SEDIMENTARY ROCKS are types of rock that are formed by the deposition
and subsequent cementation of that material at the Earth\'s surface
and within bodies of water.
The sedimentary rock cover of the continents of the Earth\'s crust is extensive (73% of the Earth's current land surface ), but the total contribution of sedimentary rocks is estimated to be only 8% of the total volume of the crust. Sedimentary rocks are only a thin veneer over a crust consisting mainly of igneous and metamorphic rocks . Sedimentary rocks are deposited in layers as strata , forming a structure called bedding . The study of sedimentary rocks and rock strata provides information about the subsurface that is useful for civil engineering , for example in the construction of roads , houses , tunnels , canals or other structures. Sedimentary rocks are also important sources of natural resources like coal , fossil fuels , drinking water or ores .
The study of the sequence of sedimentary rock strata is the main
source for an understanding of the Earth\'s history , including
palaeogeography , paleoclimatology and the history of life . The
scientific discipline that studies the properties and origin of
sedimentary rocks is called sedimentology .
Sedimentology is part of
both geology and physical geography and overlaps partly with other
disciplines in the Earth sciences , such as pedology , geomorphology ,
geochemistry and structural geology . Sedimentary rocks have also been
* 1 Classification based on origin
* 1.1 Clastic sedimentary rocks
* 1.1.1 Conglomerates and breccias * 1.1.2 Sandstones * 1.1.3 Mudrocks
* 1.2 Biochemical sedimentary rocks * 1.3 Chemical sedimentary rocks * 1.4 "Other" sedimentary rocks
* 2 Compositional classification schemes
* 3 Deposition and transformation
* 4 Properties
* 4.1 Color * 4.2 Texture * 4.3 Mineralogy * 4.4 Fossils * 4.5 Primary sedimentary structures * 4.6 Secondary sedimentary structures
* 5 Sedimentary environments
* 6 Sedimentary basins
* 6.1 Influence of astronomical cycles
* 10 References
* 10.1 Bibliography
* 11 External links
CLASSIFICATION BASED ON ORIGIN
Sedimentary rocks can be subdivided into four groups based on the processes responsible for their formation: clastic sedimentary rocks, biochemical (biogenic) sedimentary rocks, chemical sedimentary rocks, and a fourth category for "other" sedimentary rocks formed by impacts, volcanism , and other minor processes.
CLASTIC SEDIMENTARY ROCKS
Clastic sedimentary rocks are composed of other rock fragments that were cemented by silicate minerals. Clastic rocks are composed largely of quartz , feldspar , rock (lithic) fragments, clay minerals , and mica ; any type of mineral may be present, but they in general represent the minerals that exist locally.
Clastic sedimentary rocks, are subdivided according to the dominant particle size. Most geologists use the Udden-Wentworth grain size scale and divide unconsolidated sediment into three fractions: gravel (>2 mm diameter), sand (1/16 to 2 mm diameter), and mud (clay is 90% quartz grains * Feldspathic sandstones have 90%) quartz grains and have little or no clayey matrix between the grains, a lithic wacke would have abundant lithic grains and abundant muddy matrix, etc.
Although the Dott classification scheme is widely used by sedimentologists, common names like greywacke , arkose , and quartz sandstone are still widely used by non-specialists and in popular literature.
Lower Antelope Canyon was carved out of the surrounding sandstone by both mechanical weathering and chemical weathering. Wind, sand, and water from flash flooding are the primary weathering agents.
Mudrocks are sedimentary rocks composed of at least 50% silt - and clay -sized particles. These relatively fine-grained particles are commonly transported by turbulent flow in water or air, and deposited as the flow calms and the particles settle out of suspension .
Most authors presently use the term "mudrock" to refer to all rocks composed dominantly of mud. Mudrocks can be divided into siltstones, composed dominantly of silt-sized particles; mudstones with subequal mixture of silt- and clay-sized particles; and claystones, composed mostly of clay-sized particles. Most authors use "shale " as a term for a fissile mudrock (regardless of grain size) although some older literature uses the term "shale" as a synonym for mudrock.
BIOCHEMICAL SEDIMENTARY ROCKS
Biochemical sedimentary rocks are created when organisms use materials dissolved in air or water to build their tissue. Examples include:
* Most types of limestone are formed from the calcareous skeletons
of organisms such as corals , mollusks , and foraminifera .
CHEMICAL SEDIMENTARY ROCKS
Chemical sedimentary rock forms when mineral constituents in solution become supersaturated and inorganically precipitate . Common chemical sedimentary rocks include oolitic limestone and rocks composed of evaporite minerals, such as halite (rock salt), sylvite , barite and gypsum .
"OTHER" SEDIMENTARY ROCKS
This fourth miscellaneous category includes rocks formed by Pyroclastic flows , impact breccias , volcanic breccias , and other relatively uncommon processes.
COMPOSITIONAL CLASSIFICATION SCHEMES
Alternatively, sedimentary rocks can be subdivided into compositional groups based on their mineralogy:
* SILICICLASTIC SEDIMENTARY ROCKS , are dominantly composed of silicate minerals. The sediment that makes up these rocks was transported as bed load , suspended load , or by sediment gravity flows . Siliciclastic sedimentary rocks are subdivided into conglomerates and breccias , sandstone , and mudrocks .
* CARBONATE SEDIMENTARY ROCKS are composed of calcite (rhombohedral CaCO 3), aragonite (orthorhombic CaCO 3), dolomite (CaMg(CO 3) 2), and other carbonate minerals based on the CO2− 3 ion. Common examples include limestone and dolostone . * EVAPORITE SEDIMENTARY ROCKS are composed of minerals formed from the evaporation of water. The most common evaporite minerals are carbonates (calcite and others based on CO2− 3), chlorides (halite and others built on Cl− ), and sulfates (gypsum and others built on SO2− 4). Evaporite rocks commonly include abundant halite (rock salt), gypsum , and anhydrite . * ORGANIC-RICH SEDIMENTARY ROCKS have significant amounts of organic material, generally in excess of 3% total organic carbon. Common examples include coal , oil shale as well as source rocks for oil and natural gas.
* SILICEOUS SEDIMENTARY ROCKS are almost entirely composed of silica (SiO 2), typically as chert , opal , chalcedony or other microcrystalline forms. * IRON-RICH SEDIMENTARY ROCKS are composed of >15% iron; the most common forms are banded iron formations and ironstones . * PHOSPHATIC SEDIMENTARY ROCKS are composed of phosphate minerals and contain more than 6.5% phosphorus ; examples include deposits of phosphate nodules , bone beds, and phosphatic mudrocks.
DEPOSITION AND TRANSFORMATION
SEDIMENT TRANSPORT AND DEPOSITION
Sedimentary rocks are formed when sediment is deposited out of air, ice, wind, gravity, or water flows carrying the particles in suspension . This sediment is often formed when weathering and erosion break down a rock into loose material in a source area. The material is then transported from the source area to the deposition area. The type of sediment transported depends on the geology of the hinterland (the source area of the sediment). However, some sedimentary rocks, such as evaporites , are composed of material that form at the place of deposition. The nature of a sedimentary rock, therefore, not only depends on the sediment supply, but also on the sedimentary depositional environment in which it formed.
Pressure solution at work in a clastic rock . While material dissolves at places where grains are in contact, that material may recrystallize from the solution and act as cement in open pore spaces. As a result, there is a net flow of material from areas under high stress to those under low stress, producing a sedimentary rock becomes more compact and harder. Loose sand can become sandstone in this way. Main article: diagenesis
The term diagenesis is used to describe all the chemical, physical, and biological changes, exclusive of surface weathering, undergone by a sediment after its initial deposition. Some of those processes cause the sediment to consolidate into a compact, solid substance from the originally loose material. Young sedimentary rocks, especially those of Quaternary age (the most recent period of the geologic time scale ) are often still unconsolidated. As sediment deposition builds up, the overburden (lithostatic) pressure rises, and a process known as lithification takes place.
Sedimentary rocks are often saturated with seawater or groundwater , in which minerals can dissolve, or from which minerals can precipitate . Precipitating minerals reduce the pore space in a rock, a process called cementation . Due to the decrease in pore space, the original connate fluids are expelled. The precipitated minerals form a cement and make the rock more compact and competent . In this way, loose clasts in a sedimentary rock can become "glued" together.
When sedimentation continues, an older rock layer becomes buried deeper as a result. The lithostatic pressure in the rock increases due to the weight of the overlying sediment. This causes compaction, a process in which grains mechanically reorganize. Compaction is, for example, an important diagenetic process in clay, which can initially consist of 60% water. During compaction, this interstitial water is pressed out of pore spaces. Compaction can also be the result of dissolution of grains by pressure solution . The dissolved material precipitates again in open pore spaces, which means there is a net flow of material into the pores. However, in some cases, a certain mineral dissolves and does not precipitate again. This process, called leaching , increases pore space in the rock.
Some biochemical processes, like the activity of bacteria , can
affect minerals in a rock and are therefore seen as part of
Burial of rocks due to ongoing sedimentation leads to increased pressure and temperature, which stimulates certain chemical reactions. An example is the reactions by which organic material becomes lignite or coal . When temperature and pressure increase still further, the realm of diagenesis makes way for metamorphism , the process that forms metamorphic rock .
A piece of a banded iron formation , a type of rock that
consists of alternating layers with iron(III) oxide (red) and iron(II)
oxide (grey). BIFs were mostly formed during the
The color of a sedimentary rock is often mostly determined by iron , an element with two major oxides: iron(II) oxide and iron(III) oxide . Iron(II) oxide (FeO) only forms under low oxygen (anoxic ) circumstances and gives the rock a grey or greenish colour. Iron(III) oxide (Fe2O3) in a richer iron environment is often found in the form of the mineral hematite and gives the rock a reddish to brownish colour. In arid continental climates rocks are in direct contact with the atmosphere, and oxidation is an important process, giving the rock a red or orange colour. Thick sequences of red sedimentary rocks formed in arid climates are called red beds . However, a red colour does not necessarily mean the rock formed in a continental environment or arid climate.
The presence of organic material can colour a rock black or grey. Organic material is formed from dead organisms, mostly plants. Normally, such material eventually decays by oxidation or bacterial activity. Under anoxic circumstances, however, organic material cannot decay and leaves a dark sediment, rich in organic material. This can, for example, occur at the bottom of deep seas and lakes. There is little water mixing in such environments, as a result oxygen from surface water is not brought down, and the deposited sediment is normally a fine dark clay. Dark rocks, rich in organic material, are therefore often shales .
Diagram showing well-sorted (left) and poorly sorted (right) grains
The size , form and orientation of clasts (the original pieces of rock) in a sediment is called its texture . The texture is a small-scale property of a rock, but determines many of its large-scale properties, such as the density , porosity or permeability .
The 3D orientation of the clasts is called the fabric of the rock.
Between the clasts, the rock can be composed of a matrix (a cement)
that consists of crystals of one or more precipitated minerals. The
size and form of clasts can be used to determine the velocity and
direction of current in the sedimentary environment that moved the
clasts from their origin; fine, calcareous mud only settles in quiet
water while gravel and larger clasts are moved only by rapidly moving
water. The grain size of a rock is usually expressed with the
The form of the clasts can reflect the origin of the rock.
Coquina , a rock composed of clasts of broken shells, can only form in energetic water. The form of a clast can be described by using four parameters:
* Surface texture describes the amount of small-scale relief of the
surface of a grain that is too small to influence the general shape.
* rounding describes the general smoothness of the shape of a grain.
Chemical sedimentary rocks have a non-clastic texture, consisting entirely of crystals. To describe such a texture, only the average size of the crystals and the fabric are necessary.
Most sedimentary rocks contain either quartz (especially siliciclastic rocks) or calcite (especially carbonate rocks ). In contrast to igneous and metamorphic rocks, a sedimentary rock usually contains very few different major minerals. However, the origin of the minerals in a sedimentary rock is often more complex than in an igneous rock. Minerals in a sedimentary rock can have formed by precipitation during sedimentation or by diagenesis. In the second case, the mineral precipitate can have grown over an older generation of cement. A complex diagenetic history can be studied by optical mineralogy , using a petrographic microscope .
Fossil-rich layers in a sedimentary rock, Año Nuevo State
Among the three major types of rock, fossils are most commonly found in sedimentary rock. Unlike most igneous and metamorphic rocks, sedimentary rocks form at temperatures and pressures that do not destroy fossil remnants. Often these fossils may only be visible under magnification .
Dead organisms in nature are usually quickly removed by scavengers ,
bacteria , rotting and erosion, but sedimentation can contribute to
exceptional circumstances where these natural processes are unable to
work, causing fossilisation. The chance of fossilisation is higher
when the sedimentation rate is high (so that a carcass is quickly
buried), in anoxic environments (where little bacterial activity
occurs) or when the organism had a particularly hard skeleton. Larger,
well-preserved fossils are relatively rare. Burrows in a
turbidite , made by crustaceans , San Vincente Formation (early Eocene
) of the Ainsa Basin , southern foreland of the
Fossils can be both the direct remains or imprints of organisms and their skeletons. Most commonly preserved are the harder parts of organisms such as bones, shells, and the woody tissue of plants. Soft tissue has a much smaller chance of being fossilized, and the preservation of soft tissue of animals older than 40 million years is very rare. Imprints of organisms made while they were still alive are called trace fossils , examples of which are burrows , footprints , etc.
As a part of a sedimentary or metamorphic rock, fossils undergo the same diagenetic processes as does the containing rock. A shell consisting of calcite can, for example, dissolve while a cement of silica then fills the cavity. In the same way, precipitating minerals can fill cavities formerly occupied by blood vessels , vascular tissue or other soft tissues. This preserves the form of the organism but changes the chemical composition, a process called permineralization . The most common minerals involved in permineralization are cements of carbonates (especially calcite), forms of amorphous silica (chalcedony , flint , chert ) and pyrite . In the case of silica cements, the process is called lithification .
At high pressure and temperature, the organic material of a dead organism undergoes chemical reactions in which volatiles such as water and carbon dioxide are expulsed. The fossil, in the end, consists of a thin layer of pure carbon or its mineralized form, graphite . This form of fossilisation is called carbonisation . It is particularly important for plant fossils. The same process is responsible for the formation of fossil fuels like lignite or coal .
PRIMARY SEDIMENTARY STRUCTURES
Cross-bedding in a fluviatile sandstone , Middle Old Red
Structures in sedimentary rocks can be divided into 'primary' structures (formed during deposition) and 'secondary' structures (formed after deposition). Unlike textures, structures are always large-scale features that can easily be studied in the field. Sedimentary structures can indicate something about the sedimentary environment or can serve to tell which side originally faced up where tectonics have tilted or overturned sedimentary layers.
Sedimentary rocks are laid down in layers called beds or strata . A bed is defined as a layer of rock that has a uniform lithology and texture. Beds form by the deposition of layers of sediment on top of each other. The sequence of beds that characterizes sedimentary rocks is called bedding . Single beds can be a couple of centimetres to several meters thick. Finer, less pronounced layers are called laminae, and the structure it forms in a rock is called lamination . Laminae are usually less than a few centimetres thick. Though bedding and lamination are often originally horizontal in nature, this is not always the case. In some environments, beds are deposited at a (usually small) angle. Sometimes multiple sets of layers with different orientations exist in the same rock, a structure called cross-bedding . Cross-bedding forms when small-scale erosion occurs during deposition, cutting off part of the beds. Newer beds then form at an angle to older ones.
The opposite of cross-bedding is parallel lamination, where all sedimentary layering is parallel. Differences in laminations are generally caused by cyclic changes in the sediment supply, caused, for example, by seasonal changes in rainfall, temperature or biochemical activity. Laminae that represent seasonal changes (similar to tree rings ) are called varves . Any sedimentary rock composed of millimeter or finer scale layers can be named with the general term laminite. When sedimentary rocks have no lamination at all, their structural character is called massive bedding.
Graded bedding is a structure where beds with a smaller grain size occur on top of beds with larger grains. This structure forms when fast flowing water stops flowing. Larger, heavier clasts in suspension settle first, then smaller clasts. Although graded bedding can form in many different environments, it is a characteristic of turbidity currents .
The surface of a particular bed, called the bedform , can be indicative of a particular sedimentary environment, too. Examples of bed forms include dunes and ripple marks . Sole markings, such as tool marks and flute casts, are groves dug into a sedimentary layer that are preserved. These are often elongated structures and can be used to establish the direction of the flow during deposition.
Ripple marks also form in flowing water. There are two types of ripples: symmetric and asymmetric. Environments where the current is in one direction, such as rivers, produce asymmetric ripples. The longer flank of such ripples is on the upstream side of the current. Symmetric wave ripples occur in environments where currents reverse directions, such as tidal flats.
Mudcracks are a bed form caused by the dehydration of sediment that occasionally comes above the water surface. Such structures are commonly found at tidal flats or point bars along rivers.
SECONDARY SEDIMENTARY STRUCTURES
Secondary sedimentary structures are those which formed after deposition. Such structures form by chemical, physical and biological processes within the sediment. They can be indicators of circumstances after deposition. Some can be used as way up criteria .
Organic materials in a sediment can leave more traces than just
fossils. Preserved tracks and burrows are examples of trace fossils
(also called ichnofossils). Such traces are relatively rare. Most
trace fossils are burrows of molluscs or arthropods . This burrowing
is called bioturbation by sedimentologists. It can be a valuable
indicator of the biological and ecological environment that existed
after the sediment was deposited. On the other hand, the burrowing
activity of organisms can destroy other (primary) structures in the
sediment, making a reconstruction more difficult. Chert
concretions in chalk , Middle Lefkara Formation (upper
Secondary structures can also form by diagenesis or the formation of
a soil (pedogenesis ) when a sediment is exposed above the water
level. An example of a diagenetic structure common in carbonate rocks
is a stylolite . Stylolites are irregular planes where material was
dissolved into the pore fluids in the rock. This can result in the
precipitation of a certain chemical species producing colouring and
staining of the rock, or the formation of concretions . Concretions
are roughly concentric bodies with a different composition from the
host rock. Their formation can be the result of localized
precipitation due to small differences in composition or porosity of
the host rock, such as around fossils, inside burrows or around plant
roots. In carbonate based rocks such as limestone or chalk , chert or
flint concretions are common, while terrestrial sandstones can have
After deposition, physical processes can deform the sediment,
producing a third class of secondary structures.
Sedimentary dykes can also be formed in a cold climate where the soil is permanently frozen during a large part of the year. Frost weathering can form cracks in the soil that fill with rubble from above. Such structures can be used as climate indicators as well as way up structures.
The setting in which a sedimentary rock forms is called the sedimentary environment. Every environment has a characteristic combination of geologic processes and circumstances. The type of sediment that is deposited is not only dependent on the sediment that is transported to a place, but also on the environment itself.
A marine environment means that the rock was formed in a sea or ocean . Often, a distinction is made between deep and shallow marine environments. Deep marine usually refers to environments more than 200 m below the water surface. Shallow marine environments exist adjacent to coastlines and can extend to the boundaries of the continental shelf . The water movements in such environments have a generally higher energy than that in deep environments, as wave activity diminishes with depth. This means that coarser sediment particles can be transported and the deposited sediment can be coarser than in deeper environments. When the sediment is transported from the continent, an alternation of sand , clay and silt is deposited. When the continent is far away, the amount of such sediment deposited may be small, and biochemical processes dominate the type of rock that forms. Especially in warm climates, shallow marine environments far offshore mainly see deposition of carbonate rocks. The shallow, warm water is an ideal habitat for many small organisms that build carbonate skeletons. When these organisms die, their skeletons sink to the bottom, forming a thick layer of calcareous mud that may lithify into limestone . Warm shallow marine environments also are ideal environments for coral reefs , where the sediment consists mainly of the calcareous skeletons of larger organisms.
In deep marine environments, the water current working the sea bottom is small. Only fine particles can be transported to such places. Typically sediments depositing on the ocean floor are fine clay or small skeletons of micro-organisms. At 4 km depth, the solubility of carbonates increases dramatically (the depth zone where this happens is called the lysocline ). Calcareous sediment that sinks below the lysocline dissolves, as a result no limestone can be formed below this depth. Skeletons of micro-organisms formed of silica (such as radiolarians ) are not as soluble and still deposit. An example of a rock formed of silica skeletons is radiolarite . When the bottom of the sea has a small inclination, for example at the continental slopes , the sedimentary cover can become unstable, causing turbidity currents . Turbidity currents are sudden disturbances of the normally quite deep marine environment and can cause the geologically speaking instantaneous deposition of large amounts of sediment, such as sand and silt. The rock sequence formed by a turbidity current is called a turbidite .
The coast is an environment dominated by wave action. At a beach , dominantly denser sediment such as sand or gravel , often mingled with shell fragments, is deposited, while the silt and clay sized material is kept in mechanical suspension. Tidal flats and shoals are places that sometimes dry because of the tide . They are often cross-cut by gullies , where the current is strong and the grain size of the deposited sediment is larger. Where rivers enter the body of water, either on a sea or lake coast, deltas can form. These are large accumulations of sediment transported from the continent to places in front of the mouth of the river. Deltas are dominantly composed of clastic sediment (in contrast to chemical).
A sedimentary rock formed on land has a continental sedimentary
environment. Examples of continental environments are lagoons , lakes,
swamps , floodplains and alluvial fans . In the quiet water of swamps,
lakes and lagoons, fine sediment is deposited, mingled with organic
material from dead plants and animals. In rivers, the energy of the
water is much greater and can transport heavier clastic material.
Besides transport by water, sediment can in continental environments
also be transported by wind or glaciers.
Aeolian deposits can be quite striking. The depositional environment
Touchet Formation , located in the Northwestern
Sedimentary environments usually exist alongside each other in certain natural successions. A beach, where sand and gravel is deposited, is usually bounded by a deeper marine environment a little offshore, where finer sediments are deposited at the same time. Behind the beach, there can be dunes (where the dominant deposition is well sorted sand) or a lagoon (where fine clay and organic material is deposited). Every sedimentary environment has its own characteristic deposits. The typical rock formed in a certain environment is called its sedimentary facies . When sedimentary strata accumulate through time, the environment can shift, forming a change in facies in the subsurface at one location. On the other hand, when a rock layer with a certain age is followed laterally, the lithology (the type of rock) and facies eventually change. Shifting sedimentary facies in the case of transgression (above) and regression of the sea (below)
Facies can be distinguished in a number of ways: the most common are
by the lithology (for example: limestone, siltstone or sandstone) or
by fossil content.
Sedimentary environments can shift their geographical positions through time. Coastlines can shift in the direction of the sea when the sea level drops, when the surface rises due to tectonic forces in the Earth's crust or when a river forms a large delta. In the subsurface, such geographic shifts of sedimentary environments of the past are recorded in shifts in sedimentary facies. This means that sedimentary facies can change either parallel or perpendicular to an imaginary layer of rock with a fixed age, a phenomenon described by Walther\'s Law .
The situation in which coastlines move in the direction of the continent is called transgression . In the case of transgression, deeper marine facies are deposited over shallower facies, a succession called onlap . Regression is the situation in which a coastline moves in the direction of the sea. With regression, shallower facies are deposited on top of deeper facies, a situation called offlap .
The facies of all rocks of a certain age can be plotted on a map to give an overview of the palaeogeography . A sequence of maps for different ages can give an insight in the development of the regional geography.
Main article: sedimentary basin
Places where large-scale sedimentation takes place are called sedimentary basins . The amount of sediment that can be deposited in a basin depends on the depth of the basin, the so-called accommodation space . The depth, shape and size of a basin depend on tectonics , movements within the Earth's lithosphere . Where the lithosphere moves upward (tectonic uplift ), land eventually rises above sea level, so that and erosion removes material, and the area becomes a source for new sediment. Where the lithosphere moves downward (tectonic subsidence ), a basin forms and sedimentation can take place. When the lithosphere keeps subsiding, new accommodation space keeps being created.
A type of basin formed by the moving apart of two pieces of a
continent is called a rift basin .
When a piece of lithosphere that was heated and stretched cools again, its density rises, causing isostatic subsidence. If this subsidence continues long enough, the basin is called a sag basin . Examples of sag basins are the regions along passive continental margins , but sag basins can also be found in the interior of continents. In sag basins, the extra weight of the newly deposited sediments is enough to keep the subsidence going in a vicious circle . The total thickness of the sedimentary infill in a sag basins can thus exceed 10 km.
A third type of basin exists along convergent plate boundaries – places where one tectonic plate moves under another into the asthenosphere. The subducting plate bends and forms a fore-arc basin in front of the overriding plate—an elongated, deep asymmetric basin. Fore-arc basins are filled with deep marine deposits and thick sequences of turbidites. Such infill is called flysch . When the convergent movement of the two plates results in continental collision , the basin becomes shallower and develops into a foreland basin . At the same time, tectonic uplift forms a mountain belt in the overriding plate, from which large amounts of material are eroded and transported to the basin. Such erosional material of a growing mountain chain is called molasse and has either a shallow marine or a continental facies.
At the same time, the growing weight of the mountain belt can cause
isostatic subsidence in the area of the overriding plate on the other
side to the mountain belt. The basin type resulting from this
subsidence is called a back-arc basin and is usually filled by shallow
marine deposits and molasse. Cyclic alternation of competent and
less competent beds in the
Blue Lias at
INFLUENCE OF ASTRONOMICAL CYCLES
In many cases facies changes and other lithological features in sequences of sedimentary rock have a cyclic nature. This cyclic nature was caused by cyclic changes in sediment supply and the sedimentary environment. Most of these cyclic changes are caused by astronomic cycles. Short astronomic cycles can be the difference between the tides or the spring tide every two weeks. On a larger time-scale, cyclic changes in climate and sea level are caused by Milankovitch cycles : cyclic changes in the orientation and/or position of the Earth's rotational axis and orbit around the Sun. There are a number of Milankovitch cycles known, lasting between 10,000 and 200,000 years.
Relatively small changes in the orientation of the Earth's axis or length of the seasons can be a major influence on the Earth's climate. An example are the ice ages of the past 2.6 million years (the Quaternary period ), which are assumed to have been caused by astronomic cycles. Climate change can influence the global sea level (and thus the amount of accommodation space in sedimentary basins) and sediment supply from a certain region. Eventually, small changes in astronomic parameters can cause large changes in sedimentary environment and sedimentation.
The rate at which sediment is deposited differs depending on the location. A channel in a tidal flat can see the deposition of a few metres of sediment in one day, while on the deep ocean floor each year only a few millimetres of sediment accumulate. A distinction can be made between normal sedimentation and sedimentation caused by catastrophic processes. The latter category includes all kinds of sudden exceptional processes like mass movements , rock slides or flooding . Catastrophic processes can see the sudden deposition of a large amount of sediment at once. In some sedimentary environments, most of the total column of sedimentary rock was formed by catastrophic processes, even though the environment is usually a quiet place. Other sedimentary environments are dominated by normal, ongoing sedimentation.
In many cases, sedimentation occurs slowly. In a desert , for
example, the wind deposits siliciclastic material (sand or silt) in
some spots, or catastrophic flooding of a wadi may cause sudden
deposits of large quantities of detrital material, but in most places
eolian erosion dominates. The amount of sedimentary rock that forms is
not only dependent on the amount of supplied material, but also on how
well the material consolidates.
That new rock layers are above older rock layers is stated in the principle of superposition . There are usually some gaps in the sequence called unconformities . These represent periods where no new sediments were laid down, or when earlier sedimentary layers were raised above sea level and eroded away.
Sedimentary rocks contain important information about the history of
the Earth . They contain fossils , the preserved remains of ancient
plants and animals .
* ^ Wilkinson, Bruce H.; McElroy, Brandon J.; Kesler, Stephen E.;
Peters, Shanan E.; Rothman, Edward D. (2008). "Global geologic maps
are tectonic speedometers—Rates of rock cycling from area-age
frequencies". Geological Society of America Bulletin. 121: 760–779.
doi :10.1130/B26457.1 .
* ^ Buchner & Grapes (2011) , p. 24
* ^ A B Dott (1964)
* ^ A B Blatt et al. (1980) , p. 782
* ^ A B C Prothero & Schwab (2004)
* ^ A B Boggs (2006)
* ^ Stow (2005)
* ^ A B Levin (1987) , p. 57
* ^ Tarbuck & Lutgens (1999) , pp. 145–146
* ^ Boggs (1987) , p. 105
* ^ Tarbuck & Lutgens (1999) , pp. 156–157
* ^ Levin (1987) , p. 58
* ^ Boggs (1987) , pp. 112–115
* ^ Blatt et al. (1980) , pp. 55–58
* ^ Levin (1987) , p. 60
* ^ Blatt et al. (1980) , pp. 75–80
* ^ Folk (1965) , p. 62
* ^ For an overview of major minerals in siliciclastic rocks and
their relative stabilities, see Folk (1965) , pp. 62–64.
* ^ Stanley (1999) , pp. 60–61
* ^ Levin (1987) , p. 92
* ^ Stanley (1999) , p. 61
* ^ Levin (1987) , pp. 92–93
* ^ Tarbuck Press et al. (2003) , pp. 171–172.
* ^ Blatt et al. (1980) , pp. 133–135
* ^ For an explanation about graded bedding, see Boggs (1987) , pp.
143–144; Tarbuck Press et al. (2003) , p. 172.
* ^ Collinson et al. (2006) , pp. 46–52
* ^ Blatt et al. (1980) , pp. 155–157
* ^ Tarbuck Levin (1987) , pp. 93–95; and Collinson et al. (2006)
, pp. 216–232.
* ^ Collinson et al. (2006) , p. 215
* ^ For concretions, see Collinson et al. (2006) , pp. 206–215.
* ^ Collinson et al. (2006) , pp. 183–185
* ^ Collinson et al. (2006) , pp. 193–194
* ^ Collinson et al. (2006) , pp. 202–203
* ^ For an overview of different sedimentary environments, see
Press et al. (2003) or Einsele (2000) , part II.
* ^ For a definition of shallow marine environments, see Levin
(2003) , p. 63.
* ^ Tarbuck Nummedal, Dag, eds. (1978). The Channeled Scabland: A
Guide to the
* Andersen, B. G. & H. W. Borns, Jr. (1994). The
The Wikibook Historical