Alluvial fan

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Alluvial fan in the French Pyrenees Alluvial fan 01.JPG
Alluvial fan in the French Pyrenees

An alluvial fan is an accumulation of sediments that fans outwards from a concentrated source of sediments, such as a narrow canyon emerging from an escarpment. They are characteristic of mountainous terrain in arid to semiarid climates, but are also found in more humid environments subject to intense rainfall and in areas of modern glaciation. They range in area from less than 1 square kilometer (0.4 sq mi) to almost 20,000 square kilometers (7,700 sq mi).

Contents

Alluvial fans typically form where flow emerges from a confined channel and is free to spread out and infiltrate the surface. This reduces the carrying capacity of the flow and results in deposition of sediments. The flow can take the form of infrequent debris flows or one or more ephemeral or perennial streams.

Alluvial fans are common in the geologic record, such as in the Triassic basins of eastern North America and the New Red Sandstone of south Devon. Such fan deposits likely contain the largest accumulations of gravel in the geologic record. Alluvial fans have also been found on Mars and Titan, showing that fluvial processes have occurred on other worlds.

Some of the largest alluvial fans are found along the Himalaya mountain front on the Indo-Gangetic plain. A shift of the feeder channel (a nodal avulsion) can lead to catastrophic flooding, as occurred on the Kosi River fan in 2008.

Description

Alluvial fan in Death Valley Alluvial Fan.jpg
Alluvial fan in Death Valley

An alluvial fan is an accumulation of sediments that fans out from a concentrated source of sediments, such as a narrow canyon emerging from an escarpment. This accumulation is shaped like a section of a shallow cone, [1] with its apex at the source of sediments. [2]

Alluvial fans vary greatly in size, from only a few meters across at the base to as much as 150 kilometers across, with a slope of 1.5 to 25 degrees. [1] Some giant alluvial fans have areas of almost 20,000 square kilometres (7,700 sq mi). [3] The slope measured from the apex is generally concave, with the steepest slope near the apex (the proximal fan [4] or fanhead [5] ) and becoming less steep further out (the medial fan or midfan) and shallowing at the edges of the fan (the distal fan or outer fan). Sieve deposits, which are lobes of coarse gravel, may be present on the proximal fan. The sediments in an alluvial fan are usually coarse and poorly sorted, with the coarsest sediments found on the proximal fan. [6] [7]

Large alluvial fan in Death Valley showing a "toe-trimmed" profile Gigantic Alluvial Fan Being Uplift by New Fault.jpg
Large alluvial fan in Death Valley showing a "toe-trimmed" profile

When there is enough space in the alluvial plain for all of the sediment deposits to fan out without contacting other valley walls or rivers, an unconfined alluvial fan develops. Unconfined alluvial fans allow sediments to naturally fan out, and the shape of the fan is not influenced by other topological features. When the alluvial plain is more restricted, so that the fan comes into contact with topographic barriers, a confined fan is formed. [8]

Wave or channel erosion of the edge of the fan (lateral erosion) sometimes produces a "toe-trimmed" fan, in which the edge of the fan is marked by a small escarpment. [9] Toe-trimmed fans may record climate changes or tectonic processes, and the process of lateral erosion may enhance the aquifer or petroleum reservoir potential of the fan. [10] Toe-trimmed fans on the planet Mars provide evidence of past river systems. [11]

When numerous rivers and streams exit a mountain front onto a plain, the fans can combine to form a continuous apron. This is referred to as a bajada or piedmont alluvial plain. [12] [13]

Topographic map of an alluvial fan near Rawa Danau Caldera, West Java, Indonesia Alluvial Fan of Rawa Danau.png
Topographic map of an alluvial fan near Rawa Danau Caldera, West Java, Indonesia

Formation

Alluvial fans usually form where a confined feeder channel exits a mountain front [14] [15] or a glacier margin. [6] As the flow exits the feeder channel onto the fan surface, it is able to spread out into wide, shallow channels or to infiltrate the surface. This reduces the carrying power of the flow and results in deposition of sediments. [15]

Alluvial fan in the Taklamakan Desert in Xinjiang showing active left and inactive right sectors Alluvial fan, Taklimakan Desert, XinJiang Province, China, NASA, ASTER.jpg
Alluvial fan in the Taklamakan Desert in Xinjiang showing active left and inactive right sectors

Flow in the proximal fan, where the slope is steepest, is usually confined to a single channel [6] (a fanhead trench [3] ), which may be up to 30 meters (100 ft) deep. [6] This channel is subject to blockage by accumulated sediments or debris flows, which causes flow to periodically break out of its old channel (nodal avulsion) and shift to a part of the fan with a steeper gradient, where deposition resumes. [15] As a result, normally only part of the fan is active at any particular time, and the bypassed areas may undergo soil formation or erosion. [6]

Alluvial fans can be dominated by debris flows (debris flow fans) or stream flow (fluvial fans). [4] [16] [17] Which kind of fan is formed is controlled by climate, tectonics, and the type of bedrock in the area feeding the flow onto the fan. [18]

Debris flow

Debris flow fans receive most of their sediments in the form of debris flows. Debris flows are slurry-like mixtures of water and particles of all sizes, from clay to boulders, that resemble wet concrete. They are characterized by having a yield strength, meaning that they are highly viscous at low flow velocities but become less viscous as the flow velocity increases. This means that a debris flow can come to a halt while still on moderately tilted ground. The flow then becomes consolidated under its own weight. [19]

Debris flow fans occur in all climates but are more common where the source rock is mudstone or matrix-rich saprolite rather than coarser, more permeable regolith. The abundance of fine-grained sediments encourages the initial hillslope failure and subsequent cohesive flow of debris. [20] Saturation of clay-rich colluvium by locally intense thunderstorms initiates slope failure. The resulting debris flow travels down the feeder channel and onto the surface of the fan. [21]

Debris flow fans have a network of mostly inactive distributary channels in the upper fan that gives way to mid- to lower-level lobes. The channels tend to be filled by subsequent cohesive debris flows. Usually only one lobe is active at a time, and inactive lobes may develop desert varnish or develop a soil profile from eolian dust deposition, on time scales of 1,000 to 10,000 years. [22] Because of their high viscosity, debris flows tend to be confined to the proximal and medial fan even in a debris-flow-dominated alluvial fan, and streamfloods dominate the distal fan. [23] However, some debris-flow-dominated fans in arid climates consist almost entirely of debris flows and lag gravels from eolian winnowing of debris flows, with no evidence of sheetflood or sieve deposits. [24] Debris-flow-dominated fans tend to be steep and poorly vegetated. [25]

Fluvial

Fluvial fans (streamflow-dominated fans) receive most of their sediments in the form of stream flow rather than debris flows. They are less sharply distinguished from ordinary fluvial deposits than are debris flow fans. [14]

Fluvial fans occur where there is perennial, seasonal, or ephemeral stream flow that feeds a system of distributary channels on the fan. In arid or semiarid climates, deposition is dominated by infrequent but intense rainfall that produces flash floods in the feeder channel. [23] This results in sheetfloods on the alluvial fan, where sediment-laden water leaves its channel confines and spreads across the fan surface. These may include hyperconcentrated flows containing 20% to 45% sediments, which are intermediate between sheetfloods having 20% or less of sediments and debris flows with more than 45% sediments. [25] As the flood recedes, it often leaves a lag of gravel deposits that have the appearance of a network of braided streams. [23]

Where the flow is more continuous, as with spring snow melt, incised-channel flow in channels 1–4 meters (3–10 ft) high takes place in a network of braided streams. [25] Such alluvial fans tend to have a shallower slope but can become enormous. [23] The Kosi and other fans along the Himalaya mountain front in the Indo-Gangetic plain are examples of gigantic stream-flow-dominated alluvial fans, sometimes described as megafans. [26] Here, continued movement on the Main Boundary Thrust over the last ten million years has focused the drainage of 750 kilometres (470 mi) of mountain frontage into just three enormous fans. [3]

Geologic record

Pebble bed in the New Red Sandstone Pebble bed in the New Red Sandstone - geograph.org.uk - 2188766.jpg
Pebble bed in the New Red Sandstone

Alluvial fans are common in the geologic record, but may have been particularly important before the evolution of land plants in the mid-Paleozoic. [27] They are characteristic of fault-bounded basins and can be 5,000 meters (16,000 ft) or thicker due to tectonic subsidence of the basin and uplift of the mountain front. Most are red from hematite produced by diagenetic alteration of iron-rich minerals in a shallow, oxidizing environment. Examples of paleofans include the Triassic basins of eastern North America and the New Red Sandstone of south Devon, [23] the Devonian Hornelen Basin of Norway, and the Devonian-Carboniferous in the Gaspé Peninsula of Canada. [27] Such fan deposit likely contain the largest accumulations of gravel in the geologic record. [28]

Depositional facies

Several kinds of sediment deposits ( facies ) are found in alluvial fans.

Alluvial fans are characterized by coarse sedimentation, though the sediments making up the fan become less coarse further from the apex. Gravels show well-developed imbrication with the pebbles dipping towards the apex. [23] Fan deposits typically show well-developed reverse grading caused by outbuilding of the fan: Finer sediments are deposited at the edge of the fan, but as the fan continues to grow, increasingly coarse sediments are deposited on top of the earlier, less coarse sediments. However, a few fans show normal grading indicating inactivity or even fan retreat, so that increasingly fine sediments are deposited on earlier coarser sediments. Normal or reverse grading sequences can be hundreds to thousands of meters in thickness. [27] Depositional facies that have been reported for alluvial fans include debris flows, sheet floods and upper regime stream floods, sieve deposits, and braided stream flows, each leaving their own characteristic sediment deposits that can be identified by geologists. [23] [29]

Debris flow deposits are common in the proximal and medial fan. [23] These deposits lack sedimentary structure, other than occasional reverse-graded bedding towards the base, and they are poorly sorted. [30] The proximal fan may also include gravel lobes that have been interpreted as sieve deposits, where runoff rapidly infiltrates and leaves behind only the coarse material. However, the gravel lobes have also been interpreted as debris flow deposits. [30] Conglomerate originating as debris flows on alluvial fans is described as fanglomerate. [31]

Stream flow deposits tend to be sheetlike, better sorted than debris flow deposits, and sometimes show well-developed sedimentary structures such as cross-bedding. These are more prevalent in the medial and distal fan. [25] In the distal fan, where channels are very shallow and braided, stream flow deposits consist of sandy interbeds with planar and trough slanted stratification. [32] The medial fan of a streamflow-dominated alluvial fan shows nearly the same depositional facies as ordinary fluvial environments, so that identification of ancient alluvial fans must be based on radial paleomorphology in a piedmont setting. [33]

Occurrences

Alluvial fans are characteristic of mountainous terrain in arid to semiarid climates, [34] [6] but are also found in more humid environments subject to intense rainfall [7] and in areas of modern glaciation. [6] They have also been found on other bodies of the Solar System. [35] [36]

Terrestrial

Alluvial fans are built in response to erosion induced by tectonic uplift. [37] The upwards coarsening of the beds making up the fan reflects cycles of erosion in the highlands that feed sediments to the fan. However, climate and changes in base level may be as important as tectonic uplift. For example, alluvial fans in the Himalayas show older fans entrenched and overlain by younger fans. The younger fans, in turn, are cut by deep incised valleys showing two terrace levels. Dating via optically stimulated luminescence suggests a hiatus of 70,000 to 80,000 years between the old and new fans, with evidence of tectonic tilting at 45,000 years ago and an end to fan deposition 20,000 years ago. Both the hiatus and the more recent end to fan deposition are thought to be connected to periods of enhanced southwest monsoon precipitation. Climate has also influenced fan formation in Death Valley, California, US, where dating of beds suggests that peaks of fan deposition during the last 25,000 years occurred during times of rapid climate change, both from wet to dry and from dry to wet. [38]

Alluvial fans are often found in desert areas, which are subjected to periodic flash floods from nearby thunderstorms in local hills. The typical watercourse in an arid climate has a large, funnel-shaped basin at the top, leading to a narrow defile, which opens out into an alluvial fan at the bottom. Multiple braided streams are usually present and active during water flows. [34] Phreatophytes (plants with long tap roots capable of reaching a deep water table) are sometimes found in sinuous lines radiating from arid climate fan toes. These fan-toe phreatophyte strips trace buried channels of coarse sediments from the fan that have interfingered with impermeable playa sediments. [39]

Alluvial fans also develop in wetter climates when high-relief terrain is located adjacent to low-relief terrain. [37] In Nepal, the Koshi River has built a megafan covering some 15,000 km2 (5,800 sq mi) below its exit from Himalayan foothills onto the nearly level plains where the river traverses into India before joining the Ganges. Along the upper Koshi tributaries, tectonic forces elevate the Himalayas several millimeters annually. Uplift is approximately in equilibrium with erosion, so the river annually carries some 100 million cubic meters (3.5×10^9 cu ft) of sediment as it exits the mountains. Deposition of this magnitude over millions of years is more than sufficient to account for the megafan. [40]

In North America, streams flowing into California's Central Valley have deposited smaller but still extensive alluvial fans, such as that of the Kings River flowing out of the Sierra Nevada. [41] Like the Himalayan megafans, these are streamflow-dominated fans. [42]

Extraterrestrial

Mars

Large alluvial fan at the base of the rim of Gale crater, Mars PIA22210-Mars-CuriosityRover-GaleCrater-20171025-annotated-cropped-alluvial-fan.jpg
Large alluvial fan at the base of the rim of Gale crater, Mars

Alluvial fans are also found on Mars. Unlike alluvial fans on Earth, those on Mars are rarely associated with tectonic processes, but are much more common on crater rims. [43] [44] The crater rim alluvial fans appear to have been deposited by sheetflow rather than debris flows. [45]

Three alluvial fans have been found in Saheki Crater. These fans confirmed past fluvial flow on the planet and further supported the theory that liquid water was once present in some form on the Martian surface. [46] In addition, observations of fans in Gale crater made by satellites from orbit have now been confirmed by the discovery of fluvial sediments by the Curiosity rover. [47] Alluvial fans in Holden crater have toe-trimmed profiles attributed to fluvial erosion. [11]

The few alluvial fans associated with tectonic processes include those at Coprates Chasma and Juventae Chasma, which are part of the Valles Marineris canyon system. These provide evidence of the existence and nature of faulting in this region of Mars. [48]

Titan

Alluvial fans have been observed by the Cassini-Huygens mission on Titan using the Cassini orbiter's synthetic aperture radar instrument. These fans are more common in the drier mid-latitudes at the end of methane/ethane rivers where it is thought that frequent wetting and drying occur due to precipitation, much like arid fans on Earth. Radar imaging suggests that fan material is most likely composed of round grains of water ice or solid organic compounds about two centimeters in diameter. [49]

Impact on humans

Alluvial fans are the most important groundwater reservoirs in many regions. Many urban, industrial, and agricultural areas are located on alluvial fans, [50] including the conurbations of Los Angeles, California; Salt Lake City, Utah; and Denver, Colorado, in the western United States, and in many other parts of the world. [51] However, flooding on alluvial fans poses unique problems for disaster prevention and preparation. [52]

Aquifers

The beds of coarse sediments associated with alluvial fans form aquifers that are the most important groundwater reservoirs in many regions. [50] These include both arid regions, such as Egypt [53] or Iraq, [54] and humid regions, such as central Europe [55] or Taiwan. [56]

Flood hazards

Alluvial fans are subject to infrequent but often very damaging flooding, whose unusual characteristics distinguish alluvial fan floods from ordinary riverbank flooding. These include great uncertainty in the likely flood path, the likelihood of abrupt deposition and erosion of sediments carried by the flood from upstream sources, and a combination of the availability of sediments and of the slope and topography of the fan that creates extraordinary hazards. These hazards cannot reliably be mitigated by elevation on fill (raising existing buildings up to a meter (three feet) and building new foundations beneath them [57] ). At a minimum, major structural flood control measures are required to mitigate risk, and in some cases, the only alternative is to restrict development on the fan surface. Such measures can be politically controversial, particularly since the hazard is not obvious to property owners. [58] In the United States, areas at risk of alluvial fan flooding are marked as Zone AO on flood insurance rate maps. [59]

Alluvial fan flooding commonly takes the form of short (several hours) but energetic flash floods that occur with little or no warning. They typically result from heavy and prolonged rainfall, and are characterized by high velocities and capacity for sediment transport. Flows cover the range from floods through hyperconcentrated flows to debris flows, depending on the volume of sediments in the flow. Debris flows resemble freshly poured concrete, consisting mostly of coarse debris. Hyperconcentrated flows are intermediate between floods and debris flows, with a water content between 40 and 80 weight percent. Floods may transition to hyperconcentrated flows as they entrain sediments, while debris flows may become hyperconcentrated flows if they are diluted by water. [60] Because flooding on alluvial fans carries large quantities of sediment, channels can rapidly become blocked, creating great uncertainty about flow paths that magnifies the dangers. [58]

Alluvial fan flooding in the Apennine Mountains of Italy have resulted in repeated loss of life. A flood on 1 October 1581 at Piedimonte Matese resulted in the loss of 400 lives. Loss of life from alluvial fan floods continued into the 19th century, and the hazard of alluvial fan flooding remains a concern in Italy. [61]

On January 1, 1934, record rainfall in a recently burned area of the San Gabriel Mountains, California, caused severe flooding of the alluvial fan on which the towns of Montrose and Glendale were built. The floods caused significant loss of life and property. [62]

The Koshi River in India has built up a megafan where it exits the Himalayas onto the Ganges plain. The river has a history of frequently and capriciously changing its course, so that it has been called the Sorrow of Bihar for contributing disproportionately to India's death tolls in flooding. These exceed those of all countries except Bangladesh. [63] Over the last few hundred years, the river had generally shifted westward across its fan, and by 2008, the main river channel was located on the extreme western part of the megafan. In August 2008, high monsoon flows breached the embankment of the Koshi River. This diverted most of the river into an unprotected ancient channel and flooded the central part of the megafan. This was an area with a high population density that had been stable for over 200 years. [64] Over a million people were rendered homeless, about a thousand lost their lives and thousands of hectares of crops were destroyed. [65] [66] [67]

Petroleum reservoirs

Buried alluvial fans are sometimes found at the margins of petroleum basins. Debris flow fans make poor petroleum reservoirs, but fluvial fans are potentially significant reservoirs. Though fluvial fans are typically of poorer quality than reservoirs closer to the basin center, due to their complex structure, the episodic flooding channels of the fans are potentially lucrative targets for petroleum exploration. [68] Alluvial fans that experience toe-trimming (lateral erosion) by an axial river (a river running the length of an escarpment-bounded basin) may have increased potential as reservoirs. The river deposits relatively porous, permeable axial river sediments that alternate with fan sediment beds. [69]

See also

Notes

  1. 1 2 Boggs 2006, p. 246.
  2. ↑ Leeder 2011, pp. 282–285.
  3. 1 2 3 Leeder 2011, p. 285.
  4. 1 2 Boggs 2006, p. 247.
  5. ↑ Blatt, Middleton & Murray 1980, p. 629.
  6. 1 2 3 4 5 6 7 Blatt, Middleton & Murray 1980, pp. 629–632.
  7. 1 2 Boggs 2006, pp. 246–250.
  8. ↑ Nemec & Steel 1988, p. 6.
  9. ↑ Leeder 2011, p. 282.
  10. ↑ Leeder & Mack 2001, pp. 885, 889–891.
  11. 1 2 Moore & Howard 2005, 2.2 [12].
  12. ↑ Thornbury 1969, p. 173.
  13. ↑ Jackson 1997, "piedmont alluvial plain".
  14. 1 2 Boggs 2006, pp. 246–248.
  15. 1 2 3 Leeder 2011, pp. 285–289.
  16. ↑ Leeder 2011, pp. 287–289.
  17. ↑ Gao et al. 2021, p. 2.
  18. ↑ Nichols & Thompson 2005, [Abstract].
  19. ↑ Leeder 2011, p. 177.
  20. ↑ Blair 1999, [Abstract].
  21. ↑ Boggs 2006, pp. 45, 246.
  22. ↑ Leeder 2011, pp. 287–288.
  23. 1 2 3 4 5 6 7 8 Blatt, Middleton & Murray 1980, p. 631.
  24. ↑ Blair & Mcpherson 1992, [Abstract].
  25. 1 2 3 4 Boggs 2006, p. 248.
  26. ↑ Leeder 2011, pp. 288–289.
  27. 1 2 3 Boggs 2006, p. 249.
  28. ↑ Leeder 2011, p. 290.
  29. ↑ Mack & Rasmussen 1984, [Abstract].
  30. 1 2 Boggs 2006, pp. 247–249.
  31. ↑ Bates & Jackson 1987, "fanglomerate".
  32. ↑ Blatt, Middleton & Murray 1980, p. 630.
  33. ↑ Ghinassi & Ielpi 2018, [Abstract].
  34. 1 2 Shelton 1966, p. 154.
  35. ↑ Morgan et al. 2014, [Abstract].
  36. ↑ Radebaugh 2013, [Abstract].
  37. 1 2 Moore & Howard 2005, 1 [2].
  38. ↑ Leeder 2011, pp. 291–293.
  39. ↑ Mann 1957, pp. 130–132.
  40. ↑ NASA 2009, ch. 4.
  41. ↑ Croft & Gordon 1968, p. 11.
  42. ↑ Weissmann, Mount & Fogg 2002, [Abstract].
  43. ↑ Moore & Howard 2005, 2.7 [7].
  44. ↑ Davis et al. 2021, p. 1250.
  45. ↑ Kraal et al. 2008, p. 102.
  46. ↑ Morgan et al. 2014, pp. 131–132.
  47. ↑ Harwood & Wall 2012.
  48. ↑ Davis et al. 2021, p. 1250-1253.
  49. ↑ Radebaugh 2013.
  50. 1 2 Petalas 2013, p. 439.
  51. ↑ Larsen et al. 2001, p. 1.
  52. ↑ National Research Council 1996, p. 1.
  53. ↑ Khalil 2010, [Abstract].
  54. ↑ Alkinani & Merkel 2017, "Introduction".
  55. ↑ Zaharia 2011, [Abstract].
  56. ↑ Chia 2004, "Network of Monitoring Wells in the Choshui River Alluvial Fan".
  57. ↑ Hill 2014, "Methods of building elevation".
  58. 1 2 National Research Council 1996, pp. 1–2.
  59. ↑ FEMA 2020.
  60. ↑ Larsen et al. 2001, p. 2.
  61. ↑ Santangelo et al. 2012, table 1.
  62. ↑ Chawner 1935, p. 255.
  63. ↑ Bapalu & Sinha 2005, p. 1.
  64. ↑ Leeder 2011, pp. 289–291.
  65. ↑ CNN 2008.
  66. ↑ EHA-India 2008.
  67. ↑ Coggan 2008.
  68. ↑ Gao et al. 2021, pp. 2, 20–21.
  69. ↑ Leeder & Mack 2001, [Abstract], "Applications to basic analysis: architectural models".

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<span class="mw-page-title-main">Palaeochannel</span> An inactive river or stream channel that has been filled or buried

In the Earth sciences, a palaeochannel, also spelled paleochannel, is a significant length of a river or stream channel which no longer conveys fluvial discharge as part of an active fluvial system. The term palaeochannel is derived from the combination of two words, palaeo or old, and channel; i.e., a palaeochannel is an old channel. Palaeochannels may be preserved either as abandoned surface channels on the surface of river floodplains and terraces or infilled and partially or fully buried by younger sediments. The fill of a palaeochannel and its enclosing sedimentary deposits may consist of unconsolidated, semi-consolidated, or well-cemented sedimentary strata depending on the action of tectonics and diagenesis during their geologic history after deposition. The abandonment of an active fluvial channel and the resulting formation of a palaeochannel can be the result of tectonic processes, geomorphologic processes, anthropogenic activities, climatic changes, or a variable and interrelated combination of these factors.

<span class="mw-page-title-main">Pediment (geology)</span> Very gently sloping inclined bedrock surface

A pediment, also known as a concave slope or waning slope, is a very gently sloping (0.5°–7°) inclined bedrock surface. It is typically a concave surface sloping down from the base of a steeper retreating desert cliff, escarpment, or surrounding a monadnock or inselberg, but may persist after the higher terrain has eroded away.

<span class="mw-page-title-main">Avulsion (river)</span> Rapid abandonment of a river channel and formation of a new channel

In sedimentary geology and fluvial geomorphology, avulsion is the rapid abandonment of a river channel and the formation of a new river channel. Avulsions occur as a result of channel slopes that are much less steep than the slope that the river could travel if it took a new course.

<span class="mw-page-title-main">Alluvial river</span> Type of river

An alluvial river is one in which the bed and banks are made up of mobile sediment and/or soil. Alluvial rivers are self-formed, meaning that their channels are shaped by the magnitude and frequency of the floods that they experience, and the ability of these floods to erode, deposit, and transport sediment. For this reason, alluvial rivers can assume a number of forms based on the properties of their banks; the flows they experience; the local riparian ecology; and the amount, size, and type of sediment that they carry.

Channel patterns are found in rivers, streams, and other bodies of water that transport water from one place to another. Systems of branching river channels dissect most of the sub-aerial landscape, each in a valley proportioned to its size. Whether formed by chance or necessity, by headward erosion or downslope convergence, whether inherited or newly formed. Depending on different geological factors such as weathering, erosion, depositional environment, and sediment type, different types of channel patterns can form.

An alluvial megafan is a large cone or fan-shaped deposit built up by complex deposition patterns of stream flows originating from a single source point known as an apex. Megafans differ from alluvial fans in their sheer size. Due to their larger size, they may be formed by different geomorphic processes. The criterion of what differentiates megafans from typical alluvial fans is an artificial one of scale. The scale divide varies in the literature, with the most common being a 100-km apex-to-toe length. Alternative values as little of 30-km apex-to-toe length have been proposed, as well as alternative metrics like coverage areas of greater than 10,000 square-km.

Legacy sediment (LS) is depositional bodies of sediment inherited from the increase of human activities since the Neolithic. These include a broad range of land use and land cover changes, such as agricultural clearance, lumbering and clearance of native vegetation, mining, road building, urbanization, as well as alterations brought to river systems in the form of dams and other engineering structures meant to control and regulate natural fluvial processes (erosion, deposition, lateral migration, meandering). The concept of LS is used in geomorphology, ecology, as well as in water quality and toxicological studies.

<span class="mw-page-title-main">Loess Plateau</span> Plateau in north/northwest China

The Chinese Loess Plateau, or simply the Loess Plateau, is a plateau in north-central China formed of loess, a clastic silt-like sediment formed by the accumulation of wind-blown dust. It is located southeast of the Gobi Desert and is surrounded by the Yellow River. It includes parts of the Chinese provinces of Gansu, Shaanxi and Shanxi. The depositional setting of the Chinese Loess Plateau was shaped by the tectonic movement in the Neogene period, after which strong southeast winds caused by the East Asian Monsoon transported sediment to the plateau during the Quaternary period. The three main morphological types in the Loess Plateau are loess platforms, ridges and hills, formed by the deposition and erosion of loess. Most of the loess comes from the Gobi Desert and other nearby deserts. The sediments were transported to the Loess Plateau during interglacial periods by southeasterly prevailing winds and winter monsoon winds. After the deposition of sediments on the plateau, they were gradually compacted to form loess under the arid climate.

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