Clear Creek Discharge Report

The Devon River is clean, freshwater, and well dammed up. It is described as being a small, narrow river fringed by pine and birch (pg. 42) On the other hand, the Naguamsett River is described as muddy and

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.

Webb (2003) conducted numerical analysis of source-water dynamics of stream-bounded alluvial aquifers, along the Ohio River in northern panhandle of West Virginia, with consideration of lateral infiltration of groundwater from bedrock aquifer. However, the author did not verify her model to the field data. On the other hand, Kozar and McCoy (2004) presented groundwater-surface water interaction and simulation of groundwater flow in the alluvial aquifers from the northern panhandle of West Virginia without considering recharge form adjacent bedrock and leakage from overlying tributary streams. Although, Bader et al., (1997) and Unthank (1999) independently identified that the alluvium along the Ohio River, West Virginia and Kentucky respectively is recharged by the following means: (1) precipitation on the flood plain, (2) inflow from fractures in the bedrock beneath and adjacent to the alluvium, (3) inflow from tributary streams through gravel deltas and bedding-plane partings, and (4) induced inflow from the river. Water flowing in tributary streams can percolate through the deltas to the gravel under the clay-silt layer (Grain, 1966). Unthank (2013) updated model and reran it which generated significant difference between measured water levels and model-computed water levels in the aquifer. The author concluded that more accurate and site-specific estimates of field parameters, refined model geometry, and additional numerical method improve

“Drainage patterns, the hilliness of the ground, the range of soils, the nature of the bedrock,

The latest rocks in this region were formed in Pleistocene time as imperfectly consolidated gravel of river terraces and alluvial deposits of the

Running water moves sediment in the processes of erosion and deposition, causing different types of landforms. As you can tell in the picture above, Michigan’s topography plays a huge role on where the faster and slower flowing rivers are located and the transportation of the materials in the water depends on the speed of the rivers. Erosion is the breaking down of those materials by the agent, water. The water can erode the channel laterally and vertically, in the end, making the channel wider and deeper. There are different types of erosion: hydraulic action, corrasion, corrosion, cavitation, and attrition. Hydraulic action (above on the right) takes place at rapids and waterfalls because the force of the water removes rock particles from the bed and banks of the river. A great example of this in Michigan is Canyon Falls on the Sturgeon River. At the waterfall, the water is rushing at a high velocity, especially in the spring, causing rock particles to move downstream, creating a wider and deeper river. Eventually the rivers velocity begins to decrease and particles start to deposit. This could also occur because lack of precipitation or an increase in evaporation. The deposition of materials at different locations of the river that they began changes the shape of the river, and effects Michigan as a whole in the end. The particles can travel all the way to the mouth of the river, in this case, Lake Superior, causing

The Arkoma Basin is one of several foreland basins that formed along the Ouachita Orogenic Belt during the Mississippian and Pennsylvanian time periods. It covers approximately 33,800 square miles and extends from southeastern Oklahoma to central Arkansas (Perry, 1997). The Arkoma Basin is bounded to the north by the Ozark Uplift, to the south by the Ouachita Mountains, to the northwest by the Anadarko Basin, to the southwest by the Arbuckle Uplift, and to the southeast by the Mississippian Embayment (Figure 5). The red box in figure 5 denotes the general location of the study area, which is in the eastern Arkoma section.

Our sites (Figure 1.) were spread along the lowest reach of Merri Creek before it runs into the Yarra River. As a direct result of this there is an extensive valley from the constant presence of fluvial processes over geological time. The landform patterns at our sites were extensively governed by the movement and availability of water, with escarpments, gullies, cliffs and spurs of varying steepness all observed.

On April 6th 2013, our Biology II lab evaluated the health of two freshwater streams in the Denver area. Both creeks flow to the South Platte River but are situated in different environments (urban and suburban) which cause variance in biotic and abiotic indicators of stream health. The presence or absence of bioindicators is dependent on the water chemistry. Through the study of stream health, we can gain insight on the stress that humans cause to freshwater habitats. I think that Bear Creek is healthier than Cherry Creek because it is in a less urban environment and is less affected by human influences. If the

Geology: Built when the Chippewa and Flambeau Improvement Company built a dam on the Flambeau River downstream from its confluence with the Turtle River

Degraded streams are manifold throughout the nation. There a total of 42,904 impaired streams with 71,796 causes of impairment. Whereas, the Clean Water Act is paramount to stream protection, the legislation does not call for reversal or removal of out-dated traditional runoff management techniques; nor does it expect efforts to be made to prevent damage from continuing in the future. Several sections of La Nana Creek running from its mouth to SH 7 are currently listed on the federal 303(d) list section 5a for total coliform bacterial loads. This section runs through

This geologic data has shown that the basin contains sedimentary rocks of Late Cambrian to the Tertiary age, and is more than 15,000 feet thick. The depo-center of the Williston Basin started its development during the early Paleozoic era in the northwestern part of North Dakota. The sedimentary rock thickness decreases to less than 10,000 feet in eastern Montana and to less than 5000 feet along the basin margin (Peterson & MacCary, 2009). Carbonate deposition occurred throughout the area during the early to middle Paleozoic era and changed to clastic deposition in the late Paleozoic era. During the Paleozoic era, more than 8000 feet of marine sediments accumulated at the basin center, but the shape of the basin remained the same. The basin depo-center has however shifted slightly over time. The Williston Basin sedimentation in the lower and middle Paleozoic is dominated by carbonates and evaporates, whereas upper Paleozoic and younger rocks are largely siliciclastic with small admixtures of carbonate (Anderson & Gerhard,

In Figure 2 the Southeast Transect is located in the south end of Marlatt Park, near the South Parking Circle. The transect starts west at elevation of 1280 feet and progresses to the east ending at an elevation of 1260 feet . Compared to the high starting points in the previous transects, the overall elevation is lower and the topography is more gentle. The transect starts in a relatively flat area and slopes gently to the east in the first few plots, where limestone is present. The slope increases in Plot 3 were the parent material changes to shale.The transect crosses the east creek and can be seen in Table 3. The soil types vary from Florence in Plots 1 and 2, Benfield in Plots 2 to 6, and 9, and Wymore-Kennebec complex in Plots 7 and 8.

The data I have collected was based on the stage height of the Tioga River from the USGS data base. The data base showed the peak of stream flow and the discharge in cubic feet per second, and also on the scatter plot I have provided shows the stream flow and discharge in cubic feet per second. The discharge stayed mostly in between 6-15 cubic feet, which means it is at a good amount most

The surroundings of these areas differ at each site. Site one is mostly rural areas whereas, when it moves onto the last site, it becomes an urban area. These will affect on the course and direction of the river and its characteristics.