How Do We Recognize and Interpret Sedimentary Rocks in the Rock Record? (Based Closely on the University of Washington ESS 101 Lab 5: Sedimentary Rocks)

NAME______PERIOD______DATE______From Sand to Stone: How do we recognize and interpret sedimentary rocks in the rock record? (Based closely on the University of Washington ESS 101 Lab 5: Sedimentary Rocks)

Introduction:

Rock breaks down as it interacts with the surface environment. The solid particles and dissolved ions (charged atoms and molecules) freed by this action are transported by water, wind, gravity, and glaciers from their source to depositional basins (the place where they are deposited). This collection of loosely packed, unconsolidated mineral or rock fragments is called sediment. In time, sediment is buried, compacted, and lithified to form sedimentary rock. Careful examination of the mineral composition and texture of many sedimentary rocks provide clues to the: (1) original source of the sediment (provenance); (2) type and extent of the weathering processes by which the source rock was broken down; (3) agent (water, wind, gravity, and ice) that transported the sediment and, in some cases, the duration of transport; (4) physical, chemical, and biological environment in which the sediment was deposited, and; (5) changes that may have occurred after deposition (diagenesis).

Grading Grading is a term that describes how grain size CHANGES with depth in a rock or sediments as they are deposited. We will describe the grading of rocks as follows:

Ungraded: the sample has the same range of grain sizes from top to bottom, or grain size does not vary with depth.

Fining upward: the grain sizes become progressively smaller from bottom to top. This is typical of sediments of various sizes that have been stirred up and then settle through a column of water. The largest grains will settle out first (cobbles, pebbles, sand), the silts next, and the clay-sizes last. This is a characteristic of TURBIDITE DEPOSITS, another name for marine landslide deposits.

Coarsening upward: the grain sizes become coarser from bottom to top. This is sometimes called reverse grading.

Your teacher will show you a sample or diagram of each, and show you a settling column. Draw these, and label your diagrams (8 pts) Ungraded:

Fining upward:

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Coarsening upward:

Settling column: What type of grading is represented here? Draw and explain.

Activity 1: Exploring Mineral Composition The composition of a clastic sedimentary rock is, in part, a function of the source rock from which the original sediment was derived (its provenance). Mineralogy is also governed by the distance that sediment is transported. Prolonged transport allows extensive chemical and mechanical breakdown of unstable minerals. Thus, with increased distance of transport, the proportion of more stable minerals (mostly quartz and clay minerals) increases relative to the proportion of chemically unstable minerals (Table 5-1). Most Stable (last longest at Earth’s surface) Iron Oxides Aluminum Oxides Quartz Clay Minerals Muscovite Orthoclase Biotite Na Plagioclase Amphibole Pyroxene Ca Plagioclase Olivine Calcite Evaporites Least Stable (easily reacted away at Earth’s surface) Table 5-1: Stability of common minerals under weathering conditions at the surface of the Earth.

Most chemical and biochemical sedimentary rocks are composed predominantly of one mineral and commonly contain little, if any, clastic debris. The diagnostic properties of common sedimentary rock-forming minerals are listed below.

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Diagnostic Mineral Properties: Quartz Colorless, white, or gray; exterior may be frosted; broken grains are glassy; scratches glass; (grains or cement) Orthoclase Usually white or pink; 2 cleavages at 90°; commonly angular Biotite Shiny, black sheets (golden if altered); one perfect cleavage Muscovite Shiny, silvery sheets; one perfect cleavage Calcite White, gray, black; doesn't scratch glass; reacts with acid; (may be cement) Halite White, light gray, to colorless; tastes like salt; breaks into cubes Gypsum White to gray; can be scratched with fingernail Iron Oxides Yellow, orange, red, or brown (rust); usually very small particles; mainly a cement Clay White, gray, green, red, black; clay-sized particles; can be scratched with fingernail; earthy feel and smell. Organically-produced material (from organisms) may also make up significant amounts of a given sedimentary rock. These materials may include shell fragments, teeth, bones, plant remains, or other organic debris.

Identify the six common sedimentary rock-forming minerals in your tray (specimens M-1 through M-6). You identified many of these minerals in the Minerals Lab. Refer to your mineral identification charts (on the website, or in the packet in lab) and the diagnostic properties of sedimentary rock-forming minerals listed above. (6 pts) Mineral Name Mineral Name M-1 M-4

M-2 M-5

M-3 M-6

Which mineral sample would you LEAST expect to find in a sedimentary (clastic) rock that is more than 1 million years old or older? WHY? Base your answer on the information above. (2 pts)

Which mineral sample would you expect to find in a 1 million year old, or older sedimentary rock? WHY? BE SPECIFIC. (2 pts)

NAME______PERIOD______DATE______For Rocks A, B and C, name the most common mineral found in each sample. Look at it under magnification, use the mineral testing kit, or use dilute HCl to test your hypothesis. (3 pts)

Most common mineral Evidence (test)

Rock-A

Rock-B

Rock-C

Describe how you think either Rock A, B or C formed? Is the rock a chemical or detrital sedimentary rock? How did it form, based on what you observe in the sample, and what you know of the rock cycle and mineral formation? (4 pts)

NAME______PERIOD______DATE______Activity 2: Comparing and describing clastic sediments and sedimentary rocks.

Texture Sedimentary rocks containing clasts or grains of rock, minerals, or fossils have a clastic texture. Grains are not intergrown with each other, but are generally bound together or cemented by a chemical precipitate of silica, calcite, or iron oxide. If the clastic texture results from abundant fossils or fossil fragments, the rock is bioclastic, and as you saw in last week's lab, pyroclastic refers to volcanic rocks with a clastic texture. When describing the texture of a clastic sedimentary rock, it is important to look at the grain size, grain roundness, and grain-size sorting.

Grain Size Classification of clastic sedimentary rocks is based on the average diameter of constituent fragments. Grain size can be divided into four classes: (1) Coarse-grained (boulder-, cobble-, and pebble-sized) – larger than 2 mm. (2) Medium-grained (sand-sized) – between 2 mm and 0.062 mm. (3) Fine-grained (silt-sized) – between 0.062 mm and 0.005 mm. Individual grains may be too small to be seen, but rock has a distinctive “gritty” feel when rubbed. (4) Very fine-grained (clay-sized) – less than 0.005 mm. Individual grains are too small to be seen and the rock feels smooth when rubbed.

Figure 5-2: Size scale for use when describing the grain size of clastic sedimentary rocks. Size is, in part, a function of the velocity of the currents that transport sediment (for wind and water transport). The particle size that is deposited decreases as water velocity decreases. In non-flowing bodies of water, such as lakes and parts of the ocean, movement of water is partially governed by the depth to which the motions of surface waves may reach. In these environments, sediment size generally decreases with increasing water depth. Clastic sediment size is also controlled by the nature of the transporting medium. Because of the buoyancy of water, even slow-moving streams can carry much larger particles than wind. Glaciers have a different method for transporting material than either water or wind because particles are frozen into the flowing ice. In glaciers, grains are not supported by the energy of the flow, and very large material may be transported.

NAME______PERIOD______DATE______Rank sediment samples S-1, S-2, and S-3 from least to greatest grain size, and describe the size of particles, and energy of the (water) depositional environment below in the table. (6 pts) Sample Rank(1 Grain size descriptor Energy of water that smallest, 3 deposited grains largest) S-1

S-2

S-3

Rank rock samples R-1, R-2, and R-3 from least to greatest grain size, and describe the size of particles, and energy of the (water) depositional environment below in the table. (6 pts) Sample Rank(1 Grain size descriptor Energy of water that smallest, 3 deposited grains (High, med, largest) low) R-1

R-2

R-3

Grain Rounding Roundness is a measure of the angularity of fragments within clastic sedimentary rocks. It ranges from angular to rounded and may be estimated by visual comparison with Figure 5-3.

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Figure 5-3: Scale for use when describing the roundness of fragments within clastic sedimentary rocks.

Row 1 in Figure 5-3 illustrates generally equidimensional grains and Row 2 illustrates elongate grains. The degree of grain rounding, in part, depends upon the distance sediment is transported. Clastic grains are mechanically abraded during wind and water transport and become more rounded the farther they are transported.

Grain-Size Sorting

The extent of grain-size variation within a clastic rock is termed the degree of sorting (Figure 5- 4). Rocks that contain grains of uniform size are well-sorted. If the clast sizes vary, a clastic rock is termed poorly-sorted. Terms such as moderately sorted may be used to describe textures intermediate between well-sorted and poorly-sorted.

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Figure 5-4: Diagrams illustrating grain-size sorting in clastic sedimentary rocks. The degree of sediment sorting is influenced by the rate of deposition and the energy within the depositional environment. Sediment deposited rapidly in areas of little current or wave action is poorly-sorted because there is little chance for the removal of fine-sized grains. There is more opportunity for size sorting when sediment slowly accumulates in a high-energy environment. Therefore, to a certain degree, size sorting can be a measure of sediment reworking within a depositional environment.

Wind-deposited sands tend to be small grain size, and well-sorted, compared to water-transported sands. They are not necessarily well-rounded however.

For the beach and rock samples listed, describe the degree of rounding and sorting for each sample. (8 pts) Sediment Grain size Degree of Degree of Location Particle sample Rounding Sorting collected types: Rock ®, (listed on or mineral (M), outside of or shell container) fragments (SF) S-4

S-5

S-6

S-7

NAME______PERIOD______DATE______Rock Grain size Degree of Degree of Sorting Particle types: sample Rounding Rock (R), mineral (M), or shell fragments (SF) R-4

R-5

R-6

R-7

(8 pts) Based on the data you collected above, which, if any rocks R-4 through R-7 look like they could be formed from one or more of the beach samples? Describe how you arrived at your conclusion. Refer to your data. (2 pts)

What is the name of a rock formed from sand-sized particles? (1 pt)

Silt-sized particles? (1 pt)

Clay or mud-sized particles? (1 pt)

NAME______PERIOD______DATE______Activity 3: Sedimentary Structures and Environments of Deposition One of the most important goals of rock study is to learn how, and under what conditions, a particular rock formed. If we know these, we can reconstruct the geologic past, predict where we might find ore deposits or fossil fuels, reconstruct how climate conditions have varied in the past, and even formulate hypotheses about the future.

We can learn how and under what conditions ancient sediments formed by studying the environments in which modern sediments accumulate.

Sedimentary structures are features in clastic sedimentary rocks that formed during or after deposition of the sediment, but before lithification. They are important because they provide evidence of the transporting agent and the environment in which the sediments where deposited.

The most common sedimentary structures are described below. Stratification, the layering of sediment, is the most obvious type of sedimentary structure. Most sediment accumulates in horizontal layers called strata or beds. The top or bottom surface of a bed is called a bedding plane, and it represents an exposed surface that existed between sedimentary depositional events.

Inclined stratification is referred to as cross-bedding. Cross-bedding in a sedimentary rock indicates that the sediment was transported by a current (wind or water) when it was deposited.

Cross-bedding can be used to tell the direction of current, as shown in Figure 5-5 below.

Figure 5-5: Figure showing cross-beds and their relationship with current flow direction. Ripple marks are wave-like features found on bedding planes. Oscillation ripple marks are symmetrical and commonly form where the back-and-forth motion of water waves shaped the bottom sediment (Figure 5-6A). These can occur only in relatively shallow water – less than 10 meters for normal waves and up to 200 meters for storm waves. Current ripple marks form when wind and water currents shape the loose sediment into asymmetrical wave forms whose gentle slope is on the side from which the current came (Figure 5-6B).

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Figure 5-6: Diagrams showing the formation of (A) oscillatory ripples and (B) current ripples. In graded beds (Figure 5-7), larger grains on the bottom usually grade upwards into finer grains on the top. Graded beds form when a sediment-laden (turbidity) current slows after flowing down an underwater slope; larger grains settle out first, smaller ones last.

Figure 5-7: Diagram showing two graded beds. The coarsest grains are on the bottom; the finest grains are on top.

Mud cracks form when mud dries and shrinks. When sediment is deposited on top of cracked mud, some of the sediment falls into the cracks, and they are preserved in the sedimentary record. The presence of mud cracks indicates a depositional environment in which periodic wetting and drying occurred.

Some shales also preserve ancient raindrop impressions.

NAME______PERIOD______DATE______For each of the following rock samples, describe the features you see. Be as specific as possible, and refer to the information from previous activities, as well as the information above. Put your information into the table below. (15 pts) Rock sample Minerals or Grain size Sorting Rounding Fossils, Rock materials features or name present structures R-8

R-9

R-10

R-11

R-12

For ONE of these samples, describe the materials it formed from (source rock), the process that eroded and deposited it, and the type of location and environment where this might have occurred. Be as specific as possible. Refer to the information in the tables you filled in above, and information given below to defend your decision about depositional environment. (5 pts)

NAME______PERIOD______DATE______Depositional Environment Characteristic Sedimentary Rocks The most important depositional environments and the rock types that are characteristic of those environments are listed on the next page. CONTINENTAL (not marine) Stream Channel Stream Floodplain Shale, some mud cracks, and siltstone; coal may also be present.

Alluvial Fan Conglomerate, feldspar-rich sandstone, poor sorting, cross-beds. Deserts Sandstone, well-sorted, large cross-beds.

Glacier Poorly sorted, unstratified conglomerate; particles angular to rounded and may have scratches. (Glacial streams are similar to stream channel deposits.)

Swamp Coal.

Lake Shale in deep water Sandstone and conglomerate near shore (beach). Arid, hot Evaporites (rock salt, rock gypsum)

TRANSITIONAL (Coastal) Delta Complex association of marine and nonmarine sandstone, siltstone, and shale, possibly with cross-beds and ripple marks; coal common.

Beach/Barrier Island Fine- to medium-grained, well-sorted sandstone; crossbeds common.

Tidal Flat Shale, siltstone, and fine-grained sandstone; ripple marks, cross-beds, mud cracks; evaporites possible.

MARINE (off shore) Continental Shelf Sandstone: cross-beds, ripple marks common; shale; various limestones.

Reef Fossiliferous limestone, coral and algae fossils common.

Continental Slope/Rise Shale, muddy sandstones; graded bedding common.

NAME______PERIOD______DATE______Deep Marine Chert, chalk, crystalline limestone, shale.

When the transporting agent (whether it be water, wind, or ice) slows or melts, the particles in transport settle and accumulate. Such sediment, consisting of broken fragments of preexisting rocks (clasts), is called clastic sediment.

Chemical sediment is deposited when the ions that are dissolved in the water precipitate to form a solid. The solid, usually a mineral crystal, is a chemical precipitate, and the process of forming a solid from the ions in solution is chemical precipitation. Calcite, gypsum, and halite are all examples of this.

Inorganic chemical precipitation takes place within the depositional basin when the chemistry of the water is appropriate. For example, evaporation of seawater causes the concentration of Na+ (sodium) and Cl- (chloride) ions in the remaining liquid to become so great that minerals precipitate; this is how rock salt and rock gypsum form.

Biochemical precipitation, on the other hand, involves living organisms. Animals and plants extract calcium carbonate and silica from seawater to build skeletal structures such as shells or, in the case of some algae, tiny carbonate crystals that hold up the soft organic parts. When the organisms die, the skeletal parts sink and become part of the bottom sediment. This type of deposit forms chert or chalk.

Organic sediment forms directly from the decay of plant or, less commonly, animal material. The most common examples are peat and coal, which are formed from partially decayed vegetation that accumulated in a swamp.

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A rock is formed! Lithification and Diagenesis: The processes by which soft sediment is lithified (turned to rock) are collectively termed Diagenesis.

Lithification happens in two ways: (1) the sediments can become compacted by the weight of overlying sediments, and/or (2) sediment grains can be cemented together by material that precipitates from fluids passing through them. Common cementing materials are SiO2 (silica), Fe2O3 (iron oxide) and CaCO3 (calcite).

At higher temperature and pressure conditions, diagenesis merges with the lowest grades of Metamorphism.

For the samples in the lab, name, describe and draw one most likely formed from compaction, and name, describe and draw one that most likely formed from process cementation, as described above. (6 pts)

Compaction sample: Rock ______

Draw and describe:

What is the evidence that this rock formed from compaction of sediment clasts?

Cementation sample: Rock ______

Draw and describe:

What is the evidence that this rock formed from the cementation of sediment clasts?

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