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Definition of Chenier:
An accretionary feature consisting of a long, low lying, narrow strip of (gravelly) sand, typically up to 3 m high and 40 to 400 m wide, often shelly, deposited in the form of wave-built beach ridge on a swampy, deltaic, or alluvial coastal plain of fine sediment.
This is the common definition for Chenier, other definitions can be discussed in the article

Chenier plain

Fig. 1. Chenier plain in Guinée (West Africa). Image Google Earth.

A chenier plain is a strand plain consisting of long, narrow beach ridges (cheniers) and intervening mudflats with marsh or swamp vegetation. The word chenier is derived from the Cajun French word, chène, meaning oak, the dominant tree growing on the crests of cheniers in southwestern Louisiana. Often, relict cheniers can be observed as a series of coast-parallel ridges in the landscape, separated by muddy soil and/or peat[1]. They are easily distinguishable because of their higher elevation and different composition, generating a striking contrast to their surroundings. Consequently, they are often used for roads, dikes and settlements. Cheniers play a crucial role in protecting coastlines from erosion, serving as a natural barrier. Additionally, mangroves, which also contribute to shoreline stabilization, predominantly grow in areas protected by cheniers.

Chenier occurrence

Cheniers are commonly found on gently sloping coasts characteized by a low to moderate wave-energy climate[2]. Chenier plains are associated with prograding littoral environments or deltas with an ample supply of fine sediments. Extensive chenier plains exist along the coasts of Louisiana (USA) and Surinam-Guyana and in the deltas of the Huanghe and Changjiang rivers in East China. Chenier plains are found on many other mud coasts, for example the Red River delta (Vietnam), central Java, Guinée and Sierra Leone. The tidal range is not a discriminating factor for the occurrence of chenier plains.

Chenier formation

Fig. 2. Schematic of the stages of chenier formation[3]. Top: Prograding mudflat including some sand and shells. Middle: Winnowing and offshore transport of mud by energetic wave action and onshore transport of the resulting sandy/shelly top layer. Bottom: Mudflat progradation seaward of the chenier ridge. Adapted from Penland and Suter (1989[4]).

Chenier formation depends on a specific balance between wave action and sediment availability and is generally episodic[5], see Fig. 2. Contrary to beach ridges found on sandy shores, which are built from material similar in composition to the adjacent beach and shoreface, the volume of a chenier is limited by the availability of coarser particles in the otherwise muddy shoreface[6]. Under energetic (but not necessarily extreme) wave conditions, mud is gradually washed out of the seabed which initially consists of a mixture of mud with some coarser sediments (sand, possibly including shell fragments). Onshore transport of the resulting sandy top layer over the muddy substrate is in first instance promoted by waves and tidal currents, with an important role of wave asymmetry[7]. Building of a berm crest above spring tide or storm surge level takes place under average storm conditions by washover processes[2][7]. Due to the limited availability of coarse sediments, cheniers do not build up high. Only in rare occasions can cheniers grow further in volume and elevation. The landward migration may end when the chenier has reached the landward limit of onshore sediment transport or when a new chenier develops seaward on the prograding mudflat[2].

In other deltaic conditions, sandy ridges develop at the mouths of delta distributaries, where they shelter erosional backwaters that are subsequently filled with mud. These depositional chenier plains are typical of the Danube and Rhone deltas[8].

Related articles

Coastal mud belt
Dynamics of mud transport
Sediment deposition and erosion processes
Characteristics of muddy coasts
Coastal and marine sediments


  1. Russell, R.J. and Howe, H.V. 1935. Cheniers of southwestern Louisiana. Geogr. Rev. 25: 449-461
  2. 2.0 2.1 2.2 Augustinus, P.G.E.F. 1989. Cheniers and chenier plains: a general introduction. Mar. Geol. 90: 219–229
  3. Hoyt, J.H. 1969. Chenier versus barrier, genetic and stratigraphic distinction. Bull. Am. Assoc. Pet. Geol. 53: 299-306
  4. Penland, S. and Suter, J.R. 1989. The geomorphology of the Mississippi River Chenier Plain. Marine Geology 90: 231–258
  5. Otvos, E.G. and Price, W.A. 1979. Problems of chenier genesis and terminology - an overview. Mar. Geol. 31: 251–263
  6. Anthony, E.J., Brunier, G., Gardel, A. and Hiwat, M. 2019. Chenier morphodynamics on the Amazon-influenced coast of Suriname, South America: implications for beach ecosystem services. Front. Earth Sci. 7: 1–20
  7. 7.0 7.1 Tas, S. A. J., van Maren, D. S. and Reniers, A. J. H. M. 2022. Chenier formation through wave winnowing and tides. Journal of Geophysical Research: Earth Surface 127, e2022JF006792
  8. Nardin, W. and Fagherazzi, S. 2018. The role of waves, shelf slope, and sediment characteristics on the development of erosional chenier plains. Geophysical Research Letters 45: 8435–8444

The main author of this article is Job Dronkers
Please note that others may also have edited the contents of this article.

Citation: Job Dronkers (2023): Chenier. Available from [accessed on 30-05-2023]