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Coastal Dynamics and Chenier Sands in French Guiana

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Coastal Dynamics and Chenier Sands in French Guiana Marine Geology, 90 (1989) 239-267 259 Elsevier Science Publishers B.V., Amsterdam - Printed in The Netherlands , COASTAL DYNAMICS AND CHENIER SANDS IN FRENCH GUIANA M.T. PROST Centre ORSTOM de Cayenne, Departement Hydrologie, BP 165,97323, Cayenne (French Guiana) ? (Received April 30, 1988; revised and accepted January 15, 1989) Abstract Prost, M.T., 1989. Coastal dynamics and chenier sands in French Guiana. In: P.G.E.F. Augustinus (Editor), Cheniers and Chenier Plains. Mar. Geol., 90: 259-267. The Holocene coastal plain of French Guiana is an open chenier plain. The shoreline is characterized by vast . migrating shoreface-attached mudbanks. Cheniers develop within the interbank zone. These sandbodies, which rest on the Demerara marine clays, have also been observed in the inner parts of the coastal plain. This paper deals with the coastal area between Mahuri and the Maroni Rivers in French Guiana. An overview of the present state of knowledge regarding the coastal research in this area is given, and based on new evidence the problem of the provenance of the sandy accumulations will be discussed and further defined. Introduction Geographical setting The French Guiana coastal plain is an open The coastal plain of French Guiana com- am ocean chenier plain. The shoreline comprises a ier prises zone 320 km long from the Oyapock 30- an extensive shoreface with attached mudflats River to the Maroni River (Fig.l). This area and is characterized by waterfront mangroves represents only 6% of the 90,000 km2 of French rsh and subcoastal swamps and marshes. Aerial Guiana, the other 94% being formed by the ral photographs, low altitude flights, SPOT images Precambrian Guianese Shield and covered oc. in and field observations enable identification of with rain forest. Two main morphological ‘.S* narrow cheniers along the inner part of the - units have been recognized within the coastal 3s- coastal plain. At present, cheniers are still area (Fig.2): forming along the coastline. These are related (1) The “young” coastal plain situated ics In: to the specific dynamics of this coast. approximately at an altitude of between O and The development of the coast may be 5 m and formed by Holocene sediments (marine deduced from the combination of data on the and fluviomarine clays and silty clays). The present-day morphogenetic processes and inner part of the “young” coastal plain was those on palaeogeomorphology. In the ‘last formed in a paralic environment and is inter- decades, numerous investigators have been sected by narrow and elongated cheniers involved in the study of the French Guiana located approximately parallel to the present coast or of its related problems and in recent shoreline and separated by fine-grained de- years the interest in coastal research has posits, all part of the Demerara Formation. increased. (2) The “old” coastal plain situated approxi- 0025-3227/89/$03.50 0 1989 Elsevier Science Publishers B.V. ~~~~~~ Fonds Documentaire - 260 Fig.1. Skc ch map of the northern part of French Guiana. mately at a altitude of between 5 and 15 m and bert (1956, 1959, 1961, 1962), Boye (1959, 1963,), formed by the Pleistocene sediments of the Turenne (1978), Blancaneaux (1981) and Prost Coswine Formation. This formation is com- (1985, 1986a, b). The importance of the supply posed of marine clays, silty clays and fine of the Amazon River to the coastal sedimenta- sandy deposits. Between Cayenne and Ira- tion and the morphological evolution of the coubo the sandy sediments are mainly concen- coast was emphasized by researchers such as Fi trated in bars (barres prélittorales). The width Cruys (1959), Lafond (1967), Bouysse et al. of the old coastal plain diminishes in an (1977), Jeantet (1982), and reassessed during eastward direction, and the young coastal the research conducted by Pujos et al. (1984, of plain becomes more prominent in the opposite 1985), Pujos and Odin (1986), Jouanneau and tr direction, especially between Cayenne and the Pujos (1988), and Lointier and Prost (1988). fo Oyapock River. Along the. shoreline extensive shoreface- q1 attached mudflats migrate slowly westward, m Coastal research the shoreline undergoing progradation in TI these areas. Between two mudbanks - in the cc interbank zones - the shoreline undergoes During the past 30 years, particularly since PZ the mid-seventies, research concerning the Ho- erosion and retreats. This system of accretion kr t ’ locene coastal plain and the shoreline changes and erosion migrates continually to the west. SI has increased. The investigations of the Holo- The frequency and intensity of sedimentation en cene coastal plain with emphasis on the predom- and erosion vary in time and space, and their 19 inantly clayey deposits and on the sandy coastal mutual relationship determines whether there Ri formations will be discussed briefly. is a net accretion or erosion. This dynamic process creates very short- 191 The Holocene coastal plain term morpholo&cal variations and is related to Lc the huge discharge from the Amazon River Pr Geological and geomorphological features (110-130 x lo6 tons per yr of suspended sedi- in1 have been analyzed, among others, by Chou- ment, öf which l0-20% moves along the coast thi ,, 261 LOWLANDS HIGHLANDS -/ \ N +++++++ m Demerara sand rm" Demerara clay ( HOLOCENE ) Coswine sand (PLEISTOCENE) FEI Coswine clay ( PLEISTOCENE) 'Ply ita- Crystalline basement the L as Fig.2. Diagrammatical section of French Guiana coastal plain. al. ,ing 384, of the Guianas) (Eisma, 1988). The sediment region and their morphosedimentary evolu- 2nd transport takes place in suspension and in the tion. form of migrating mudbanks. The estimated Many papers on estuaries in French Guiana ice- quantities are 140~10~m3/yr and 110~10~ have been published: Brugière (1963), LCHF trd, m3/yr respectively (Wells and Coleman, 1978). (1965, 1967), Lafond (1967), Berthois and in There are presently six mudbanks along the Hoorelbeck (1968), Bellesort and Martin (1968), the coast of French Guiana, of which the intertidal Mignot (1970), Dubreuil et al. (1974), Roche oes parts (the mudflats) vary in length from 20 to 40 (1978), Fritsch (1984), Audige (1986), Lointier ion km. Chenier formation is associated with the (1986), Jouanneau and Pujos (1987, 1988). est. shoreline dynamics and takes place in the Lointier and Prost (1988) have shown, using ion I erosive interbank zones (Augustinus, 1978, hydrological and sedimentological investiga- teir 1980; Rine and Ginsburg, 1985; Prost, 1986a, b; tions, that the influence of the local rivers ere Rine, 1988). on the coastal sedimentation is minimal - Analysis of shoreline changes (Boye, 1959, approximately 1% of the suspended load trans- wt- 1963; Turenne, 1978; Froidefond et al., 1985; ported along the coast. The supply of alluvial €to Lointier, 1986; Froidefond and Pujos, 1988a, b; sand is limited, due to hydrodynamic condi- ver Prost, 1988, in press) and displacement of tions. ?di- intertidal mudflats has contributed new data to The sedimentology and the stratigraphy of 'ast the research on muddy coasts of the equatorial the Holocene sediments was studied by Chou- 262 bert (1959, 1961), Boye and Cruys (1961), Boye formations at this point are at a depth of (1963), Sourdat and Delaune (1970), Turenne approximately 30 m (Leveque, 1962). Several (1978), Guillobez (1979), Prost and Lointier other cores drilled by the BRGM and by (1987). In his comparative analysis of Suriname Marius (1986) in the Mana area were compli- and Guyana, Turenne (1978) recognized three mented with field observations. sedimentary phases, Mara (8000 yrs B.P.), Marius (1966) distinguished two sedimento- Moleson (2500-1300 yrs B.P.) and Comowine logical facies within the sediments of the (1000 yrs B.P.-present). The Mara/Moleson Demerara Formation (Mana area): a mangrove and Moleson/Comowine phases are separated facies (a) and a subtidal facies (b)..The facies by sandy ridges. The thickness of the Demerara association passes gradually from (b) to (a), deposits in French Guiana does not exceed with laminations of sand and mud passing into 15 m (Leveque, 1962). dark grey unstructured clays with many roots Two cores drilled by the Bureau de Re- and much organic matter. cherches Geologiques et Minières (BRGM) on The muddy environment appears to be domi- the left bank of the Approuague River passed nant, not only along the shoreline but also on through 10 m of Demerara clay. The basement the nearby shelf (Bouysse et al., 1977; Jeantet, W louth of the Mana River Swamp Indented coast t I -_-- ATLANTIC OCEAN MANA RIVER C I / \ ./ \ /- / \N / Sd Receding chenier 1 f art Topstrata formed by deflation MZ 1 lat De wa rec tio an1 pai Fig.3. Schematic cross section of Galibi beach, Pointe Isère. (L( t 263 1 of 1982; Pujos et al., 1984, 1985; Pujos and Odin, At present, cheniers are still developing eral 1986) and is controlled by the Amazon River. In within the interbank zones during periods of by comparison to the muddy environment, sandy high water level (e.g near Cayenne). When ipli- material appears to be rare. more sand is removed than is deposited (e.g. at Point Isere, Fig.3) cheniers are eroded, particu- nto- The sandy coastal deposits larly during spring tides and during periods of the strong winds (January to May). rove The sandy deposits have never been studied An investigation on beaches and cheniers cies as extensively as the fine-grained sediments has been carried out in some key areas (4, and there are relatively few data available (Cayenne, Sinnamary, Marais Sarcelle and into concerning their nature, mineralogical compo- Pointe Isere) using field observations, aerial oots sition and sedimentary structures. photographs, low-altitude flights, satellite pho- ? The Holocene sandy ridges were described tographs and laboratory analysis. In each key omi- by Turenne (1978) as being 70-200 m wide, area, sand samples were collected the same day 2 on having one or two crests, and consisting of under the same tidal conditions mostly in the itet, local sands, composed of quartz and heavy foreshore area, and a few were collected from minerals.
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