View source for Earth:Sediment

{{short description|Particulate solid matter that is deposited on the surface of land}}
[[File:Sediment plume at sea.jpg|thumb|upright=1.2| {{center|River discharging sediment into the ocean}}]]

'''Sediment''' is a naturally occurring material that is broken down by processes of [[Earth:Weathering|weathering]] and [[Earth:Erosion|erosion]], and is subsequently [[Physics:Sediment transport|transported]] by the action of wind, water, or ice or by the force of [[Physics:Gravity|gravity]] acting on the particles. For example, sand and [[Earth:Silt|silt]] can be carried in [[Chemistry:Suspension|suspension]] in river water and on reaching the sea bed deposited by [[Sedimentation|sedimentation]]; if buried, they may eventually become [[Earth:Sandstone|sandstone]] and [[Earth:Siltstone|siltstone]] ([[Earth:Sedimentary rock|sedimentary rock]]s) through [[Earth:Lithification|lithification]].

Sediments are most often transported by water (fluvial processes), but also wind ([[Earth:Aeolian processes|aeolian processes]]) and [[Earth:Glacier|glacier]]s. Beach sands and river channel deposits are examples of fluvial transport and [[Earth:Deposition (geology)|deposition]], though sediment also often settles out of slow-moving or standing water in lakes and oceans. Desert sand dunes and [[Earth:Loess|loess]] are examples of aeolian transport and deposition. Glacial [[Earth:Moraine|moraine]] deposits and [[Earth:Till|till]] are ice-transported sediments.

== Classification ==
[[File:Sediment in the Gulf of Mexico.jpg|thumb|Sediment in the Gulf of Mexico]]
[[File:Sediment off the Yucatan Peninsula.jpg|thumb|Sediment off the Yucatán Peninsula]]

Sediment can be classified based on its grain size, grain shape, and composition.

===Grain size===

Sediment size is measured on a log base 2 scale, called the "Phi" scale, which classifies particles by size from "colloid" to "boulder".

{| class="wikitable"
|-
! φ scale !! Size range<br>(metric) !! Size range<br>(inches) !! Aggregate class<br>(Wentworth) !! Other names
|-
| < −8 || &gt; 256&nbsp;mm || > 10.1 in || [[Earth:Boulder|Boulder]]
|-
| −6 to −8 || 64–256&nbsp;mm || 2.5–10.1 in || [[Earth:Cobble (geology)|Cobble]]
|-
| −5 to −6 || 32–64&nbsp;mm || 1.26–2.5 in || Very coarse [[Earth:Gravel|gravel]] || [[Earth:Pebble|Pebble]]
|-
| −4 to −5 || 16–32&nbsp;mm || 0.63–1.26 in || Coarse gravel || Pebble
|-
| −3 to −4 || 8–16&nbsp;mm || 0.31–0.63 in || Medium gravel || Pebble
|-
| −2 to −3 || 4–8&nbsp;mm || 0.157–0.31 in || Fine gravel || Pebble
|-
| −1 to −2 || 2–4&nbsp;mm || 0.079–0.157 in || Very fine gravel || [[Earth:Granule (geology)|Granule]]
|-
| 0 to −1 || 1–2&nbsp;mm || 0.039–0.079 in || Very coarse sand
|-
| 1 to 0 || 0.5–1&nbsp;mm || 0.020–0.039 in || Coarse sand
|-
| 2 to 1 || 0.25–0.5&nbsp;mm || 0.010–0.020 in || Medium sand
|-
| 3 to 2 || 125–250 [[Micrometre|μm]] || 0.0049–0.010 in || Fine sand
|-
| 4 to 3 || 62.5–125&nbsp;μm || 0.0025–0.0049 in || Very fine sand
|-
| 8 to 4 || 3.9–62.5&nbsp;μm || 0.00015–0.0025 in || [[Earth:Silt|Silt]] || [[Earth:Mud|Mud]]
|-
| > 8 || < 3.9&nbsp;μm || < 0.00015 in || [[Earth:Clay|Clay]] || Mud
|-
| > 10 || < 1&nbsp;μm || < 0.000039 in || [[Physics:Colloid|Colloid]] || Mud
|}

===Shape===
[[File:Rounding & sphericity EN.svg|thumb|300px|Schematic representation of difference in grain shape. Two parameters are shown: sphericity (vertical) and [[Earth:Roundness (geology)|rounding]] (horizontal).]]
The shape of particles can be defined in terms of three parameters. The ''form'' is the overall shape of the particle, with common descriptions being spherical, platy, or rodlike. The ''roundness'' is a measure of how sharp grain corners are. This varies from well-rounded grains with smooth corners and edges to poorly rounded grains with sharp corners and edges. Finally, ''surface texture'' describes small-scale features such as scratches, pits, or ridges on the surface of the grain.<ref>{{cite book |last1=Boggs |first1=Sam |title=Principles of sedimentology and stratigraphy |date=2006 |publisher=Pearson Prentice Hall |location=Upper Saddle River, N.J. |isbn=0131547283 |edition=4th |page=65}}</ref>

====Form====
Form (also called ''sphericity'') is determined by measuring the size of the particle on its major axes. William C. Krumbein proposed formulas for converting these numbers to a single measure of form,<ref>{{cite journal |last1=Krumbein |first1=William C. |title=Measurement and Geological Significance of Shape and Roundness of Sedimentary Particles |journal=SEPM Journal of Sedimentary Research |date=1941 |volume=11 |pages=64–72 |doi=10.1306/D42690F3-2B26-11D7-8648000102C1865D}}</ref> such as

:<math>\psi_l = \sqrt[3]{\frac{D_S D_I}{D_L^2}}</math>

where <math>D_L</math>, <math>D_I</math>, and <math>D_S</math> are the long, intermediate, and short axis lengths of the particle.{{sfn|Boggs|2006|p=582}} The form <math>\psi_l</math> varies from 1 for a perfectly spherical particle to very small values for a platelike or rodlike particle. 

An alternate measure was proposed by Sneed and Folk:<ref>{{cite journal |last1=Sneed |first1=Edmund D. |last2=Folk |first2=Robert L. |title=Pebbles in the Lower Colorado River, Texas a Study in Particle Morphogenesis |journal=The Journal of Geology |date=March 1958 |volume=66 |issue=2 |pages=114–150 |doi=10.1086/626490|bibcode=1958JG.....66..114S |s2cid=129658242 }}</ref>

:<math>\psi_p = \sqrt[3]{\frac{D_S^2}{D_L D_I}}</math>

which, again, varies from 0 to 1 with increasing sphericity.

====Roundness====
{{Main|Earth:Roundness (geology)}}
[[File:Rounding.gif|thumb|Comparison chart for evaluating roundness of sediment grains]]
Roundness describes how sharp the edges and corners of particle are. Complex mathematical formulas have been devised for its precise measurement, but these are difficult to apply, and most geologists estimate roundness from comparison charts. Common descriptive terms range from very angular to angular to subangular to subrounded to rounded to very rounded, with increasing degree of roundness.{{sfn|Boggs|2006|pp=66-67}}

====Surface texture====
Surface texture describes the small-scale features of a grain, such as pits, fractures, ridges, and scratches. These are most commonly evaluated on [[Chemistry:Quartz|quartz]] grains, because these retain their surface markings for long periods of time. Surface texture varies from polished to frosted, and can reveal the history of transport of the grain; for example, frosted grains are particularly characteristic of [[Earth:Aeolian processes|aeolian]] sediments, transported by wind. Evaluation of these features often requires the use of a [[Physics:Scanning electron microscope|scanning electron microscope]].{{sfn|Boggs|2006|pp=68-70}}

===Composition===
Composition of sediment can be measured in terms of:
* Parent [[Earth:Rock (geology)|rock]] [[Earth:Lithology|lithology]]
* [[Earth:Mineral|Mineral]] composition
* Chemical make-up

This leads to an ambiguity in which [[Earth:Clay|clay]] can be used as both a size-range and a composition (see [[Chemistry:Clay mineral|clay mineral]]s).

== Sediment transport ==
[[File:StoneFormationInWater.jpg|thumb|Sediment builds up on human-made breakwaters because they reduce the speed of water flow, so the stream cannot carry as much sediment load.]]
[[File:Glacial Transportation and Deposition.jpg|thumb|Glacial transport of boulders. These boulders will be deposited as the glacier retreats.]]

{{main|Physics:Sediment transport}}

Sediment is transported based on the strength of the flow that carries it and its own size, volume, density, and shape. Stronger flows will increase the lift and drag on the particle, causing it to rise, while larger or denser particles will be more likely to fall through the flow.

=== Fluvial processes ===
{{excerpt|Fluvial sediment processes}}

===Aeolian processes: wind===
{{main|Earth:Aeolian processes}}
Wind results in the transportation of fine sediment and the formation of sand dune fields and soils from airborne dust.

===Glacial processes===
[[File:GLMsed.jpg|thumb|Glacial sediments from Montana]]
Glaciers carry a wide range of sediment sizes, and deposit it in [[Earth:Moraine|moraine]]s.

===Mass balance===
{{main|Exner equation}}

The overall balance between sediment in transport and sediment being deposited on the bed is given by the [[Exner equation]]. This expression states that the rate of increase in bed elevation due to deposition is proportional to the amount of sediment that falls out of the flow. This equation is important in that changes in the power of the flow change the ability of the flow to carry sediment, and this is reflected in the patterns of erosion and deposition observed throughout a stream. This can be localized, and simply due to small obstacles; examples are scour holes behind boulders, where flow accelerates, and deposition on the inside of [[Earth:Meander|meander]] bends. Erosion and deposition can also be regional; erosion can occur due to [[Biology:Dam removal|dam removal]] and [[Earth:Base level|base level]] fall. Deposition can occur due to dam emplacement that causes the river to pool and deposit its entire load, or due to base level rise.

== Shores and shallow seas ==

Seas, oceans, and lakes accumulate sediment over time. The sediment can consist of ''terrigenous'' material, which originates on land, but may be deposited in either terrestrial, marine, or lacustrine (lake) environments, or of sediments (often biological) originating in the body of water. Terrigenous material is often supplied by nearby rivers and streams or reworked [[Earth:Marine sediment|marine sediment]] (e.g. sand). In the mid-ocean, the exoskeletons of dead organisms are primarily responsible for sediment accumulation.

Deposited sediments are the source of [[Earth:Sedimentary rock|sedimentary rock]]s, which can contain [[Biology:Fossil|fossil]]s of the inhabitants of the body of water that were, upon death, covered by accumulating sediment. Lake bed sediments that have not solidified into rock can be used to determine past [[Earth:Climate|climatic]] conditions.

=== Key marine depositional environments ===
[[File:EolianiteLongIsland.JPG|thumb|right|[[Earth:Holocene|Holocene]] eolianite and a carbonate beach on Long Island, Bahamas]]
The major areas for deposition of sediments in the marine environment include:
* Littoral sands (e.g. beach sands, runoff river sands, coastal bars and spits, largely clastic with little faunal content)
* The continental shelf ([[Earth:Silt|silt]]y [[Earth:Clay|clay]]s, increasing marine faunal content).
* The shelf margin (low terrigenous supply, mostly [[Chemistry:Calcite|calcareous]] faunal skeletons)
* The shelf slope (much more fine-grained silts and clays)
* Beds of estuaries with the resultant deposits called "[[Earth:Bay mud|bay mud]]".

One other depositional environment which is a mixture of fluvial and marine is the [[Earth:Turbidite|turbidite]] system, which is a major source of sediment to the deep [[Earth:Sedimentary basin|sedimentary]] and [[Earth:Abyssal plain|abyssal basins]] as well as the deep [[Earth:Oceanic trench|oceanic trench]]es.

Any depression in a marine environment where sediments accumulate over time is known as a [[Earth:Sediment trap (geology)|sediment trap]].

The null point theory explains how sediment deposition undergoes a hydrodynamic sorting process within the marine environment leading to a seaward fining of sediment grain size.

==Environmental issues==

===Erosion and agricultural sediment delivery to rivers===
One cause of high sediment loads is slash and burn and shifting cultivation of tropical forests. When the ground surface is stripped of vegetation and then seared of all living organisms, the upper soils are vulnerable to both wind and water erosion. In a number of regions of the earth, entire sectors of a country have become erodible. For example, on the {{wipe|Madagascar}} high central [[Earth:Plateau|plateau]], which constitutes approximately ten percent of that country's land area, most of the land area is devegetated, and gullies have eroded into the underlying soil to form distinctive gulleys called ''[[Earth:Lavaka|lavaka]]s''. These are typically {{convert|40|m||sp=us}} wide, {{convert|80|m||sp=us}} long and {{convert|15|m||sp=us}} deep.<ref>{{cite web |last1=Sawe |first1=Benjamin Elisha |title=Erosion Landforms: What Is A Lavaka? |date=25 April 2017 |url=https://www.worldatlas.com/articles/erosion-landforms-what-is-a-lavaka.html |publisher=WorldAtlas |access-date=24 September 2021}}</ref> Some areas have as many as 150 lavakas/square kilometer,<ref>{{cite journal |last1=Voarintsoa |first1=N. R. G. |last2=Cox |first2=R. |last3=Razanatseheno |first3=M.O.M.|last4=Rakotondrazafy |first4=A.F.M. |title=Relation Between Bedrock Geology, Topography and Lavaka Distribution in Madagascar |journal=South African Journal of Geology |date=1 June 2012 |volume=115 |issue=2 |pages=225–250 |doi=10.2113/gssajg.115.225|bibcode=2012SAJG..115..225V }}</ref> and lavakas may account for 84% of all sediments carried off by rivers.<ref>{{cite journal |last1=Cox |first1=Rónadh |last2=Bierman |first2=Paul |last3=Jungers |first3=Matthew C.|last4=Rakotondrazafy |first4=A.F. Michel|title=Erosion Rates and Sediment Sources in Madagascar Inferred from 10 Be Analysis of Lavaka, Slope, and River Sediment |journal=The Journal of Geology |date=July 2009 |volume=117 |issue=4 |pages=363–376 |doi=10.1086/598945|bibcode=2009JG....117..363C |s2cid=55543845 }}</ref> This [[Earth:Siltation|siltation]] results in discoloration of rivers to a dark red brown color and leads to fish kills.

Erosion is also an issue in areas of modern farming, where the removal of native vegetation for the cultivation and harvesting of a single type of crop has left the soil unsupported.<ref>{{cite journal |last1=Ketcheson |first1=J. W. |title=Long-Range Effects of Intensive Cultivation and Monoculture on the Quality of Southern Ontario Soils |journal=Canadian Journal of Soil Science |date=1 March 1980 |volume=60 |issue=3 |pages=403–410 |doi=10.4141/cjss80-045}}</ref> Many of these regions are near rivers and drainages. Loss of soil due to erosion removes useful farmland, adds to sediment loads, and can help transport anthropogenic fertilizers into the river system, which leads to [[Earth:Eutrophication|eutrophication]].<ref>{{cite book |last1=Ohlsson |first1=Thomas |editor1-last=Motarjemi |editor1-first=Yasmine |editor2-last=Lelieveld |editor2-first=Hubb |title=Food safety management: a practical guide for the food industry |date=2014 |publisher=Elsevier |isbn=9780128056820 |chapter-url=https://books.google.com/books?id=sCR3DAAAQBAJ&dq=%22Monoculture+agriculture%22+%22eutrophication%22&pg=PP6 |access-date=24 September 2021 |chapter=Sustainability and Food Production}}</ref>

The Sediment Delivery Ratio (SDR) is fraction of gross erosion (interill, rill, gully and stream erosion) that is expected to be delivered to the outlet of the river.<ref>{{Cite journal|last1=Fernandez|first1=C.|last2=Wu|first2=J. Q.|last3=McCool|first3=D. K.|last4=Stöckle|first4=C. O.|date=2003-05-01|title=Estimating water erosion and sediment yield with GIS, RUSLE, and SEDD|url=http://www.jswconline.org/content/58/3/128|journal=Journal of Soil and Water Conservation|language=en|volume=58|issue=3|pages=128–136|issn=0022-4561}}</ref> The sediment transfer and deposition can be modelled with sediment distribution models such as WaTEM/SEDEM.<ref>{{Cite journal|last1=Van Rompaey|first1=Anton J. J.|last2=Verstraeten|first2=Gert|last3=Van Oost|first3=Kristof|last4=Govers|first4=Gerard|last5=Poesen|first5=Jean|date=2001-10-01|title=Modelling mean annual sediment yield using a distributed approach|journal=Earth Surface Processes and Landforms|language=en|volume=26|issue=11|pages=1221–1236|doi=10.1002/esp.275|issn=1096-9837|url=https://lirias.kuleuven.be/handle/123456789/76728|bibcode=2001ESPL...26.1221V|s2cid=128689971}}</ref> In Europe, according to WaTEM/SEDEM model estimates the Sediment Delivery Ratio is about 15%.<ref>{{Cite journal|date=2018-02-01|title=A step towards a holistic assessment of soil degradation in Europe: Coupling on-site erosion with sediment transfer and carbon fluxes|journal=Environmental Research|language=en|volume=161|pages=291–298|doi=10.1016/j.envres.2017.11.009|pmid=29175727|pmc=5773246|issn=0013-9351|last1=Borrelli|first1=P.|last2=Van Oost|first2=K.|last3=Meusburger|first3=K.|last4=Alewell|first4=C.|last5=Lugato|first5=E.|last6=Panagos|first6=P.|bibcode=2018ER....161..291B}}</ref>

===Coastal development and sedimentation near coral reefs===

Watershed development near coral reefs is a primary cause of sediment-related coral stress. The stripping of natural vegetation in the watershed for development exposes soil to increased wind and rainfall, and as a result, can cause exposed sediment to become more susceptible to erosion and delivery to the marine environment during rainfall events. Sediment can negatively affect corals in many ways, such as by physically smothering them, abrading their surfaces, causing corals to expend energy during sediment removal, and causing algal blooms that can ultimately lead to less space on the seafloor where juvenile corals (polyps) can settle.

When sediments are introduced into the coastal regions of the ocean, the proportion of land, marine and organic-derived sediment that characterizes the seafloor near sources of sediment output is altered. In addition, because the source of sediment (i.e. land, ocean, or organically) is often correlated with how coarse or fine sediment grain sizes that characterize an area are on average, grain size distribution of sediment will shift according to relative input of land (typically fine), marine (typically coarse), and organically-derived (variable with age) sediment.  These alterations in marine sediment characterize the amount of sediment that is suspended in the water column at any given time and sediment-related coral stress.
<ref>{{cite journal |last1=Risk |first1=Michael J |title=Assessing the effects of sediments and nutrients on coral reefs |journal=Current Opinion in Environmental Sustainability |date=April 2014 |volume=7 |pages=108–117 |doi=10.1016/j.cosust.2014.01.003|bibcode=2014COES....7..108R }}</ref>

===Biological considerations===
In July 2020, [[Biology:Marine biology|marine biologists]] reported that [[Biology:Aerobic organism|aerobic]] [[Biology:Microorganism|microorganism]]s (mainly), in "[[Biology:Suspended animation|quasi-suspended animation]]", were found in organically-poor sediments, up to 101.5 million years old, 250 feet below the [[Earth:Seabed|seafloor]] in the South Pacific Gyre (SPG) ("the deadest spot in the ocean"), and could be the [[Biology:List of longest-living organisms|longest-living life forms]] ever found.<ref name="NYT-2200728">{{cite news |last=Wu |first=Katherine J. |title=These Microbes May Have Survived 100 Million Years Beneath the Seafloor - Rescued from their cold, cramped and nutrient-poor homes, the bacteria awoke in the lab and grew. |work=The New York Times |url=https://www.nytimes.com/2020/07/28/science/microbes-100-million-years-old.html |date=28 July 2020 |access-date=31 July 2020 }}</ref><ref name="NC-20200728">{{cite journal |author=Morono, Yuki |display-authors=et al. |title=Aerobic microbial life persists in oxic marine sediment as old as 101.5 million years |date=28 July 2020 |journal=Nature Communications |volume=11 |number=3626 |page=3626 |doi=10.1038/s41467-020-17330-1 |pmid=32724059 |pmc=7387439 |bibcode=2020NatCo..11.3626M }}</ref>

==See also==
{{div col}}
* {{annotated link|Earth:Bar (river morphology)}}
* {{annotated link|Earth:Beach cusps}}
* {{annotated link|Earth:Biorhexistasy}}
* {{annotated link|Earth:Bioswale}}
* {{annotated link|Chemistry:Decantation}}
* {{annotated link|Earth:Deposition (geology)}}
* {{annotated link|Earth:Depositional environment}}
* {{annotated link|Earth:Erosion}}
* {{annotated link|Exner equation}}
* {{annotated link|Earth:Grain size|aka=particle size}}
* {{annotated link|Earth:Sedimentology}}
* {{annotated link|Earth:Sediment trap (geology)|Sediment trap}}
* {{annotated link|Chemistry:Settling}}
* {{annotated link|Earth:Surface runoff}}
{{div col end}}

==References==
{{reflist}}

==Further reading==
*{{Citation |first1=Donald R. |last1=Prothero |first2=Fred |last2=Schwab |title=Sedimentary Geology: An Introduction to Sedimentary Rocks and Stratigraphy |publisher=W. H. Freeman |year=1996 |isbn=978-0-7167-2726-2 }}
*{{Citation |first=Raymond |last=Siever |title=Sand |publisher=Scientific American Library |location=New York |year=1988 |isbn=978-0-7167-5021-5 |url-access=registration |url=https://archive.org/details/sand00siev }}
*{{Citation |first=Gary |last=Nichols |title=Sedimentology & Stratigraphy |publisher=Wiley-Blackwell |location=Malden, MA |year=1999 |isbn=978-0-632-03578-6 }}
*{{Citation |first=H. G. |last=Reading |title=Sedimentary Environments: Processes, Facies and Stratigraphy |publisher=Blackwell Science |location=Cambridge, Massachusetts |year=1978 |isbn=978-0-632-03627-1 }}


[[Category:Sediments| ]]
[[Category:Sedimentology]]
[[Category:Environmental soil science]]
[[Category:Petrology]]

{{Sourceattribution|Sediment}}