Werribee Geological Formations

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 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 country rock was identified in the field to be a Meta-Limestone, but a more in-depth chemical analysis done by others classifies it as a dolostone of the Strath Suardal formation from the Durness group. (Digimap, 2017) (Goodenough et al. 2011)

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

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

Neotectonism is express in different ways in the eastern Uplands of north Queensland, in Atherton and Chillagoe territory. Some are identify by magmas dating (e.g. Nulla Volcanic Region) to know youngest ages (Nulla Volcanic Region) while others hold ropy structure (pahoehoe). In Atherton territory, most recent Pleistocene (Eacham) basalt is openly exhibited. Other evidence of neotectonics in Eastern Upland are seen where the Lake George and Shoalhaven reverse fault offset Palaeozoic layers across Miocene.

Raw gley soils are found within mineral material that has remained waterlogged since deposition (Thompson, 2007). The soils are missing a distinctive top soil and contain gleyed subsurface horizons (Avery, 1980). They also contain a mineral horizon which starts at <20cm and extends below 30cm (Avery, 1980). Jarvis (1984) also states that the soils are distinctly mottled above 40cm depth. Raw gley soil types are mostly confined to intertidal flats (Avery, 1980) or areas that represent various stages in the development of salt marshes (Thompson, 2007).

The geology of Pembrokeshire is well known for the coastal display of diversity of rocks and scenery over 250 miles exposure than any equivalent area in Britain. It has ancient landscape which was formed many years ago (290 million) at the end of Carboniferous period. The geological process and action such as river weathering, glaciations and marine erosion on this variety of rock is as a result of diversity of coastal landscape.

Much of the diversity of Putney’s soils can be attributed to the movements of the Laurentide ice sheet that, 20,000 years ago, covered the region in several thousand feet of ice. As the glaciers proceeded south, they reconfigured the land’s surface layer by scraping away the existing soil. As the world’s climate warmed, the ice retreated, redepositing glacial till across the landscape. Topography played an integral role in the distribution of soil following glaciation. In the hills, this unsorted till, a collection of boulders, cobbles, gravel, sands, silt, and clay, began the slow process of pedogenisis (soil formation) as plants and animals brought life to this barren world. In the valleys, material was sorted by the water from the melting ice as it flowed down from the hills (Stewart 55). Below, in figure 1, the areas of unsorted till are represented in orange while areas of sorted sediment such as gravel, sand, outwashes,

North Ridgeville is associated with the Devonian time period as it is in the northeastern part of Ohio, and has deposits of shale,

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

Rock suitable for the production of stone tools is fOW1don every mountain range, and in creek beds as cobbles and pebbles. Two surveys have been conducted in the area. Horned Toad Consultants conducted extensive judgemental surveys during initial impact assessment, concentrating on the grasslands of the Little Bison valley, two arbitrarily chosen tributary valleys (Cripple Creek and Silver Creek), one cirque (below Smith Peak) and the Inverness Plateau. Four site types were defined. Camp sites contain a wide range of artifact types and fire broken rock. Kill sites contain a restricted range of artifacts (mainly projectile points) and large quantities of bone. Lithic scatters are small sites with no diagnostic artifacts. Quarries have large quantities of debitage, usually associated with shallow pits dug into bedrock. The distribution of sites and diagnostic artifacts is shown in Figure 8.1. Recently R. Bootheel undertook a survey of the area using random sampling techniques. Although her M.A. thesis is still being written, she has commented on the previous survey as follows:

The Taconic orogeny is evidenced in the Hudson Valley. This orogeny has formed by the convergence of the Laurentia and the Shelburne arc. The Taconic orogeny has led to the formation of sedimentary rocks that can be classified into autochthonous and allochthonous, whereas the Normanskill formation is autochthonous, and five distinctive thrust slices from the low Taconic sequence are allochthonous. Another feature is the Cortland Complex, which is a late Ordovician magmatic intrusion formed by norite, gabbro, hornblende norite, monzodiorite, diorite, hornblende pyroxenite, and peridotite. The sedimentary rocks in the Dutchess county and Westchester counties, New York, have suffered metamorphism due to convergence activities as well as magma

The major geographic regions include the Ozark mountain region, this region was in the Northwest part of the state of Arkansas. Much of the Ozark Mountain region was heavily forested and was noted for timber production, and there were some very old rocks noted to be found during this time in the Ozark Mountains, the oldest rocks were the Ordovician. These rocks aged back 505-438 million years ago. They were found in the bluffs, steam beds and flood plains of the Northwest part of the county. There was also a minimal amount of farming except in some valleys and plateau

The lithology of the Forest Hill in Wayne County is similar to that described for this formation in the counties in central and western Mississippi. The main difference is the occurrence of fossiliferous lenses (marine fossils) in the otherwise darkgray, silty to arenaceous, micaceous, carbonaceous clay. The term "Forest Hill Sand," which has been used in numerous publications, is a poor indicator of the formation's true litho logy, as Bob Ainsworth77 reported in his mineralogical and grainsize data paper published in 1967. His computed averages for Forest Hill samples collected in the Jackson and Vicksburg areas show 51 percent silt, 32 percent sand, and 17 percent clay. In Wayne County the percent of clay is considerably higher.