Uses and Abuses of Carbonate Sequence Stratigraphy

With our observation of the Shawangunk formation, we see a sedimentary rock formation containing a range of grain size. Such sizes range from pebbles (3cm-5cm), fine-grain sand, and medium-grain sand. There is some grading towards the bottom left of the outcrop known as a reverse grading with some small cross beds present (Figure 2). The grading occurs towards a slight part of the outcrop where we see the grading beginning as fine grain sediments and working up to coarser grain. With moderate sorting we see variations of degree of sorting per bed. As the degree of sorting varies as does the sphericity. The sediment bedding is well seen ranging in sizes of +/--20 cm to 40 cm. This outcrop has thick beds as one can see the basic units with cracks in between each (Figure 3). With mostly tabular beds consisting of sub-angular, and sub-rounded sediments, this outcrop also consists of some ventricular beds (Figure 4). When looking at figure 4, we have a small space of a ventricular bed present. This is because the bed comes in, pinches thicker bedding,

The Repton Long Barrow sits between the parish church and the River Esk in Repton, Bluffshire, U.K. Last summer, I examined evidence for previous disturbance(s) of the site and assessed the extent to which the original Neolithic burial mound remained intact. I excavated two different sites on the mound, one on the east end and another on the west end of the barrow. While excavating and cleaning each of the sections, I recovered artifacts and human bones. I was also able to draw a stratigraphic profile of each excavation site. Using documentary sources pertaining to the Repton Long Barrow site to assist in my interpretation of the history, I was able to reconstruct the

Next, these rocks undergo erosion, which is the process of moving sediments from one place to another. Then, these sediments are deposited all at one place and over time they start to converge and cement as layers which are also known as strata. As time keeps going, new sediments deposit and cement together over old ones forming new layers. This is a repetitive process that eventually build up layers to make up a Sedimentary rock. Approximately 40 major sedimentary rock layers exposed in the Grand Canyon National Park area range in age from about 200 million to nearly 2 billion years old. As you can see, sedimentary rock formation takes an excessive amount of time.

Based on the drawing, Culture D is most likely the oldest. Most of the artifacts labeled as being from Culture D are in the bottom layer of soil. Though they do crop up in all the other layers, they appear to be disturbed rather than primary. Several are impeded in the temple, meaning that the culture that built the temple probably used dirt which happened to contain the artifacts was used unintentionally. The other D artifacts that appear closer to and at the surface were likely churned up by the constant disruption of the soil from the following culture. The third oldest culture was probably Culture C. There is a clear layer under which most of the D artifacts were buried. A trash pit

There are coarsening-upward sequences preserved, with flooding surfaces represented by low-relief erosional contact of trough-cross-stratification (runnel) upon low-angle planar bedding (swash zone).

Structural Geology – When large bodies of rocks are formed these did not happen in one day. They have history within that can be studied. Structural Geology discovers this history to be able to tell what happened before, what kind of tectonic plate occurred. Structural Geology supports other Geology areas such as Petrology to discover natural gas or petroleum to say the least.

The Mesozoic tectonic history of the North American Cordilleran region is very complex and involves:

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

| |sequences of events thus telling|sediment stacked on top of each |and the determining how old |

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,

They documented a flight of six terrace surfaces rising above the modern floodplain of Carrizo Wash. The highest and oldest surface (T6) consists of Pleistocene gravel, and the lowest three surfaces (T1–T3) date to the historical period. The remaining two terraces (T4 and T5) were formed during the prehistoric portion of the Holocene. Anderson and Edwards differentiated the alluvium into four stratigraphic units, and seven radiocarbon dates on detrital charcoal provided temporal control. The oldest deposits, designated Garcia Ranch I, underlie the T5 tread and are associated with radiocarbon dates of 7090 and 6132 14C yr BP. Anderson and Edwards believed that stream down-cutting followed the deposition of Garcia Ranch I deposits. Garcia Ranch II deposits are inset into the older Garcia Ranch I alluvium, but also form part of the T5 surface. The lower portion of this unit contained charcoal that yielded dates of 4250 and 3780 14C yr BP. The upper part of the Garcia Ranch II unit includes paleochannel fill dated at 3890 14C yr BP. Garcia Ranch III deposits contained charcoal dated at 2410 and 2520 14C yr BP. Pueblo I and II materials on the surface of this unit suggest that Garcia Ranch III deposition ended prior to about 1,200 years ago. The youngest prehistoric deposits are inset into T5 and consist of

The South Brae oilfield is mainly Kimmeridgian to mid-Volgian in age, however on some accounts it may possibly be of Oxfordian (Turner et al, 1987). The oilfield is heavily developed along the western, fault-bounded margin of the South Viking Graben approximately 161 miles NE of Aberdeen flanking Fladen Ground Spur (see Fig.1). The Upper Jurassic rifting of the South Viking Graben encountered, pronounced movement along the western bounding fault as syn-rift extension proceeded (Harris & Fowler, 1987, Gregory et al, 2007). Syn‐tectonic deposition throughout the Jurassic ensued the formation of a distinct sediment wedge thinning eastwards into the basin, outlining the main phase of fault movement down the boundary fault (Roberts, 1991). As a result, the Brae oilfields are a series of

When we think of history, we think of important people, places, cultures, events, and much more. The backbone of history rests on its chronology. It gives us the "when" of basic analysis. It gives us a frame of reference, the order of things. Before having an "absolute" way of determining dates, history was based in guesses and assumptions. Many attempts were made to organize the dates of the past. Some of these attempts were made by geologist. Geologist used the idea of "stratigraphic succession" (Renfrew, 1973) which is based on the "principle that when successive layers or strata are observed in position, the underlying ones are the earliest." (Pg. 23 Renfrew, 1973) By setting the layers in

By testing sediment and recording whether it was deposited under conditions of normal polarity and then measuring successive layers, we can build a time chart. By matching different charts from different areas with similar fossils, a more global correlation can be made.