Slave Carton Analysis

Canada and especially Ontario have very interesting and much filled geologic pasts. Ontario has many types of rocks and minerals that have formed and are still forming due to the geology. Ontario has sedimentary rocks; igneous rock, and metamorphic rock as well as minerals such as gold, silver, quartz, and many more. In this paper, we will begin by talking about ten rocks that were collected right here in Windsor Ontario. The rocks were examined from the outside which tended to be weathered and the inside which were fresh.

Approximately 17 meters thick, Unit A defines the lowest third of the Juniata Formation. Fragments of marine fossils, including bryozoans, brachiopods, and gastropods, are commonly found in the bottom-most portion of this unit of structureless mudstone and quartz arenite. Quartz grains in the sandstone beds of Unit A are typically immature and fine-grained, though the sandstone packages tend to coarsen upwards. Though typically structureless, intermittent bedding of the sandstone and shale packages is observed in this unit, and some areas display

Starved Rock State covers about 200 miles and some 470 million years, from Ordovician sandstones to Pleistocene glacial till. The Ordovician St. Peter Formation sandstone was deposited across the midcontinent during the second major marine transgression of the Paleozoic Era. The first transgression deposited Upper Cambrian to Lower Ordovician clastics and carbonates. The clastic to carbonate rock transition is consistent with gradual sea level rise over the North American craton. Sea level dropped late in the early Ordovician, exposing the carbonate strata to processes of cave development.

The site is of major geoconservation significance because of being the only place on earth where rocks from the earth’s mantle - 6 km

Copper-zinc (VMS-type?) mineralized zones were discovered in Archean volcanic rocks in the southern part of North Williams Township by Metron Explorations Limited in 1970. The mineralized zone and surrounding area were evaluated with a HLEM survey and drilled with 2 DDHs (totaling 61.3 m) that did not intercept significantly mineralized rocks (Willars, 1971).

Sims et al. (1989) synthesized U-Pb zircon ages for the Pembine-Wausau terrane. Sims concluded that the volcanic rocks were generated from around 1889 to 1860 Ma as island arcs and closed back-arc basins above the south-dipping subduction zone (Niagara fault zone). Granitoid rocks in the terrane, emplaced from around 1870 to 1760 Ma, are mainly granodiorite and tonalite but include gabbro, diorite, and granite. These developed as island arcs above the Eau Pleine shear zone. The Niagara fault zone contains a relict ophiolite, suggesting that the rocks in the Pembine-Wausau terrane probably accumulated on

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.

Next, we can see that the rock displays a subtle porphyritic texture with plagioclase comprising the phenocrysts. The overall texture of the surrounding groundmass is granoblastic equigranular. Under thin section we also see a weakly defined foliation evidenced in the preferential alignment of actinolite grains and to a lesser extent chlorite grains. Undulose extinction is also observed in quartz indicating the rock was subject to deformation. The normalized quartz, alkali-feldspar, and plagioclase (QAP) values of this rock indicate that it is classified as a grano-diorite according to the IUGS QAPF classification system which is consistent with the hand sample interpretation.

The three faults being considered are thought to have influenced the character of some 120,000 square miles. The Big Pine, Garlock, and San Andreas faults are all mutually active, deep, long, and steep and noted as being conjugate shears. In concert, the faults have defined a primary strain pattern of relative east-west extension and north-south shortening of the area of 120,000 square miles. The large region is noted for its deformity, with the source of this being a northeast-southwest counterclockwise compressive couple. The compressive couple was potentially supported through drag as a result of the deep-seated movement of rock material from the Pacific region (Hill & Dibblee, 1953). The interaction of the faults in the San Andreas region since the Jurassic period have served to shape and contour the present geology of the land, while a study of the paleontology of the region likewise requires such knowledge to effectively determine conditions at any given point in time.

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 objective of the trip to Blount Springs, Alabama was to observe and gather data on the geological structure of the area. Blount Springs is located in the northern part of Alabama just 33 miles north of Birmingham, and lies on the southernmost part of the Appalachian fold belt. The field work began on the morning of Saturday April, 7th at 8:50am. The weather was cloudy with temperatures in the mid 40’s, and the area was wet from rain the previous night. Our materials included a map of the area, list of formations, a Brunton compass, and a Rite in the Rain field book. The procedure of the field work involved 12 stops at outcrops to gather data, one stop was omitted from the original plans. This data gathered included bedding and joint orientations

Most drilled massive sulfide deposits and iron formation layers occur near the top of the volcanic pile and overly the flanks of the LLIC. Felsic rocks underlying massive sulfide deposits in the top of the volcanic pile are FI and FII types. Rocks with a magnetic signature similar to known massive sulfide deposits occur down section and over the center of the LLIC. These rocks are interpreted as having the highest potential for hosting Au-rich VMS deposits. Mafic rocks of the Oaks Intrusion (OI) occur in the eastern part of the belt and have been dated at 2671±8 Ma (Keatts et al, 2003). Likely time correlative to the OI, a magnetic mafic sill (Oaks Intrusion sill; OIS) intruded and inflated the volcanic pile after or contemporaneously with the main deformation event (D2).

Phase 1 - Data collection (April 2017): My local collaborator Xin Wang and I will work at MGK for a week to collect nine OSL samples from MGK1, MGK2, and MGK6 and a soil column from a natural profile near MGK. After the completion of our fieldwork, I will ship all newly acquired OSL samples together with other OSL samples collected in 2016 to the University of Georgia Luminescence Dating Laboratory. Additionally, I ship the new soil column to the Geoarchaeology Laboratory at Washington University in St. Louis.

The upper Miocene strata are conformable, with no evidence for faulting or extensive erosion during the intervening period (~24 to ~11 Ma). The pre-rift flood volcanics and syn-rift units show a regional SE dip. The contact between Megezez and flood volcanics can be traced in imagery throughout the region (from Wolfenden et al, 2004).

Not all scientists have accepted the validity of these observations or of their interpretation, Dimroth and Kimberley(1976) argued that at least some red beds antedate the end of BIF deposition, that Archean granites have paleoweathering profiles indicative of oxic environments, and that oxidised sulphur minerals (sulphates) occur in some of the oldest known sedimentary successions. All of these observations are correct, and we must ask whether they