Stratigraphic Architecture of a Transgressive Tidal Inlet

Journal of Coastal Research SI 39 1731 - 1736 ICS 2004 (Proceedings) Brazil ISSN 0749-0208

KULP, M.A.; FITZGERALD, D.; PENLAND, S.; MOTTI, J.; BROWN, M.; FLOCKS, J; MINER, M.; McCARTY,P., and MOBLEY, C., 2006. Stratigraphic architecture of a transgressive tidal inlet-flood tidal delta system: RaccoonPass, Louisiana. Journal of Coastal Research, SI 39 (Proceedings of the 8th International Coastal Symposium),1731 - 1736. Itajaí, SC, Brazil, ISSN 0749-0208.

Raccoon Pass is a wave-dominated, transgressive tidal inlet of the south-central Mississippi River delta plain. Itsflood-tidal delta is building into Timbalier Bay, intercepting the longshore transport of sand and reworking flooddelta deposits onshore as the shoreline translates landward. Vibracores and historical aerial photographs and mapshave been used to document its evolution and stratigraphy. These data identify a complex arrangement of lithofaciesin a dynamic setting reflecting inlet migration, spit formation, and washover deposition as a result of tidal, wave, andstorm-generated currents. Despite nearly 3-km of landward translation and the complexity of shoreline processes,Raccoon Pass has remained relatively fixed in position as a result of incision into a buried, relict, fluvio-deltaicdistributary system.

ADDITIONAL INDEX WORDS: Backbarrier deposits, Mississippi River delta, transgressive deposition.

ABSTRACT

Stratigraphic Architecture of a Transgressive Tidal Inlet-Flood Tidal DeltaSystem: Raccoon Pass, Louisiana

M.A. Kulp†; D. FitzGerald‡; S. Penland†; J. Motti†; M. Brown†; J. Flocks ; M. Miner†;P. McCarty† and C. Mobley †

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INTRODUCTION

Objectives

Data Base and Methods

Flood-tidal deltas are accumulations of sand-rich sedimenton the landward side of inlets (H , 1975). Although wavetransport and storm surges can be critically important factors intheir evolution, generating arcuate to multi-lobate shapedgeometries, deceleration of inlet-flow into backbarrier bays orlagoons is their primary mode of deposition. Spatialsegregation of tidal currents and time-velocity asymmetry oftidal flow control the landward movement of sediment and theresulting flood tidal delta morphology. Investigations of thefacies and evolution of flood-tidal deltas on mesotidal andmixed energy coasts of the eastern U.S. (H , 1975;

and 1985), and to some extent themicrotidal Texas and Florida coasts of the U.S. (e.g.,

., 1987; ., 2003) have provided important insightinto the architecture of flood-tidal deltas, and how they can bedifferentiated from related washover deposits alongtransgressive coasts and 1987).

Minimal attention however, has been given to flood-tidaldeltas of the Louisiana coast along the north-central Gulf ofMexico basin (Figure 1), despite the necessity of understandinglandward translation of barrier shorelines along this highlytransgressive setting. The lack of information concerning thesesystems likely stems from the overall turbid nature of theregional waters and microtidal conditions making them difficultto recognize. Because sand is sequestered within flood-tidaldeltas, they provide potentially important sediment resourcesfor shoreline restoration ., 2003). Moreover, theyconstitute an important component within the continuum ofdepositional processes operative along transgressive coastlinesthrough the transfer of sediment from foreshore to backshoreenvironments.

This paper focuses on the stratigraphic framework andsedimentation processes of a flood-tidal delta along a highlytransgressive segment of the microtidal, south-centralLouisiana coastal zone. Raccoon Pass is located between adeteriorating deltaic headland (Bayou Lafourche headland) andEast Timbalier Island, approximately 100-km west of the

Mississippi River Balize delta complex (Figure 1). Flood-tidaldelta deposits of Raccoon Pass are currently migrating intoTimbalier Bay as the inlet intercepts longshore transported sandand reworks former seaward flood-delta sediments onshorewithin a regime of high rates of relative sea-level rise. The goalof this paper is to identify the erosional-depositional processesoperating at Raccoon Pass.

An historical record of inlet, seafloor, and shoreline evolutionis provided by . (1994). Additional information wasgathered from aerial photography archived at the University ofNew Orleans Coastal Research Laboratory. This datasetprovides information fundamental to recognizing variability inthe tidal inlet and flood tidal delta geometry and linkingerosional and depositional history of the barrier shoreline tostratigraphic relationships that were identified in vibracores.

Stratigraphic data presented herein were collected duringthree separate summer field seasons. Preliminary work focusedon texturally characterizing and mapping sand-rich strata inTimbalier Bay for shoreline renourishment projects (K

., ), whereas subsequent fieldwork focusedspecifically on acquiring vibracores to establish thestratigraphic framework of the Raccoon Pass flood-tidal deltaand adjacent back-barrier environments. Cores from all threephases were visually described to document sedimentarystructures and stratification. Samples were taken at 30-cmintervals from the vibracores to quantify textural variabilitywith a particle-size analyzer. This system useslaser diffraction to measure the size and frequency distributionof particles between 0.4 m and 2 mm, providing a detailedrecord of mean grain size, sorting and percent sand, silt, andclay versus depth for each core. Textural classifications arebased on the Wentworth size scale 1922) andcolors are from the GSArock-color chart (1995).

Significantly, some vibracores and aerial photography post-date recent tropical cyclones (2002 storms Isidore and Lilli) thatmade landfall along the south-central Louisiana coast, allowinga direct examination of the storm-induced impacton stratigraphic relationships and the barrier-to-inletmorphology.

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†Dept. of Geology and GeophysicsUniv. New Orleans, New Orleans LA70148, [email protected]

Journal of Coastal Research Special Issue 39, 2006,

‡ Dept. of Earth SciencesBoston University, Boston MA02215, USA

� USGS Center for Coastal &Watershed Studies, St. Petersburg FL33701, USA


Kulp et al.1732

HISTORICAL EVOLUTION

STRATIGRAPHY

Mississippi River delta plain growth during the last 7,000years has been a dynamic and episodic process (e.g.1967). Progradation of deltaic headlands has alternated withheadland retreat as depocenters are abandoned, reworked, andinundated by marine waters ., 1988). The mostrecent progradational event in the vicinity of Raccoon Pass areais tied to the Bayou Lafourche distributary. Abandonment ofBayou Lafourche occurred approximately 300 yr BP,whereupon reworking and lateral dispersal of the headlandsediment, through the process of relative sea-level rise andlongshore transport, led to the development of a spit (LafourcheSpit) and barrier island system (East Timbalier) on the west,downdrift side of the headland built by the Lafourchedistributary (Figure 1).

. (2003) examined bathymetric and shorelineerosion/accretion maps for the 1880's, 1930's and 1980's from

. (1994) to determine historical trends in the evolutionand morphological development of Raccoon Pass and thedowndrift shoreline. In the 1880's the shoreline was a smooth,semi-continuous arcuate shoreline and Raccoon Pass was thelargest inlet along this shoreline segment. Width and depth ofthe pass was approximately 0.5 km and less than 1 m,respectively. The pass extended landward into anapproximately 4-km wide, shallow-water platform built offlood tidal delta and overwash deposits (Figure 2a).

A comparison of 1880's bathymetry to the 1980's shorelineindicates that early 20th century modifications to BayouLafourche strongly influenced shoreline evolution (Figure 2b).In 1904 Bayou Lafourche was dammed from the MississippiRiver, cutting off sediment supply to the downdrift spit andbarrier system ., 1985), except for sedimentderived from reworking of the Lafourche headland. Post 1930'sshoreline erosional trends reflect the influence of jettyconstruction at Belle Pass, which interrupted the westward-directed littoral transport along the Lafourche headland andresulted in a sediment-starved downdrift shoreline

., 1985). Within the last 70 years there has been a westwardelongation of the Lafourche spit as well as storm-inducedbreaching and overwash (Figure 3a). Aerial photography from1989 clearly shows a well-developed inlet and flood-tidal deltaplatform characterized by bifurcating channels, a multi-lobateform, and the presence of several swash bars on the updrift sideof the inlet (Figure 3a). The presence of inlets and breachesalong the length of the spit, most notably on the distal end, andthe presence of bayside vegetated overwash platforms suggestssubstantial shoreline modification as a result of storm impacts.Swash bars along the updrift side of the inlet at this time likelyconstricted tidal flow through the inlet channel, whichenhanced the dispersal of sediment to the backbarrier anddevelopment of the flood-tidal delta platform with morphologicsimilarity to the flood deltas of micro and mesotidal coasts(Figure 2a). In general, Raccoon Pass has progressivelyevolved into a deeper inlet as indicated by the landwardexcursion of isobaths (Figure 2b). However, in 2002 the areawas impacted by storm surges from Tropical Storm Isidore andHurricane Lilli, resulting in substantial alteration to the linkedspit-inlet system with major washover deposition behind theLafourche spit (Figure 3b). The majority of vibracorespresented in this paper predate the fall 2002 storm impacts.

Curiously, despite nearly 3 km of shoreline translation since1887, downdrift spit elongation, and multiple storm impacts,Raccoon Pass has remained in the same approximate shorelineposition relative to the adjacent barriers (compare Figure 2a to2b).

Landward translation of the Lafourche-East Timbaliershoreline suggests a dynamic sedimentation regime involvinginlet migration, spit accretion, flood -tidal delta development,and storm washover. One problem encountered by researchersof transgressive barrier stratigraphy has been the differentiationof flood tidal delta, washover, and similarly transgressivedeposits and 1987; and

2003). Because these deposits are composed ofmaterial from a common source area (sediment that has beenredistributed from the foreshore), grain-size variation of thesedeposits alone has yielded limited useful information for thedifferentiation of these facies. Moreover, the lack of significanttidal-generated stratification within flood delta deposits ofmicrotidal settings further complicates their separation.Consequently, distinguishing between these types of depositshas relied extensively upon, often subtle variation withinstratification, color, geometry, grain size and relationship tostratigraphically adjacent facies. Herein we expand upon thework of (2003) to establish the key lithofacies andtheir characteristics within an area of barrier reworkingresulting from tidal-inlet exchange and overwash.

On the basis of detailed grain size analyses, .(2003) recognized an overall coarsening upward trend for theupper 6 m of strata in the backbarrier area. The upper 6 meters isbroadly divisible into three primary units that containincreasing percentages of sand stratigraphically upward. Theseunits are further divisible into individual lithofacies, whichinclude from oldest to youngest: 1) a fluvio-deltaic facies, 2) abackbarrier facies, and 3) mixed spit/inlet, flood tidal delta, andwashover facies. In the following section we present detaileddescriptions of these facies and interpretations for their origins.

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Figure 1. Map of the Raccoon Pass study area along the south-central Louisiana coastline. Delta chronology from(1967). Boxes on lower diagram indicate core locations.

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Raccoon Pass Flood Tidal Delta 1733

The stratigraphically lowest interval (bottom of corepenetration to 2 to 3-m subseafloor encountered in vibracoresconsists of thin (<5 cm) to thick (5 to 10 cm), dark to medium-gray clay beds interbedded with lenticular, medium dark-gray,fine-grained sand. Through much of the interval discretehorizons of moderate reddish-brown oxidized clays are adistinctly different color from clay-rich intervals encountered inoverlying facies. Locally, along the northern edge of crosssection A-A' (Figure 4) and behind the western end of theLafourche spit the facies contains very fine-grained, grayishyellow to yellowish gray sand. The sand is as much as 1.5-mthick with thin but distinct horizontal to ripple crossstratification. Grayish yellow, sand-filled burrows are minimalbut present in discrete locations, whereas shells and shellfragments are generally absent. Significantly, the sand-rich,laminated strata within this interval coincide with the downdiptrend of a distributary channel that was mapped farther northusing high-resolution seismic data (Figure 1; ., 2003).Clay within this facies is similar to strata interpreted as prodeltaby . (2001) and the finely laminated sand issimilar to delta front and distributary channel-fill depositsrecognized by . (2001) along the Baratariashoreline farther east of the study area. This facies representsfluvio-deltaic deposition by distributary networks associatedwith an early phase of Lafourche delta deposition.

A1 to 2-m thick interval of light olive-gray to moderate olive-brown clay and silty to sandy clay lies gradationally above thefluvio-deltaic facies on the bayside of Raccoon Pass (Figure 4).Generally the lower contact can be identified by the appearance

of massively bedded, grayer clay compared to well-bedded andcolored clays of the underlying fluvio-deltaic facies (Figure 5).Gray, sand-filled burrows and fragmented shells are presentthroughout and large, disarticulated shells are presentlocally. Additionally, fine black organic detritus in cm-scaleconcentrations is present throughout much of the facies. On thebasis of the dark organics, extent and magnitude ofbioturbation, stratigraphic level, and predominantly clayeynature this interval is interpreted to reflect deposition in a low-energy, backbarrier environment.

Within the upper strata the laterally most continuouslithofacies forms a lens-shaped accumulation of mostly fine

sand across an area of approximately 3.5 km . From its thickestlocation, proximal to the current location of Raccoon Pass, itthins toward the north, west, and east; average thickness of theunit is approximately 1.5 m (Figure 4).

Across the study area the lower contact of the sand deposit isgenerally sharp, recognized by a sharp increase in sand and siltfrom the subjacent backbarrier facies. The facies coarsensupward from gray, sandy clay into olive gray, fine-grained sandand some clayey sand (Figure 5). On the basis of thickness,location, and relationship to stratigraphically adjacent facies,we interpret this as the Raccoon Pass flood tidal delta facies.Fragmented shells are scattered throughout the intervalbut may also be present within relatively thin (< 3-cm thick)horizons. Subtle variation in color, sand content, and volume ofshell material provides the basis for further separation of theunit into proximal and distal flood tidal delta components.

Overall, the distal facies consists of gray, sandy clay, whereasthe proximal facies is comparatively coarser grained (sand andsome clayey sand) and more shell-rich (Figure 5). Shell clastswithin the stratigraphically higher proximal flood tidal deltaunit indicate an increasing competence of tidal currents flowinginto the backbarrier as the system translates landward and theflood delta platform expands. The distal flood tidal delta faciesis often in sharp contact with the underlying backbarrier faciesand generally grades uniformly into the overlying proximalflood tidal delta facies.Clay-rich Lenticular Sand Facies

Burrowed Organic Clay Facies

Lens-Shaped Fine-Sand Facies

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Figure 2. Bathymetric change maps from . (1994).Gray dot on maps identifies the same geographic coordinate.

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Figure 3. Aerial photography of the study area in 1989 andNovember 2002 after the 2002 hurricane season.

Graded Shelly Sand Facies

Bayside-Rooted Sand Facies

DISCUSSIONS

Yellowish-gray to light olive-gray, fine-grained sandscharacterize a unit confined primarily in the inlet and downdriftzone between the Lafourche spit and East Timbalier Island.Although best observed in core RPC where it attains a thicknessof slightly more than 1 m, it is also present in cores RPB andRP6 (see Figures 1, 4 and 5). Within other cores acquired forthis study the basal contact of this sand-rich facies is difficult toseparate from the underlying sand-rich flood tidal deposits.However, a disconformable contact is subtly indicated wherecm-thick beds of fragmented and whole species arepresent. In several cores these shell-hash horizons form thebasal sediments of 0.25 to 0.5-m thick, fining-upward intervalsthat are capped by slightly finer-grained, less shell-richsediment. Sequential aerial photography of the Lafourche spitmorphology demonstrates a persistent longshore transport tothe west, providing a mechanism to introduce shoreface sandsinto the downdrift inlet. This fining upward interval containingbasal shell lags is interpreted to be the result of channeldeposition followed by downdrift spit migration and theintroduction of shoreface sediment into the tidal inlet.

On the bayside of the Lafourche spit yellowish-gray tomoderate-yellow sediment having as much as 95% sand taperstoward the north from 1.5 m to less than 0.5 m. The unit is insharp contact with the underlying clay-rich backbarrier faciesand contains numerous, very fragmented shells.Locally, the unit consists of several fining upward zones that arecapped by slightly more clay-rich, gray sand beds resemblingflood tidal delta facies. This deposit has a significantly lesseramount of fragmented shells than the underlying unit.roots and burrows provide an explanation for the generallystructureless unit, although in some cores there is subtleindication of horizontal bedding (core RP2, Figure 5).Location, geometry, rooted horizons, and stratification form thebasis for interpreting this unit as overwash deposits thatperiodically experienced shallow water or subaerial-platformconditions capable of supporting vegetation. Figures 3a and 3breveal the presence of several breaches and washover platformsalong the Lafourche spit within historical time. Aerialphotography after the extratropical cyclone activity of fall 2002clearly demonstrate a tendency for overwash of the Lafourchespit and reoccuring presence of washover deposition intoTimbalier Bay on the bayside of the spit. Historical recordsindicate that breaches along the Lafourche spit were maintainedfor at least short periods of time, before closure by depositionfrom longshore transport. Gray clayey sand, present within thewashover sediments as isolated lenses, records these closures or

peripheral flood tidal delta deposition in the back barriershadow of the spit.

Historical bathymetry, aerial photographs, examination ofshoreline accretion and erosion maps, and stratigraphicrelationships indicate a dynamic geomorphological anddepositional history for the Raccoon Pass area. Tidal inletexpansion in conjunction with overwash deposition during thistime period has led to the construction of a shallow-water,backbarrier platform composed of flood tidal delta andwashover deposits. Overall, this lens-shaped platform consistsof coarsening upward sediments. Locally, the trend isinterrupted behind the Lafourche spit by overwash deposits,which fine upward and record reduced tidal exchange as thebreaches closed. This pattern of geomorphologic evolution hascreated an overall coarsening upward sequence that records thedynamic interaction of transgressive processes as atransgressive facies mosaic overlying an earlier formed intervalrecording deltaic progradation.

Conceivably, the flood tidal delta-overwash deposits formthe base for the landward translation of the retreating shoreline.However, preservation potential of the deposits in this zone of islimited. Vibracores and high-resolution seismic profiles on thegulfside of the system reveal only horizontal reflectors of clay-rich strata ., 2002). Facies and seismic reflectorsindicative of tidal-inlet scars, buried paleo distributarychannels, or flood-tidal and washover platform deposits areabsent. Apparently the depth of erosion on the gulfside isoccurring at such high rates and extending to a depth thatprevents their preservation, despite the high rates of relative

sea-level rise (~1 cm yr ) documented along the south-centralcoastal zone.

Although this shoreline system has migrated nearly 3.0-kmshoreward within the last 100 years the position of RaccoonPass has remained relatively constant. Previous work of tidalinlet evolution has shown that antecedent geology can exert asubstantial influence on the location of tidal inlets along barriershoreline systems (e.g. and , 1973;

1979; 1995). In the relatively fine-grainedfluvio-deltaic systems of the Holocene Mississippi River deltaplain, distributary channels may contain proportionally coarser,more easily eroded sediment than the prodelta, delta front, orrestricted bay deposits they incise. Distributary systemstherefore represent a depositional dip elongated trend that ispreferentially occupied and scoured by tidal inlets. Thepresence of a seismically-imaged distributary system trendingtoward Raccoon Pass (Figure 1) coupled with stratigraphic dataindicating channel-fill below the flood tidal delta platform

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Figure 4. South-trending cross section across the Raccoon Pass flood tidal delta platform, Raccoon Pass, and Lafourche spit into the Gulfof Mexico. Location of cross section is depicted in Figure 1. Offshore surface deposits (ETD and NS) are similar to those described by

. (2003).FITZGERALD et al

Raccoon Pass Flood Tidal Delta 1735


(Figure 4) suggests that Raccoon Pass may be controlled by thisburied remnant of an earlier formed regressive event.

We thank the crew of the UNO R/V Greenhead, USGS R/VGilbert, and students of a UNO summer course for help duringfieldwork. Funding was provided by an UNO-USGScooperative study for stratigraphic framework investigations.We are grateful to Karen Westphal for providing historicalaerial photography.

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ACKNOWLEDGEMENT

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Stratigraphic Architecture of a Transgressive Tidal Inlet