An area with dunes is called a dune system.[1][2][3][4][5] In physical geography, a dune is a hill of loose sand built by aeolian processes (wind) or the flow of water.[6] Dunes occur in different shapes and sizes, formed by interaction with the flow of air or water. Dunes can be natural, but also man made(artificial).[7][8][9][10] Most kinds of dunes are longer on the stoss (upflow) side, where the sand is pushed up the dune, and have a shorter "slip face" in the lee side. The valley or trough between dunes is called a slack.

An erg or sand sea is a large[11] broad, flat area covered with wind-swept sand and/or dunes with little or no vegetation. Smaller areas are called dune fields.[12]

Dunes occur in some deserts, inland and along some coasts. Some coastal areas have one or more sets of dunes running parallel to the shoreline directly inland from the beach. In most cases, the dunes are important in protecting the land against potential ravages by storm waves from the sea. Although the most widely distributed dunes are those associated with coastal regions, the largest complexes of dunes are found inland in dry regions and associated with ancient lake or sea beds. Dunes can form under the action of water flow (fluvial processes), and on sand or gravel beds of rivers, estuaries and the sea-bed.

The modern word "dune" came into English from French around 1790,[13] which in turn came from Middle Dutch dūne.[6]


Dunes are made of sand-sized particles, and may consist of quartz, calcium carbonate, snow, gypsum, or other materials. The upwind/upstream/upcurrent side of the dune is called the stoss side; the downflow side is called the lee side. Sand is pushed (creep) or bounces (saltation) up the stoss side, and slides down the lee side. A side of a dune that the sand has slid down is called a slip face (or slipface).

The Bagnold formula gives the speed at which particles can be transported.

Aeolian dunes

Aeolian dune shapes

Five basic dune types are recognized: crescentic, linear, star, dome, and parabolic. Dune areas may occur in three forms: simple (isolated dunes of basic type), compound (larger dunes on which smaller dunes of same type form), and complex (combinations of different types).[14]

Barchan or crescentic

Barchan dunes are crescent-shaped mounds which are generally wider than they are long. The lee-side slipfaces are on the concave sides of the dunes. These dunes form under winds that blow consistently from one direction (unimodal winds). They form separate crescents when the sand supply is comparatively small. When the sand supply is greater, they may merge into barchanoid ridges, and then transverse dunes (see below).

Some types of crescentic dunes move more quickly over desert surfaces than any other type of dune. A group of dunes moved more than 100 metres per year between 1954 and 1959 in China's Ningxia Province, and similar speeds have been recorded in the Western Desert of Egypt. The largest crescentic dunes on Earth, with mean crest-to-crest widths of more than three kilometres, are in China's Taklamakan Desert.[15]

See lunettes and parabolic dunes, below, for dunes similar to crescent-shaped ones.

Transverse dunes

Abundant barchan dunes may merge into barchanoid ridges, which then grade into linear (or slightly sinuous) transverse dunes, so called because they lie transverse, or across, the wind direction, with the wind blowing perpendicular to the ridge crest.[16]

Seif or longitudinal dunes

Seif dunes are linear (or slightly sinuous) dunes with two slip faces.[16] The two slip faces make them sharp-crested. They are called seif dunes after the Arabic word for "sword". They may be more than 160 kilometres (100 miles) long, and thus easily visible in satellite images (see illustrations).

Seif dunes are associated with bidirectional winds. The long axes and ridges of these dunes extend along the resultant direction of sand movement (hence the name "longitudinal").[17] Some linear dunes merge to form Y-shaped compound dunes.[15]

Formation is debated. Bagnold, in The Physics of Blown Sand and Desert Dunes, suggested that some seif dunes form when a barchan dune moves into a bidirectional wind regime, and one arm or wing of the crescent elongates. Others suggest that seif dunes are formed by vortices in a unidirectional wind.[16] In the sheltered troughs between highly developed seif dunes, barchans may be formed, because the wind is constrained to be unidirectional by the dunes.

Seif dunes are common in the Sahara. They range up to 300 m (980 ft) in height and 300 km (190 mi) in length. In the southern third of the Arabian Peninsula, a vast erg, called the Rub' al Khali or Empty Quarter, contains seif dunes that stretch for almost 200 km and reach heights of over 300 m.

Linear loess hills known as pahas are superficially similar. These hills appear to have been formed during the last ice age under permafrost conditions dominated by sparse tundra vegetation.


Radially symmetrical, star dunes are pyramidal sand mounds with slipfaces on three or more arms that radiate from the high center of the mound. They tend to accumulate in areas with multidirectional wind regimes. Star dunes grow upward rather than laterally. They dominate the Grand Erg Oriental of the Sahara. In other deserts, they occur around the margins of the sand seas, particularly near topographic barriers. In the southeast Badain Jaran Desert of China, the star dunes are up to 500 metres tall and may be the tallest dunes on Earth.


Oval or circular mounds that generally lack a slipface. Dome dunes are rare and occur at the far upwind margins of sand seas.


Fixed crescentic dunes that form on the leeward margins of playas and river valleys in arid and semiarid regions in response to the direction (s) of prevailing winds, are known as lunettes, source-bordering dunes, bourrelets and clay dunes. They may be composed of clay, silt, sand, or gypsum, eroded from the basin floor or shore, transported up the concave side of the dune, and deposited on the convex side. Examples in Australia are up to 6.5 km long, 1 km wide, and up to 50 metres high. They also occur in southern and West Africa, and in parts of the western United States, especially Texas.[18]


U-shaped mounds of sand with convex noses trailed by elongated arms are parabolic dunes. These dunes are formed from blowout dunes where the erosion of vegetated sand leads to a U-shaped depression. The elongated arms are held in place by vegetation; the largest arm known on Earth reaches 12 km. Sometimes these dunes are called U-shaped, blowout, or hairpin dunes, and they are well known in coastal deserts. Unlike crescent shaped dunes, their crests point upwind. The bulk of the sand in the dune migrates forward.

In plan view, these are U-shaped or V-shaped mounds of well-sorted, very fine to medium sand with elongated arms that extend upwind behind the central part of the dune. There are slipfaces that often occur on the outer side of the nose and on the outer slopes of the arms.

These dunes often occur in semiarid areas where the precipitation is retained in the lower parts of the dune and underlying soils. The stability of the dunes was once attributed to the vegetative cover but recent research has pointed to water as the main source of parabolic dune stability. The vegetation that covers them—grasses, shrubs, and trees—help anchor the trailing arms. In inland deserts, parabolic dunes commonly originate and extend downwind from blowouts in sand sheets only partly anchored by vegetation. They can also originate from beach sands and extend inland into vegetated areas in coastal zones and on shores of large lakes.

Most parabolic dunes do not reach heights higher than a few tens of metres except at their nose, where vegetation stops or slows the advance of accumulating sand.

Simple parabolic dunes have only one set of arms that trail upwind, behind the leading nose. Compound parabolic dunes are coalesced features with several sets of trailing arms. Complex parabolic dunes include subsidiary superposed or coalesced forms, usually of barchanoid or linear shapes.

Parabolic dunes, like crescent dunes, occur in areas where very strong winds are mostly unidirectional. Although these dunes are found in areas now characterized by variable wind speeds, the effective winds associated with the growth and migration of both the parabolic and crescent dunes probably are the most consistent in wind direction.

The grain size for these well-sorted, very fine to medium sands is about 0.06 to 0.5 mm. Parabolic dunes have loose sand and steep slopes only on their outer flanks. The inner slopes are mostly well packed and anchored by vegetation, as are the corridors between individual dunes. Because all dune arms are oriented in the same direction, and, the inter-dune corridors are generally swept clear of loose sand, the corridors can usually be traversed in between the trailing arms of the dune. However to cross straight over the dune by going over the trailing arms, can be very difficult. Also, traversing the nose is very difficult as well because the nose is usually made up of loose sand without much if any vegetation.

A type of extensive parabolic dune that lacks discernible slipfaces and has mostly coarse grained sand is known as a zibar.[19] The term zibar comes from the Arabic word to describe "rolling transverse ridges ... with a hard surface".[20] The dunes are small, have low relief, and can be found in many places across the planet from Wyoming (United States) to Saudi Arabia to Australia. Spacing between zibars ranges from 50 to 400 metres and they don't become more than 10 metres high.[21] The dunes form at about ninety degrees to the prevailing wind which blows away the small, fine-grained sand leaving behind the coarser grained sand to form the crest.[22]

Reversing dunes

Occurring wherever winds periodically reverse direction, reversing dunes are varieties of any of the above shapes. These dunes typically have major and minor slipfaces oriented in opposite directions. The minor slipfaces are usually temporary, as they appear after a reverse wind and are generally destroyed when the wind next blows in the dominant direction.[16]


Draas are very large-scale dune bedforms; they may be tens or a few hundreds of metres in height, kilometres wide, and hundreds of kilometres in length.[16] After a draa has reached a certain size, it generally develops superimposed dune forms.[23] They are thought to be more ancient and slower-moving than smaller dunes,[16] and to form by vertical growth of existing dunes. Draas are widespread in sand seas and are well-represented in the geological record.[23]

Dune complexity

All these dune shapes may occur in three forms: simple (isolated dunes of basic type), compound (lager dunes on which smaller dunes of same type form), and complex (combinations of different types).[14] Simple dunes are basic forms with the minimum number of slipfaces that define the geometric type. Compound dunes are large dunes on which smaller dunes of similar type and slipface orientation are superimposed. Complex dunes are combinations of two or more dune types. A crescentic dune with a star dune superimposed on its crest is the most common complex dune. Simple dunes represent a wind regime that has not changed in intensity or direction since the formation of the dune, while compound and complex dunes suggest that the intensity and direction of the wind has changed.

Dune movement

The sand mass of dunes can move either windward or leeward, depending on if the wind is making contact with the dune from below or above its apogee. If wind hits from above, the sand particles move leeward. If sand hits from below, sand particles move windward. The leeward flux of sand is greater than the windward flux. Further, when the wind carrying sand particles when it hits the dune, the dune's sand particles will saltate more than if the wind had hit the dune without carrying sand particles.[24]

Coastal dunes

Coastal dunes[25] form when wet sand is deposited along the coast and dries out and is blown along the beach.[26] Dunes form where the beach is wide enough to allow for the accumulation of wind-blown sand, and where prevailing onshore winds tend to blow sand inland. The three key ingredients for coastal dune formation are a large sand supply, winds to move said sand supply, and a place for the sand supply to accumulate.[27] Obstacles—for example, vegetation, pebbles and so on—tend to slow down the wind and lead to the deposition of sand grains.[28] These small "incipient dunes or "shadow dunes" tend to grow in the vertical direction if the obstacle slowing the wind can also grow vertically (i.e., vegetation). Coastal dunes expand laterally as a result of lateral growth of coastal plants via seed or rhizome.[29][30] Models of coastal dunes suggest that their final equilibrium height is related to the distance between the water line and where vegetation can grow.[31] Coastal dunes can be classified by where they develop, or begin to take shape. Dunes are commonly grouped into either the Primary Dune Group or the Secondary Dune Group.[32] Primary dunes gain most of their sand from the beach itself, while secondary dunes gain their sand from the primary dune. Along the Florida Panhandle, most dunes are considered to be foredunes or hummocks.[33][34] Different locations around the globe have dune formations unique to their given coastal profile.

Coastal sand dunes can provide privacy and/or habitats to support local flora and fauna. Animals such as sand snakes, lizards, and rodents can live in coastal sand dunes, along with insects of all types.[35] Often the vegetation of sand dunes is discussed without acknowledging the importance that coastal dunes have for animals. Further, some animals, such as foxes and feral pigs can use coastal dunes as hunting grounds to find food.[36] Birds are also known to utilize coastal dunes as nesting grounds. All these species find the coastal environment of the sand dune vital to their species' survival.

Over the course of time coastal dunes may be impacted by tropical cyclones or other intense storm activity, dependent on their location. Recent work has suggested that coastal dunes tend to evolve toward a high or low morphology depending on the growth rate of dunes relative to storm frequency.[37][38] During a storm event, dunes play a significant role in minimizing wave energy as it moves onshore. As a result, coastal dunes, especially those in the foredune area affected by a storm surge, will retreat or erode.[39] To counteract the damage from tropical activity on coastal dunes, short term post-storm efforts such as fences can be made by individual agencies through fencing to help with sand accumulation.[40]

How a much a dune erodes during any storm event is related to its location on the coastal shoreline and the profile of the beach during a particular season. During the summer, a beach tends to take on more of a convex appearance due to gentler waves, while the same beach in the winter may take on more of a concave appearance. As a result, coastal dunes can erode much more quickly in the winter than in the summer.[41]

Ecological succession on coastal dunes

As a dune forms, plant succession occurs. The conditions on an embryo dune are harsh, with salt spray from the sea carried on strong winds. The dune is well drained and often dry, and composed of calcium carbonate from seashells. Rotting seaweed, brought in by storm waves adds nutrients to allow pioneer species to colonize the dune. These pioneer species are marram grass, sea wort grass and other sea grasses in the United Kingdom. These plants are well adapted to the harsh conditions of the foredune typically having deep roots which reach the water table, root nodules that produce nitrogen compounds, and protected stoma, reducing transpiration. Also, the deep roots bind the sand together, and the dune grows into a foredune as more sand is blown over the grasses. The grasses add nitrogen to the soil, meaning other, less hardy plants can then colonize the dunes. Typically these are heather, heaths and gorses. These too are adapted to the low soil water content and have small, prickly leaves which reduce transpiration. Heather adds humus to the soil and is usually replaced by coniferous trees, which can tolerate low soil pH, caused by the accumulation and decomposition of organic matter with nitrate leaching.[42] Coniferous forests and heathland are common climax communities for sand dune systems.

Young dunes are called yellow dunes and dunes which have high humus content are called grey dunes. Leaching occurs on the dunes, washing humus into the slacks, and the slacks may be much more developed than the exposed tops of the dunes. It is usually in the slacks that more rare species are developed and there is a tendency for the dune slacks soil to be waterlogged and where only marsh plants can survive. In Europe these plants include: creeping willow, cotton grass, yellow iris, reeds, and rushes. As for vertebrates in European dunes, natterjack toads sometimes breed here.

Coastal dune floral adaptations

Dune ecosystems are extremely difficult places for plants to survive. This is due to a number of pressures related to their proximity to the ocean and confinement to growth on sandy substrates. These include:

  • Little available soil moisture
  • Little available soil organic matter/nutrients
  • Harsh winds
  • Salt spray
  • Erosion/shifting and sometimes ephemeral substrate
  • Tidal influences

There are many adaptations plants have evolved to cope with these pressures:

  • Deep taproot to reach water table (Pink Sand Verbena)
  • Shallow but extensive root systems
  • Prostrate growth form to avoid wind/salt spray (Abronia spp., Beach Primrose)
  • Krummholz growth form (Monterrey Cypress-not a dune plant but deals with similar pressures)
  • Thickened cuticle/Succulence to reduce moisture loss and reduce salt uptake (Ambrosia/Abronia spp., Calystegia soldanella)
  • Pale leaves to reduce insolation (Artemisia/Ambrosia spp.)
  • Thorny/Spiky seeds to ensure establishment in vicinity of parent, reduces chances of being blown away or swept out to sea (Ambrosia chamissonis)

Nabkha dunes

A nabkha, or coppice dune, is a small dune anchored by vegetation. They usually indicate desertification or soil erosion, and serve as nesting and burrow sites for animals.

Sub-aqueous dunes

Sub-aqueous (underwater) dunes form on a bed of sand or gravel under the actions of water flow. They are ubiquitous in natural channels such as rivers and estuaries, and also form in engineered canals and pipelines.[43][44][45] Dunes move downstream as the upstream slope is eroded and the sediment deposited on the downstream or lee slope in typical bedform construction.[46] In the case of sub-aqueous barchan dunes, sediment is lost by their extremities, known as horns.[47][48]

These dunes most often form as a continuous 'train' of dunes, showing remarkable similarity in wavelength and height. The shape of a dune gives information about its formation environment.[49] For instance, rivers produce asymmetrical ripples, with the steeper slip face facing downstream. Ripple marks preserved in sedimentary strata in the geological record can be used to determine the direction of current flow, and thus an indication of the source of the sediments.

Dunes on the bed of a channel significantly increase flow resistance, their presence and growth playing a major part in river flooding.

Lithified dunes

A lithified (consolidated) sand dune is a type of sandstone that is formed when a marine or aeolian sand dune becomes compacted and hardened. Once in this form, water passing through the rock can carry and deposit minerals, which can alter the color of the rock. Cross-bedded layers of stacks of lithified dunes can produce the cross-hatching patterns, such as those seen in the Zion National Park in the western United States.

A slang term, used in the southwest US, for consolidated and hardened sand dunes is "slickrock", a name that was introduced by pioneers of the Old West because their steel-rimmed wagon wheels could not gain traction on the rock.


Sand dunes can have a negative impact on humans when they encroach on human habitats. Sand dunes move via a few different means, all of them helped along by wind. One way that dunes can move is by saltation, where sand particles skip along the ground like a bouncing ball. When these skipping particles land, they may knock into other particles and cause them to move as well, in a process known as creep. With slightly stronger winds, particles collide in mid-air, causing sheet flows. In a major dust storm, dunes may move tens of metres through such sheet flows. Also as in the case of snow, sand avalanches, falling down the slipface of the dunes—that face away from the winds—also move the dunes forward.

Sand threatens buildings and crops in Africa, the Middle East, and China. Drenching sand dunes with oil stops their migration, but this approach is quite destructive to the dunes' animal habitats and uses a valuable resource. Sand fences might also slow their movement to a crawl, but geologists are still analyzing results for the optimum fence designs. Preventing sand dunes from overwhelming towns, villages, and agricultural areas has become a priority for the United Nations Environment Programme. Planting dunes with vegetation also helps to stabilise them.


Dune habitats provide niches for highly specialized plants and animals, including numerous rare species and some endangered species. Due to widespread human population expansion, dunes face destruction through land development and recreational usages, as well as alteration to prevent the encroachment of sand onto inhabited areas. Some countries, notably the United States, Australia, Canada, New Zealand, the United Kingdom, Netherlands, and Sri Lanka have developed significant programs of dune protection through the use of sand dune stabilization. In the U.K., a Biodiversity Action Plan has been developed to assess dunes loss and to prevent future dunes destruction.





North America

South America


World's highest dunes

Note: This table is partially based on estimates and incomplete information.
DuneHeight from Base feet/metresHeight from Sea Level feet/metresLocationNotes
Duna Federico Kirbus ≈4,035/1,230≈9,334/2,845Bolsón de Fiambalá, Fiambalá, Catamarca Province, ArgentinaHighest in the world[58]
Cerro Blanco ≈3,860/1,176≈6,791/2,080Nazca Province, Ica Region, Peru 14.868°S 74.838°W / -14.868; -74.838 (Cerro Blanco Dune)Highest in Peru, second highest in the world
Badain Jaran Dunes ≈1,640/500≈6,640/2,020Badain Jaran Desert, Alashan Plain, Inner Mongolia, Gobi Desert, ChinaWorld's tallest stationary dunes and highest in Asia[59]
Rig-e Yalan Dune ≈1,542/470≈3,117/950Lut Desert, Kerman, IranNear World the hottest place (Gandom Beryan)
Average Highest Area Dunes 1,410/430?≈6,500/1,980?Isaouane-n-Tifernine Sand Sea, Algerian SaharaHighest in Africa
Big Daddy/Dune 7
(Big Mama?)[60]
1,256/383≈1,870/570Sossusvlei Dunes, Namib Desert, Namibia / Near Walvis Bay Namib Desert, Namibiaaccording to the Namibian Ministry of Environment & Tourism the highest dune in the world
Mount Tempest ≈920/280≈920/280Moreton Island, Brisbane, AustraliaHighest in Australia
Star Dune >750/230≈8,950/2,730Great Sand Dunes National Park and Preserve, Colorado, USAHighest in North America
Dune of Pyla ≈345/105≈699/130Bay of Arcachon, Aquitaine, FranceHighest in Europe
Ming-Sha Dunes ?5,660/1,725Dunhuang Oasis, Taklamakan Desert, Gansu, China
Medanoso Dune ≈1805/550≈5446/1,660Atacama Desert, ChileHighest in Chile

Sand dune systems

(coastal dunes featuring succession)

Extraterrestrial dunes

Dunes can likely be found in any environment where there is a substantial atmosphere, winds, and dust to be blown. Dunes are common on Mars and in the equatorial regions of Titan.

Titan's dunes include large expanses with modal lengths of about 20–30 km. The regions are not topographically confined, resembling sand seas. These dunes are interpreted to be longitudinal dunes whose crests are oriented parallel to the dominant wind direction, which generally indicates west-to-east wind flow. The sand is likely composed of hydrocarbon particles, possibly with some water ice mixed in.[61]

See also


  1. http://www.encyclopedia.chicagohistory.org/pages/394.html
  2. https://www.biology-fieldwork.org/a-level/succession/sand-dunes/
  3. https://www.michigan.gov/documents/deq/wrd-cda-dune-systems_558207_7.pdf
  4. https://www.restoconlife.eu/en/habitat-to-be-protected/the-dune-system/
  5. https://www.dropbearadventures.com.au/2018/08/10/the-great-sandy-coastal-dune-system/
  6. Fowler, H.W.; Fowler, F.G. (1984). Sykes, J.B. (ed.). The Concise Oxford Dictionary of Current English (7th ed.). Oxford: Clarendon Press. ISBN 978-0-19-861132-5.
  7. https://www.telegraph.co.uk/expat/expatnews/6613101/Dutch-construct-dunes-against-rising-seas.html
  8. "Archived copy". Archived from the original on 17 November 2019. Retrieved 17 November 2019.CS1 maint: archived copy as title (link)
  9. https://www.audubon.org/magazine/march-april-2015/slip-sliding-away
  10. https://www.ctc-n.org/sites/www.ctc-n.org/files/UNFCCC_docs/ref18x43_35.pdf
  11. "Erg Landforms". WorldLandForms. Retrieved 13 October 2019.
  12. "Aeolian Landform (08. Erg)". Fast Wind To Aim. Blogspot. Retrieved 13 October 2019.
  13. "Dune—Define Dune". Dictionary.com. Dictionary.com, LLC. Retrieved 1 May 2018.
  14. Types of dunes, a USGS publication
  15. "Types of Dunes". Archived from the original on 14 March 2012. Retrieved 8 March 2012.
  16. Mangimeli, John (10 September 2007), Geology of Sand Dunes, U.S.A. National Park Service
  17. Radebaugh, Jani; Sharma, Priyanka; Korteniemi, Jarmo; Fitzsimmons, Kathryn E. (2014). "Longitudinal Dunes (or Linear Dunes)". Encyclopedia of Planetary Landforms. pp. 1–11. doi:10.1007/978-1-4614-9213-9_460-2. ISBN 978-1-4614-9213-9.
  18. Twidale, C.R. & Campbell, E.M. (2005, revised edition): Australian landforms: understanding a low, flat, arid and old landscape. Rosenberg Publishing. pp. 241–3. ISBN 1 877058 32 7
  19. Goudie, Ron Cooke; Andrew Warren; Andrew (1996). Desert geomorphology (2. impr. ed.). London: UCL Press. pp. 395–396. ISBN 978-1-85728-017-3.
  20. Goudie, Ron Cooke; Andrew Warren; Andrew (1996). Desert geomorphology (2. impr. ed.). London: UCL Press. p. 395. ISBN 978-1-85728-017-3.
  21. "USGS Landform Glossary" (PDF). United States Geological Survey. Retrieved 3 October 2013.
  22. Nielsen, Ole. "Zibar Dunes". My Opera. Archived from the original on 3 November 2013. Retrieved 3 October 2013.
  23. Lancaster, N. (1 March 1988). "The development of large aeolian bedforms". Sedimentary Geology. 55 (1–2): 69–89. Bibcode:1988SedG...55...69L. doi:10.1016/0037-0738(88)90090-5.
  24. Jiang, Hong; Dun, Hongchao; Tong, Ding; Huang, Ning (15 April 2017). "Sand transportation and reverse patterns over leeward face of sand dune". Geomorphology. 283: 41–47. Bibcode:2017Geomo.283...41J. doi:10.1016/j.geomorph.2016.12.030.
  25. https://www.nature.com/scitable/knowledge/library/coastal-dunes-geomorphology-25822000/
  26. Bird, ECF (1976). Coasts: an introduction to systematic geomorphology. Canberra, Australia: Australian National University Press.
  27. Goldsmith, V (1978). Coastal dunes. In Coastal sedimentary environments. New York, NY: Springer. pp. 171–235.
  28. Hesp, P. (1989). "A review of biological and geomorphological processes involved in the initiation and development of incipient foredunes". Proceedings of the Royal Society of Edinburgh. Section B. Biological Sciences. 96: 181–201. doi:10.1017/S0269727000010927.
  29. Godfrey, P. J. (1 September 1977). "Climate, plant response and development of dunes on barrier beaches along the U.S. east coast". International Journal of Biometeorology. 21 (3): 203–216. Bibcode:1977IJBm...21..203G. doi:10.1007/BF01552874. ISSN 0020-7128.
  30. Goldstein, Evan B.; Moore, Laura J.; Vinent, Orencio Durán (8 August 2017). "Lateral vegetation growth rates exert control on coastal foredune "hummockiness" and coalescing time". Earth Surface Dynamics. 5 (3): 417–427. doi:10.5194/esurf-5-417-2017. ISSN 2196-6311.
  31. Durán, O.; Moore L. J. (2013). "Vegetation controls on the maximum size of coastal dunes". Proceedings of the National Academy of Sciences. 110 (43): 17217–17222. Bibcode:2013PNAS..11017217D. doi:10.1073/pnas.1307580110. PMC 3808624. PMID 24101481.
  32. Sloss, CR; Shepherd, M; Hesp, P. "Coastal dunes: geomorphology". Nature Education Knowledge. Retrieved 4 December 2018.
  33. Houser, C; Hapke, C; Hamilton, S (15 August 2008). "Controls on coastal dune morphology, shoreline erosion and barrier island response to extreme storms". Geomorphology. 100 (3–4): 223–40. Bibcode:2008Geomo.100..223H. doi:10.1016/j.geomorph.2007.12.007.
  34. Claudino-Sales, V; Wang, P; Horwitz, MH (15 March 2008). "Factors controlling the survival of coastal dunes during multiple hurricane impacts in 2004 and 2005: Santa Rosa Barrier Island, Florida". Geomorphology. 95 (3–4): 295–315. Bibcode:2008Geomo..95..295C. doi:10.1016/j.geomorph.2007.06.004.
  35. Ronica, D (27 October 2008). "How sand dunes work". HowStuffWorks. Retrieved 4 December 2018.
  36. Hill, K. "Dune Habitats". Smithsonian Marine Station. Retrieved 4 December 2018.
  37. Durán Vinent, Orencio; Moore, Laura (February 2015). "Barrier island bistability induced by biophysical interactions". Nature Climate Change. 5 (2): 158–162. Bibcode:2015NatCC...5..158D. doi:10.1038/nclimate2474. ISSN 1758-6798.
  38. Goldstein, Evan B.; Moore, Laura J. (2016). "Stability and bistability in a one-dimensional model of coastal foredune height". Journal of Geophysical Research: Earth Surface. 121 (5): 964–977. Bibcode:2016JGRF..121..964G. doi:10.1002/2015JF003783. ISSN 2169-9011.
  39. Morton, RA (1 May 1976). "Effects of Hurricane Eloise on beach and coastal structures, Florida Panhandle". Geology. 4 (5): 277–80. Bibcode:1976Geo.....4..277M. doi:10.1130/0091-7613(1976)4<277:EOHEOB>2.0.CO;2.
  40. Charbonneau, B; Wnek, JP. "Reactionary fence installation for post-Superstorm Sandy dune recovery". EarthArXiv. Retrieved 4 December 2018.
  41. Maine Sea Grant. "Seasonal changes". Maine Sea Grant College Program. Archived from the original on 5 December 2018. Retrieved 4 December 2018.
  42. Miles, J. (1985). "The pedogenic effects of different species and vegetation types and the implications of succession". European Journal of Soil Science. 36 (4): 571–584. doi:10.1111/j.1365-2389.1985.tb00359.x.
  43. Franklin, E.M.; Charru, F. (2009). "Morphology and displacement of dunes in a closed-conduit flow". Powder Technology. 190 (1–2): 247–251. arXiv:1608.07729. doi:10.1016/j.powtec.2008.04.065.
  44. Franklin, E. M.; Charru, F. (2011). "Subaqueous barchan dunes in turbulent shear flow. Part 1. Dune motion". Journal of Fluid Mechanics. 675: 199–222. Bibcode:2011JFM...675..199F. doi:10.1017/S0022112011000139.
  45. Cardona Florez, Jorge Eduar; Franklin, Erick de Moraes (2016). "The formation and migration of sand ripples in closed conduits: Experiments with turbulent water flows". Experimental Thermal and Fluid Science. 71: 95–102. arXiv:1608.04792. Bibcode:2016arXiv160804792E. doi:10.1016/j.expthermflusci.2015.10.017.
  46. Prothero, D. R. and Schwab, F., 1996, Sedimentary Geology, pg. 45–49, ISBN 0-7167-2726-9
  47. Alvarez, Carlos A.; Franklin, Erick M. (18 December 2017). "Birth of a subaqueous barchan dune". Physical Review E. 96 (6): 062906. arXiv:1712.07162. Bibcode:2017PhRvE..96f2906A. doi:10.1103/PhysRevE.96.062906. PMID 29347350.
  48. Alvarez, Carlos A.; Franklin, Erick M. (19 October 2018). "Role of Transverse Displacements in the Formation of Subaqueous Barchan Dunes". Physical Review Letters. 121 (16): 164503. arXiv:1810.11074. doi:10.1103/PhysRevLett.121.164503. PMID 30387641.
  49. "Ripples". Archived from the original on 1 May 2018. Retrieved 11 January 2018.
  50. "Alexandria Coastal Dunefields". UNESCO World Heritage. Archived from the original on 18 November 2009. Retrieved 11 January 2010.
  51. Wahiba Sands
  52. "Herring Cove Beach – Cape Cod National Seashore (U.S. National Park Service)". www.nps.gov. Retrieved 29 July 2018.
  53. "Race Point Beach – Cape Cod National Seashore (U.S. National Park Service)". www.nps.gov. Retrieved 29 July 2018.
  54. "Province Lands Bike Trail – Cape Cod National Seashore (U.S. National Park Service)". www.nps.gov. Retrieved 29 July 2018.
  55. Mann, D. H.; Heiser P. A.; Finney B. P. (2002). "Holocene history of the Great Kobuk Sand Dunes, Northwestern Alaska" (PDF). Quaternary Science Reviews. 21 (4): 709–731. Bibcode:2002QSRv...21..709M. CiteSeerX doi:10.1016/S0277-3791(01)00120-2. Archived from the original (PDF) on 19 September 2015.
  56. Smith, S. & Mark, S. (2006). Alice Gray, Dorothy Buell, and Naomi Svihla: "Preservationists of Ogden Dunes". The South Shore Journal, 1. "Account Suspended". Archived from the original on 13 September 2012. Retrieved 11 June 2012.
  57. Smith, S. & Mark, S. (2009). "The Historical Roots of the Nature Conservancy in the Northwest Indiana/Chicagoland Region: From Science to Preservation". The South Shore Journal, 3. "Account Suspended". Archived from the original on 1 January 2016. Retrieved 22 November 2015.
  58. Kirbus, Federico B. "Bolsón de Fiambalá". Sandboard Magazine. Retrieved 1 May 2018.
  59. "Mystery of world's tallest sand dunes solved"—24 November 2004—New Scientist Archived 26 October 2008 at the Wayback Machine
  60. Big Mama highest dune Archived 2 September 2009 at the Wayback Machine
  61. Peeking Through the Haze: Titan's Surface, part II—The Planetary Society Blog | The Planetary Society Archived 28 April 2007 at the Wayback Machine


  • Bagnold, Ralph (2012) [1941]. The Physics of Blown Sand and Desert Dunes. Courier Dover Publications. ISBN 978-0-486-14119-0.

Further reading

This article is issued from Wikipedia. The text is licensed under Creative Commons - Attribution - Sharealike. Additional terms may apply for the media files.