Presentation is loading. Please wait.

Presentation is loading. Please wait.

Characteristics Of Sedimentary Rocks

Similar presentations

Presentation on theme: "Characteristics Of Sedimentary Rocks"— Presentation transcript:

1 Characteristics Of Sedimentary Rocks
An understanding of some of the basic characteristics of sedimentary rocks is required to comprehend West Virginia’s geologic history. This presentation is not intended to be anything other than a very brief introduction to sedimentary rocks. Enter

2 Ancestry: The Origin of Earth’s Crustal Rocks
Click On A Topic For More Information Ancestry: The Origin of Earth’s Crustal Rocks Making Sedimentary Rocks: Weathering, Erosion, Sediment, Deposition, and Lithification Depositional Environments and Facies Bedding of Sedimentary Rocks Response of Rocks to Stress { When you see this symbol, click on it and it will return you to this page. Back

3 Ancestry: The Origin of Earth’s Crustal Rocks
We have no record of the 500 million years following Earth’s formation. We speculate that it was a time of intense meteoroid bombardment when the mantle and the crust that surrounds the molten iron core were forming. Basaltic magmas rose to the surface and spread across the surface of the underlying mantle in a relatively thin layer that was eventually to become the oceanic crust. The surface of the crust during this primeval time was being formed and re-assimilated as underlying convection currents churned the outermost layer of Earth. The heat from the molten core, heat generated by the breakdown of radioactive elements, and the intense bombardment by meteoroids kept the temperature at Earth’s surface very high. Partial melting of the basaltic crustal rocks eventually began to generate masses of molten granitic rock. In time, these granitic masses would coalesce to form small continents. These micro-continents eventually converged and sutured together to form larger continents. Over time, the thermal activity within the crust began to slow as Earth cooled, the abundance of radioactive elements dwindled and the frequency of meteoroid impacts diminished. Estimates indicate that by 2.5 billion years ago the present mass of continental crust had formed. At this point the processes of weathering and erosion assumed their roles in creating sediments that would eventually become sedimentary rock. Back

4 Making Sedimentary Rocks: Weathering,
Erosion, Sediment, Deposition, and Lithification Test Your Term Knowledge What do the following terms mean? Click on the terms and see if you’re right. Weathering The destruction of rock into sediment due to the actions of wind, water, or ice. (Making smaller rocks out of bigger rocks!) Beginning about 2.5 billion years ago Earth’s surface had cooled sufficiently to allow precipitation. Water vapor, erupted by the world-wide volcanism and stored in the atmosphere, condensed and began to fall as rain. Once the rains started, the water filled the basaltic low area creating the oceans that cover 70% of Earth’s surface. The granitic high area above sea level became land. The presence of precipitation initiated weathering and erosion. These processes produced sediment which was moved by wind and water and ice to areas of deposition where the sediment was lithified. Sediments Varying sized pieces of rocks produced by the agents of weathering. Erosion Transport of sediment to new locations by wind, water, or ice. Deposition Accumulation of transported sediment in a variety of different environments and geographic settings. Lithification Rock making process whereby deposited individual sediment grains are cemented together. Back

5 Sediment Particle Size
Sediment is weathered (broken) pieces of older rock. Sediment is classified by size ranging from clay to boulder. Clay-sized sediment produces the rock shale. 70% of West Virginia sedimentary rocks are shale! Sand-sized sediment becomes sandstone. Limestone forms in its own unique way. Back

6 to view step descriptions:
Shale is a fissile rock composed of composed of oriented clay-sized particles. Fissile refers to the fact that a shale can be separated into layers. Click on Steps below to view step descriptions: Randomly arranged clay-size sediment is deposited as mud. Much water is located between individual particles. Step 1: Continuing deposition buries sediment. Weight of overlaying material begins to compress clay particles together. Water is squeezed out as particles become less randomly oriented. Step 2: Continuation of compression removes more water and produces highly aligned clay particles. Step 3: Majority of water removed and sediment particles are aligned producing the fissile rock we call shale. Step 4: Back

7 Question: Click here to find out.
Sand is a size term referring to sediment particles ranging from 1/16 to 2 millimeters in diameter. When the sized particles cement together into the rock called sandstone a entire suite of fine-grained, medium-grained, or coarse-grained sandstones may result. As in shales, once the sand sediment is deposited, the removal of water initiates the rock forming sequence. Question: Without something to hold the individual sand grains together, the rock would not exist. It would just be a pile of sand. What process is required to form the rock called sandstone that we have not yet talked about? Click here to find out. Back

8 places for the accumulation of water, oil, and natural gas to collect.
Answer = CEMENT Sand-sized particles are cemented together when iron (Fe2O3), silica (SiO2), or calcium carbonate (CaCO3) precipitate from ground water moving through or being forced out of the sediment particles as they are being compacted. Some of the iron, silica, or calcium carbonate precipitates and is left behind (brown areas). This material becomes the cement holding individual grains together to form the rock called sandstone. Water between sand-sized sediment grains contains cementing agents that are dissolved in water. The open spaces between the sand grains are called pores. Pores provide places for the accumulation of water, oil, and natural gas to collect. Back

9 Limestone is predominately calcium carbonate (CaCO3).
Calcium carbonate is dissolved in water and can be removed and turned into a carbonate-rich mud either chemically or biologically. In either case, the CaCO3 is both the accumulating sediment and the cementing agent holding the sediment together to form the rock called limestone. Aqueous environments where carbonate-rich sediment accumulates over a large area is sometimes referred to as a “carbonate shelf.” Back

10 Depositional Environments and Facies
The two basic depositional environments are terrestrial and marine. Terrestrial environments are located on land with the most important being those associated with streams; such deposits are referred to as fluvial deposits. Marine deposits are those that accumulate in ocean/sea environments. Unique nearshore brackish areas such as estuaries, lagoons, and tidal basins are referred to as non-marine. Deposition occurs simultaneously at different locations and, therefore, the elements of time and location must be considered. Geologists call this concept “facies.” Back

11 Fluvial deposits include sediments accumulated in
stream channels, as levees, or on floodplains. Back

12 Facies and Facies Changes Transgression and Regression
A typical facies scenario would occur where three types of sediment are being simultaneously deposited in bands parallel to a shoreline. In this scenario sand-sized particles accumulate in the near-shore environment and beach area while clay-sized materials accumulate in slightly deeper water because they are separated from the sand by ocean currents and then carried farther offshore. At the same time, if the water is relatively warm, limestone (also called carbonate) would accumulate in still deeper ocean depths even further offshore. Upon lithification, a single layer of sedimentary rock would be created that would, in various locations, be composed of three different rock types: sandstone, shale, and limestone. These rocks would be seen to change into each other laterally. Each rock type would represent a particular depositional environment and would be referred to as a facies of the overall unit. The lateral change from one facies to another is called a facies change. Note that within an individual layer, the order of facies change points either landward (limestone to shale to sandstone) or seaward (sandstone to shale to limestone). Back Facies and Facies Changes Within certain depositional environments, different types of sedimentary materials are being deposited simultaneously as part of a single layer. A typical scenario would be the deposition that occurs on the surface of the continental shelf (Figure 15) where three types of materials are being simultaneously deposited in bands parallel to the shoreline: 1) sand in the near-shore environment, part of which may be the beach deposits, 2) clay-sized materials in a more off-shore area, having been separated from the sand by the ocean currents and carried into deeper water, and 3) if the water is warm, either chemically or bio-chemically precipitated CaCO3. Upon lithification, a single layer of sedimentary rock would be created containing three types of sedimentary rock, sandstone, shale, and limestone, which would change laterally into another (Figure 16). Each rock type would represent a particular depositional environment and would be referred to as a facies and the lateral changes from one facies to another is called a facies change. Note that within an individual layer, the order of change of lithology, the facies change, points either landward (limestone to shale to sandstone) or seaward (sandstone to shale to limestone). Transgression and Regression Let us add the factor of time to our facies and facies changes. If, over time, sea level rose, perhaps due to the melting of continental glaciers, the shore line and each of the three depositional facies environments would demonstrate transgression. Note that with the passage of time and rise in sea level each environment would move over the more landward environment. For example, during transgression, the carbonate environment moves over the clay-rich environment which, in turn, moves over the sand-rich environment which, in turn, moves over terrestrial deposits (Figure 17). Note that regardless of where the sediments would be observed, one would observe more landward environments overlain by more seaward environments. In an outcrop, therefore, the process of transgression would be recorded by observing a marine sandstone overlain by a marine shale overlain by a marine limestone. As sea level falls, the shore line and each of the depositional environments would move seaward, a process called regression. With the passage of time, each environment would move seaward over the more seaward environment. That is, the sand-rich environment moves over the clay-rich environment which, in turn, moves over the carbonate environment (Figure 18). In outcrop, therefore, the process of regression would be recorded by observing a marine limestone overlain by a marine shale overlain by a marine sandstone.

13 Bedding of Sedimentary Rocks
The basic characteristic of all sedimentary rocks is that they are bedded, that is, they are made up of layers called beds. Bedding is the result of the original sediments having been deposited in essentially horizontal layers, be it on an ocean floor, a lake bottom, or a floodplain, a relationship summarized during the early days of geology in the law of original horizontality. The significance of the law of original horizontality is this… Should you see sedimentary beds in anything other than a horizontal position it means that the rocks were subjected to some degree of deformation after they formed. Back

14 Response of Rocks to Stress
The way any material responds to an applied force depends on the kind of force, the ability of the material to withstand external forces and the physical nature of the material. The general term for all external forces is stress. The ability of a material to resist external stress is called strength. The way a material responds to stress is referred to as strain or, more commonly, deformation with deformation being defined as any change in either shape or size. S T R E N G H STRAIN STRESS Click on a button to learn more about each of these topics STRESS STRAIN STRENGTH Back

15 Stress is defined as a directionally applied force of which there
are basically only two kinds: Compression Tension Compression Compression In compression, the forces are directed toward each other. Compressional force can be oriented either directly opposite each other (non-rotational compression) or along parallel paths (rotational compression). This is a “PUSH TOGETHER” or “SLIDING PAST” motion. Compression Compression Tensional forces are always oriented directly opposite each other. This is a “PULL APART” motion. Tension Back

16 Click on terms below for more:
Strain Once strength is exceeded, materials deform in one of three ways: 1) elastic, 2) plastic, or 3) brittle. The type of strain can be determined using the decision tree. Plastic Or Brittle Deformation START HERE Did the material return to its original shape when the stress was removed? NO Click on terms below for more: Elastic Deformation YES Did the material break? Brittle Deformation YES TIP: It is important to know that a material may begin to deform plastically and then break. The reason being that only so much energy can be absorbed and internally consumed (plastic deformation). The remaining energy must be released by breaking (brittle deformation). Plastic Deformation NO Back

17 Inherent Strength of Rocks
Every material has an inherent strength which is simply the ability of a material to absorb stress without deformation. Strength can be looked upon as an invisible wall that stands between stress (applied force) and strain (deformation). Before any material deforms under stress, the strength of the material must be exceeded. Once strength is exceeded, a material will deform. Inherent Strength of Rocks Rocks are very weak under tension but very strong under compression. The best example involves a bit of ancient history, in particular, the architecture of ancient Greece and of Rome demonstrates basic engineering methods for dealing with the inherent strength of rocks. Back

18 Greek engineering construction techniques
Compressive and tensile forces in columns of the Greek Parthenon. The architecture of ancient Greece is characterized by the use of many columns as is beautifully exemplified by the Parthenon. The reason why the Greeks used so many columns is because they were never able to overcome the inherent weakness of rocks under tension. The ancient Greeks spanned the distance between columns with rock slabs called lintels. Whenever the distance between columns became too great, the lintels would fail by collapse. The reason for the failure was that with the lintels supported from their ends and loaded from above, the forces generated within the lintel were tensional. When the span between adjacent columns became too great, the rock failed under the tensional forces. This, of course, necessitated the use of many columns. Back

19 Roman Engineering Construction Techniques
The Romans spanned the space between columns with an arch. They discovered that by placing a keystone at the apex of an arch, all of the forces within the structure experienced non-rotational compression. Under this situation rocks are very strong. The result of their discovery resulted in all of the vaulted ceilings and domes of all the cathedrals as well as all of the arched structures such as the bridge over the New River gorge. Back

20 Elastic Deformation Hitting a baseball with a bat is a great example of elastic deformation. At the moment of impact the bat bends and the ball flattens) on one side. Both bat and ball are deformed. However, both return to their original shape. This is the basic definition of elastic deformation. Kicking a football or soccer ball also demonstrates elastic deformation because both your foot and the ball return to their original shape. Back

21 Faulting: The Brittle Deformation of Rocks
Brittle failure of rocks under compression and tension creates faults. Faults are breaks in Earth’s crust along which there is movement. In both compression and tension, the break occurs at an angle to the direction of stress; the difference being in the relative movement of the rock mass on opposite sides of the fault. Historically, the mass of rock above the fault is called the hanging wall while the mass below the fault is called the foot wall. These are terms originated by miners following beds of ore that encountered faults in the mine. Faults formed under tensional forces are called normal faults and are described as a fault where the hanging wall has moved down relative to the foot wall. Faults formed under non-rotational compression are called thrust or reverse faults, where, in both cases, the hanging wall has moved up relative to the foot wall. Back

22 Folding: The Plastic Deformation of Rocks
Plastic deformation of rocks does not break the rocks but folds them. Folds do not form at or near Earth’s surface where rocks are most brittle but rather at depth where increased temperatures and pressures result in a more plastic response. There are three types of folds: 1) monoclines, 2) anticlines, and 3) synclines. A monocline is a regional steepening of an otherwise uniform dip Anticlines and synclines usually occur together and are the result of compressive forces. Anticlines are upwarps in Earth’s crust while synclines are downwarps. The limb (side) of an anticline is also the limb of the adjacent syncline! Back

Download ppt "Characteristics Of Sedimentary Rocks"

Similar presentations

Ads by Google