display graded bedding as well as slumping and soft-sediment deformation (Frey and Venzke, 1991).Chemical sedimentary rocks in the OB include iron formation and chert. The tendency of massive sulfide deposits to occur in brecciated piles of tuff fragments with associated footwall alteration indicates they are not seawater precipitates. Chert is typically sulfidic, with pyrite and pyrrhotite as the main sulfide minerals.