Definition and Morphology
Cheniers are relict wave-built coastal plain ridges that occur in sets inland from the shoreline where they originally formed along an active beach as littoral ridges. They are sheltered from daily wave and tidal processes and generally consist of sand, sandy shell, and occasionally sandy gravel. Chenier ridge sequences may develop on prograding deltas or non-deltaic coastal plains. Cheniers form subparallel sets of elongated, narrow ridges (typically up to 3 m high and 40–400 m wide), usually rising slightly above the highest high-tide level. Wave action and storm overwash build the original littoral ridges. The term chenier (Russell and Howe 1935) originated in the French native word (chêne) for the majestic evergreen “live oak” tree (Quercus virginiana) that lines chenier ridges of southwest Louisiana. Cheniers differ from beach ridge sets (q.v.) by the presence of intervening, parallel, low, and level surfaces that represent predominant portion of chenier plains.
Cheniers are separated by wide intertidal or shallow subtidal mudflats, much wider than the ridges, covered by wetland vegetation. Low-lying interior inter-ridge flats may occasionally be submerged by high tides or river floodwaters to form brackish or fresh water wetlands. Intervening areas may even be barren of vegetation or covered at least in part by grasses, salt marsh, freshwater swamp, or mangroves. Misidentification can happen when inter-ridge swales (lows) in a (non-chenier) ridge plain are filled by fine-grained peaty alluvial or delta deposits, covered by recent wetland vegetation. The term chenier plain includes both the inter-ridge flats and the chenier ridges, where at least two successively formed ridges are present (Otvos and Price 1979). The latter caveat has unfortunately, occasionally has been disregarded. The term was misapplied to beaches capped by shell-concentrate berm ridges at high-tide level where the beach foreshore faces low intertidal mudflats along the ocean shore (e.g., Neal et al. 2002; Weill et al. 2012). Equally inappropriately, a “chenier” designation was also applied in at least one highly dynamic setting with significant ebb and flood tidal action. Prograding arms of constantly changing, low intertidal sand bar ridges in this small estuary have been migrating over and surrounded small areas of intertidal-subtidal mud flats (Morales et al. 2014).
Chenier coasts are associated with a broad spectrum of tidal amplitudes that range from microtidal (e.g., SW Louisiana) and mesotidal to macrotidal (e.g., Van Diemen Gulf in northern Australia, Gulf of California). Most cheniers are of mid- to late-Holocene age, but cheniers of Pleistocene age occur in the Colorado Delta region of the Gulf of California (Meldahl 1993).
In small bays mudflat progradation, alternating with sand and shell accumulation and chenier incorporation into developing chenier ridges occur simultaneously (Woodroffe and Grime 1999). Side-by-side formation of a chenier passing laterally into a sandy beach ridge was described from the northeastern coast of Australia (Chappell and Grindrod 1984).
Regressive and Transgressive Cheniers: Sea Level Relationship
Following the original definition of cheniers as transgressive features (Russell and Howe 1935, pp. 27–34), several authors defined “true” chenier ridges as landward-driven landforms (Otvos 2000). However, stratigraphic and morphological data indicate that most Louisiana cheniers are not transgressive.
Transgressive cheniers are generally emplaced during storm surges, when large waves on a temporarily raised sea level sweep beach sediment inland. With their shallow ridge bases, transgressive chenier ridges display washover-induced, landward-inclined stratification. They overlie intertidal, low-supertidal mud/marsh surfaces at very shallow depths. Powerful tropical storms often erode and even flatten landward migrating ridges. Even if lesser events effectively translated them landward before and after the storm, the 1974 hurricane surprisingly had no appreciable impact on the landward migration of sand and shell ridges in Shoal Bay, Australia (Woodroffe and Grime 1999). Several articles shed light on details of evolution and regional correlations of cheniers in Australia (Horne et al. 2014) and New Zealand (Daugherty and Dickson 2012; Horne et al. 2015). Chenier plains in northern and southern Australia developed mostly between 2400 and 1300 yr BP and probably during the last 1000 years.
Conditions of Mudflat Development
Alternating chenier ridge and inter-ridge-mudflat development, in Louisiana, has long been associated with periodic avulsion-related delta lobe switching. Distal positions of river discharge generally result in (mudflat) shore erosion and shell and sand concentration that lead to formation of (“pre-chenier”) add hyphen between pre and chenier active littoral ridges along the shoreline. Large-scale mud discharge from nearby (proximal) active lobes, on the other hand, favors mudflat progradation. Roberts and Huh (1995) and Anthony et al. (2011) provided valuable new insights regarding the evolution of Amazon-discharge-related Guiana mud belts, respectively, recently developing Atchafalaya mudflats along Louisiana’s previously severely receded eastern chenier plain sector. Longshore transport from the Atchafalaya delta and onshore stranding of suspended fluid mud during winter cold front water level set-down resulted in extensive mudflat formation. Momentarily dry weather and other climate conditions favor the process. In the course of desiccation and compaction, low-tidal flats prograded along a 20 km stretch of the low-microtidal chenier coast. Progradation averaged 50 m/year in the most actively accreting sectors.
Cheniers plains, including regressive and transgressive relict littoral ridge sets and intervening, often wetland-covered intertidal mudflats reflect important coastal episodes of stream discharge and shore erosion- and progradation-related changes. The occasionally still misused term “chenier plain” includes both the inter-ridge flats and the chenier ridges, where at least two successively formed ridges are present. Chenier ridges are isolated from the active beaches that front the chenier plains; they are insulated from daily littoral processes of wave and tidal action. Ridges are composed of sand, seashell, and occasionally gravel. New findings confirm the role of weather conditions in the sediment sources, desiccation, and consolidation of inter-ridge mud flats. In the large Louisiana chenier plain, delta lobe switching due to trunk stream avulsion played a role in changing sites of mud flat deposition. Two late Holocene episodes of chenier plain development have been identified in Australia’s numerous small chenier plains. (q.v.,Beach ridges; Gulf shorelines: Last Eustatic Cycle).
- Anthony EJ, Gardel A, Dolique F, Marin D (2011) The Amazon-influenced mud-bank coast of South America: an overview of short- to-long-term morphodynamics of “inter-bank” areas and chenier development. J Coastal Res Special Issue 64:25–29Google Scholar
- Byrne JV, LeRoy DO, Riley CM (1959) The chenier plain and its stratigraphy, southwestern Louisiana. Trans Gulf Coast Assoc Geol Soc 9:237–260Google Scholar
- Chappell J, Grindrod J (1984) Chenier plain formation in northern Australia. In: Thom BG (ed) Coastal geomorphology in Australia. Academic, Sydney, pp 197–231Google Scholar
- Cook PJ, Polach HA (1973) Sedimentology and Holocene history of a tropical estuary (Broad Sound, Queensland). Bur Mine Res Bull 170:260Google Scholar
- Otvos EG (2000) Beach ridges-definition and significance. Geomorphology 32: 83-108Google Scholar
- Roberts HH, Huh OK (1995) The eastern Chenier plain: an update on downdrift coastal progradation associated with the building of an new Holocene delta lobe in the Mississippi Delta Complex. Gulf Coast Assoc Geol Soc Trans 45:644–646Google Scholar
- Russell RJ, Howe HV (1935) Geology of Cameron and Vernillion parishes. Louisiana Geol Survey Bull 6:242Google Scholar
- Thomson RW (1968) Tidal flat sedimentation on the Colorado river delta, northwest Gulf of California. Geol Soc Am Mem 107:133Google Scholar
- Vann JH (1959) The geomorphology of the Guiana coast. Second coastal geography conference. Coastal Studies Institute, Louisiana State University, Washington, DC, pp 153–187Google Scholar