Papago Park Pediment

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).

In my opinion I believe Linda should honestly consider the call an emergency, and give the doctor then message for them to call her back or at least help her out and Linda ask the doctor what she should do.

The Waucoba Wash Quadrangle, California cross section begins with the deposition of the Cambrian layers such as the Campito Formation, Poleta Formation (upper and middle members and undivided), Harkless Formation, Saline Valley Formation (lower and upper members), Mule Spring Limestone, Monola Formation (lower and upper members), and the Bonanaza King dolomite (dominantly limestone and undivided). These Cambrian rocks are followed by rock layers from the Devonian period, thus meaning that an unconformity occurred between the layers. The Devonian dolomite rock layers include the Hidden Valley dolomite and the Lost Burro Formation (cherty dolomite). These are followed by the Mississippian

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.

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,

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 youngest of these rocks are dated at about 220,000 years ago. Rhyodacties and quartz latites in the modern caldera area extruded from about 320,000 years ago to 260,000 years ago, and then silica-rich rhyolites at Glass Mountain northeast of the caldera erupted from about 210,000 years ago to 80,000 years ago. The scattered distribution of the initial mafic eruptions indicates that they were erupted from the mantle, while the slightly younger domes and flows were from a deep-crustal source. The youngest rhyolite eruptions erupted at the northeast rim of the caldera at Glass Mountain and were the first activity of the silicic Long Valley magma chamber (Bailey, et. al., 1989).

It is subdivided, from north to south, into the Wabigoon, Quetico, Wawa, and Minnesota River Valley (MRV) subprovinces (Figure 2, Jirsa et al., 2011). The Wabigoon subprovince is composed of greenschist facies mafic volcanic and volcaniclastic rocks intruded by granitoid batholiths. Algoma-type iron formation and small mafic intrusions are also common in this terrane. Amphibolite to greenschist facies rocks comprise the majority of the Quetico subprovince. In Minnesota, it occurs as a westward thinning belt of relatively homogenous metasediments and interstratified migmatites. The Wawa subprovince is composed of greenschist facies mafic and felsic volcanic rocks, granitoid batholiths and subsidiary Algoma-type iron formation. The MRV is the oldest of the terranes, and is characterized by granulite facies gneissic domes (Jirsa et al., 2011). Although not included as part of this study, a comprehensive overview of the mineral potential of the Vermillion Greenstone (Wawa Terrane in MN) was provided by Peterson

The quadrangle is considered to be a part of the Allegheny Plateau, so the rocks in this region are mostly of Carboniferous age. Carboniferous rocks are subdivided into two series: the Pennsylvanian and Mississippian. The rocks of both series mainly consist of alternating beds of shale and sandstone, but Mississippian rocks on southern parts of the plateau include thick limestones (Phalen 1). Both series are represented in the Johnstown quadrangle. The Pennsylvanian series, however, covers most of the region, while Mississippian rocks appear only at the surface along deeply eroded anticlines.

Emilie Tixeront explains the rock cycle, the formation of the Glasshouse Mountains, and what makes rocks so special anyway.

The Sangre de Cristo Mountains are a structurally complex block having a Precambrian igneous core that is bounded by major, high-angle reverse faults and highly contorted, steeply dipping to overturned sedimentary beds of Paleozoic and Mesozoic age. The range resulted from uplift and eastward thrusting during the Laramide orogeny commencing in Late Cretaceous time and continuing intermittently to possibly late Tertiary time (Wanek and Read, 1956).

Papago Woman, written by Ruth M. Underhill, is an ethnography of the life of a native american woman named Maria Chona, a member of the Southern Arizona Papago people located right outside of Tucson, Arizona on a reservation. Ruth lived among the Papago from 1931 till 1933. She studied the life of the Papago with her main subject an older Papago woman named Chona. She says at one point how she learned amongst these people and Chona, “I feel, nevertheless, that out of all this flurry there came the story as it had appeared in Chona's mind,” (27). By hearing the life of this Papago woman she learned about life as a Papago.

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

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

The soil and biotic/abiotic features of the park vary greatly depending on the area of park being studied. The volcanic rock that underlies the