programme tuesday, july, 31 - UniversitÃ© de Caen Basse Normandie

Tidalites 2012 

8th International Conference 

on Tidal Environments 

Caen, France 

July 31 - August 2 

Abstract book

Acknowledgments 

The organizing committee of Tidalites 2012 greatly thanks the following partners 

for their support: 

The research Lab UMR M2C 

The CNRS - INSU 

The APGN (Association of the Geological Heritage of Normandy) 

The University of Caen - Basse Normandie 

The University of Rouen 

The City of Caen 

The Basse Normandie Regional Council 

The Calvados Department Council 

The Geological Society of France (SGF) 

The Association of French Sedimentologists (ASF) 

We sincerely thank also the following additional partners for field trip organisation: 

University of La Rochelle, UMR LIENSs, The Charente-Maritime Department Council (FT1) 

University of Angers, BIAF lab, LaSalle Beauvais School, MNHN (FT3) 

University of Lille 1, UMR Géosystèmes, Carrière Oscar Savreux (FT4) 

University of Caen, UMR M2C, Total, MINES ParisTech, Syndicat Mixte Mont Saint Michel (FT5)

Main organizing committee 

The Tidalites 2012 conference 

is organized by the research laboratory 

“Morphodynamique Continentale et Côtière” 

(CNRS - Universities of Caen Basse Normandie and Rouen) 

Bernadette Tessier (general coordination) 

Anthony Dubois (webmaster, data base) 

Jacques Avoine, Olivier Dugué, Isabelle Neghaban, Marie-Pierre Bouet 

(financial management) 

Valérie Casado, Isabelle Neghaban (secretariat) 

Venue 

Auditorium - Musée des Beaux-Arts 

Caen Castle

PROGRAMME 

TUESDAY, JULY, 31 

Auditorium of the "Musée des Beaux-Arts", Caen Castle 

8h00 - 9h00 - Registration and Poster installation 

9h00 - 10h00 - Conference introduction 

Chairman: Daidu FAN 

10h00 - BARTHOLDY Jesper, ERNSTSEN Verner B. 

ON THE FORMATION OF RIPPLES AND DUNES 

10h20 - FLOESER Goetz, BURCHARD Hans, RIETHMUELLER Rolf 

OBSERVATIONAL EVIDENCE FOR THE INWARD TRANSPORT OF SUSPENDED MATTER BY ESTUARINE CIRCULATION IN THE 

WADDEN SEA 

10h40 - WANG Ya Ping 

SEDIMENT RESUSPENSION, FLOCCULATION AND SETTLING IN A MACROTIDAL ESTUARINE ENVIRONMENT 

11h00 - LIU James T., CHEN Wayne, C. 

SEDIMENT TRANSPORT PATTERNS AND SOURCES IN A RIVER DELTA-TIDAL FLAT COMPLEX IN TAIWAN 

11h20 - ALVAREZ Luis G., RAMIREZ Rafael 

FACTORS INFLUENCING SEDIMENT MOBILITY ON THE INTER-TIDAL FLATS OF THE UPPER GULF OF CALIFORNIA. 

11h40 - CHANG Taesoo 

BAEKSU OPEN-COAST TIDAL FLAT OF THE KOREAN WEST SEA COAST REVISITED: A DEPOSITIONAL MODEL AND ITS 

PRESERVATION POTENTIAL 

12h00 - 14h00 -Lunch at the restaurant "Café Mancel" 

Chairman: Kyungsik CHOI 

14h00 - JABLONSKI Bryce, DALRYMPLE Robert W. 

SEDIMENTOLOGY OF A FLUVIALLY DOMINATED, TIDALLY INFLUENCED POINT BAR: THE LOWER CRETACEOUS MIDDLE 

MCMURRAY FORMATION, LOWER STEEPBANK RIVER AREA, NORTHEASTERN ALBERTA, CANADA 

14h20 - PELLETIER Jonathan, ABOUESSA Ashour, DURINGER Philippe, SCHUSTER Mathieu, GHIENNE Jean-François, RUBINO Jean-Loup 

RHYTHMIC CLIMBING RIPPLES LAMINATION FROM MODERN (BAY OF THE MONT-SAINT-MICHEL, FRANCE) AND ANCIENT (DUR AT 

TALAH, PALEOGENE, LIBYA) TIDAL DEPOSITIONAL ENVIRONMENTS: DESCRIPTION, GENESIS, SIGNIFICANCE AND NEW CRITERION 

FOR TIDAL EVIDENCE. 

14h40 - REITH Geoff, DALRYMPLE Robert W., MACKAY Duncan, ICHASO Aitor 

UNDERSTANDING THE DEPOSITION OF TIDALLY DEPOSITED MUDSTONES: AN EXAMPLE FROM THE TILJE FORMATION 

(JURASSIC), OFFSHORE NORWAY 

15h00 - LEGLER Berit, JOHNSON Howard, HAMPSON Gary, MASSART Benoit, JACKSON Christopher, JACKSON Matthew, EL-BARKOOKY 

Ahmed, RAVNAS Rodmar 

FACIES MODEL OF A FINE-GRAINED, TIDE-DOMINATED DELTA: LOWER DIR ABU LIFA MEMBER (EOCENE), WESTERN DESERT, 

EGYPT 

15h20 - QUIJADA I. Emma, SUAREZ-GONZALEZ Pablo, BENITO M. Isabel, MAS Ramón 

TIDE-INFLUENCED FLUVIAL-DELTAIC SEDIMENTS VERSUS CONTINENTAL SANDY-MUDDY FLAT DEPOSITS: EVIDENCE FROM THE 

HUERTELES FM (EARLY CRETACEOUS, N SPAIN) 

15h40 - LONGHITANO Sergio, CHIARELLA Domenico, SPALLUTO Luigi 

TIDAL FACIES IN SILICICLASTIC, CARBONATE AND MIXED MICROTIDAL ANCIENT SYSTEMS OF SOUTHERN ITALY 

Coffee break and poster session 

Chairman: Jesper BARTHOLDY 

17h00 - MARGOTTA José, TRENTESAUX Alain, TRIBOVILLARD Nicolas, ABRAHAM Romain 

FRENCH FLANDERS FIELDS: DECIPHERING THE HOLOCENE SEDIMENTARY HISTORY OF THE COASTAL PLAIN OF NORTHERN 

FRANCE 

17h20 - JOHANNESSEN Peter N., NIELSEN Lars Henrik, MØLLER Ingelise, NIELSEN Lars Henrik, ANDERSEN Thorbjørn Joest, PEJRUP 

Morten 

THE SEDIMENTARY DEVELOPMENT OF A HOLOCENE TO RECENT BARRIER ISLAND, DANISH WADDEN SEA 

17h40 - FRUERGAARD Mikkel, ANDERSEN Thorbjørn Joest, NIELSEN Lars Henrik, JOHANNESSEN Peter N., PEJRUP Morten 

EVOLUTION AND STRATIGRAPHY OF A HOLOCENE MICRO-TIDAL BARRIER SYSTEM IN THE NORTHERN WADDEN SEA 

18h00 - WANG Yunwei, YU Qian, GAO Shu 

EFFECTS OF GRAIN-SIZE SORTING ON THE SCALE-DEPENDENCES OF EQUILIBRIUM MORPHOLOGY OF BACKBARRIER TIDAL 

BASINS 

18h30 - 20h00 - Conference cocktail

WEDNESDAY, AUGUST, 01 


Chairman: Burghard FLEMMING 

08h30 - TRENTESAUX Alain, ABRAHAM Romain, BAFFREAU Alexandrine, DAUVIN Jean-Claude, LOZACH Sophie, MALENGROS Deny, 

POIZOT Emmanuel 

MARINE HABITAT CLASSIFICATION: A PLURIDISCIPLINARY APPROACH IN A HIGH MACROTIDAL ENVIRONMENT. THE CASE OF THE 

ENGLISH MEDIAN CHANNEL 

08h50 - DAUVIN Jean-Claude, BERYOUNI Khadija, LOZACH Sophie, MEAR Yann, MURAT Anne, POIZOT Emmanuel 

LIVE UNDER TIDAL REGIME: THE ROLE OF THE BRITTLE-STAR OPHIOTHRIX FRAGILIS BEDS FROM THE EASTERN BAY OF SEINE IN 

THE FINE PARTICLE DEPOSIT-SUSPENSION MECHANISMS 

09h10 - BARTHOLOMAE Alexander, HOLLER Peter 

ANALYSIS OF SUBTIDAL HABITATS IN THE GERMAN WADDEN SEA ON THE BASE OF HYDRO-ACOUSTIC REMOTE SENSING DATA 

09h30 - BAUCON Andrea, FELLETTI Fabrizio 

A QUANTITATIVE TOOL FOR THE ICHNOLOGICAL ANALYSIS OF TIDAL ENVIRONMENTS: THE ICHNOGIS METHOD 

09h50 - VALERIUS Jennifer, MILBRADT Peter, VAN ZOEST Michael, ZEILER Manfred 

DEVELOPMENT OF A SEABED MODEL FOR ANALYZING SEDIMENT AND MORPHODYNAMIC PROCESSES IN THE GERMAN BIGHT 

(NORTH SEA) 


Chairman: Robert W. DALRYMPLE 

11h00 - ARCHER Allen 

COMPARISON OF HYPERTIDAL SYSTEMS IN EUROPE, SOUTH AND NORTH AMERICA 

11h20 - FURGEROT Lucille, MOUAZE Dominique, TESSIER Bernadette, HAQUIN Sylvain, PEREZ Laurent, VIEL Félix 

INFLUENCE OF THE TIDAL BORE ON SEDIMENT TRANSPORT IN THE MONT-SAINT-MICHEL ESTUARY, NW FRANCE. 

11h40 - FAN Daidu, SHANG Shuai, TU Jinbiao, CAI Guofu, WU Yijing 

SEDIMENTATION PROCESSES AND SEDIMENTARY CHARACTERISTICS OF TIDAL BORES IN THE QIANTANG ESTUARY, 

EAST-CENTRAL CHINA 

12h00 - CHAMIZO BORREGUERO M., MELENDEZ N., DE BOER Poppe 

TIDAL BORE INDUCED SEDIMENTS IN INCISED VALLEYS, UTRILLAS FM, ALBIAN, SW IBERIAN RANGES, SPAIN 

12h20 - DE BOER Poppe 

MILANKOVITCH-SCALE ORBITALLY FORCED TIDAL CYCLICITY 

12h40 - 14h30 -Lunch at the restaurant "Café Mancel" 

Chairman: Eric CHAUMILLON 

14h30 - GONG Wenping 

ASSESSMENT OF SILTATION AT THE DREDGED CHANNEL IN THE HUANGMAOHAI ESTUARY, PEARL RIVER DELTA, CHINA 

14h50 - GLUARD Lucile, LEVOY Franck 

THE 18.6 YEAR TIDAL CYCLE INFLUENCE ON THE COUESNON RIVER BEHAVIOUR, MONT-SAINT-MICHEL BAY (FRANCE) 

15h10 - CHOI Kyungsik, HONG Chang Min, OH Chung Rok, JUNG Jae Hoon 

MORPHODYNAMICS OF TIDAL CHANNELS IN THE MACROTIDAL YEOCHARI TIDAL FLAT, GYEONGGI BAY, WEST COAST OF KOREA: 

IMPLICATION FOR THE ARCHITECTURE OF INCLINED HETEROLITHIC STRATIFICATION 

15h30 - HERRLING Gerald, WINTER Christian 

THE EFFECT OF HIGH-ENERGY EVENTS ON EBB-TIDAL DELTA SEDIMENTOLOGY AND MORPHOLOGY – A PROCESS-BASED MODEL 

STUDY 

15h50 - FERRET Yann, LE BOT Sophie, LAFITE Robert, BLANPAIN Olivier, GARLAN Thierry 

INFLUENCE OF TIDE VS WAVE ON SEDIMENT DYNAMICS AND DUNE INTERNAL ARCHITECTURE ON A MACROTIDAL INNER 

CONTINENTAL SHELF (EASTERN ENGLISH CHANNEL). 


Chairman: Poppe DE BOER 

17h00 - YU Qian 

MODELING THE FORMATION OF A SAND BAR WITHIN A LARGE FUNNEL-SHAPED, TIDE-DOMINATED ESTUARY: QIANTANGJIANG 

ESTUARY, CHINA 

17h20 - CHAUMILLON Eric, FENIES Hugues, BILLY Julie, BREILH Jean-François 

TIDAL AND CLIMATE CONTROLS ON THE MORPHOLOGICAL EVOLUTIONS AND THE INTERNAL ARCHITECTURE OF A TIDAL BAR: 

THE PLASSAC TIDAL BAR IN THE BAY-HEAD DELTA OF THE GIRONDE ESTUARY. 

17h40 - SAITO Yoshiki 

MONSOON-CONTROLLED DELTAIC SEDIMENTATION IN A TIDE-DOMINATED SETTING: EXAMPLES FROM MEGA-DELTAS IN ASIA 

18h00 - MASSUANGANHE Elidio, BANDEIRA Salomao, WESTERBERG Lars-Ove 

IMPACTS OF FLOODS AND CYCLONES ON MANGROVE OVER A SECTOR OF THE SAVE RIVER DELTA PLAIN, MOZAMBIQUE. 

18h20 - MAKINO Yasuhiko, ARAI Shota, ITO Takashi, NANAYAMA Futoshi 

EFFECT OF THE 2011 GIANT TSUNAMI ON A SANDY BEACH AT OARAI, EASTERN JAPAN 

18h45 - Departure from the conference place for the Conference Dinner (by bus)

THURSDAY, AUGUST, 02 


Chairman: Jean-Yves REYNAUD 

08h30 - CHOI Kyungsik, JUNG Jae Hoon, JO Joo Hee 

RAPID INFILLING OF MACROTIDAL ESTUARY DURING EARLY HOLOCENE IN YEOCHARI TIDAL FLAT, GYEONGGI BAY, WEST COAST 

OF KOREA 

08h50 - KITAZAWA Toshiyuki 

TIDAL RAVINEMENT SURFACE IN A TIDE-DOMINATED ESTUARY: PLEISTOCENE NHA BE ESTUARY, SOUTHERN VIETNAM. 

09h10 - EKWENYE Ogechi, NICHOLS Gary, NWAJIDE Sunny, OBI Gordian 

DEPOSITIONAL ARCHITECTURE AND ICHNOLOGY OF THE TIDALLY-INFLUENCED ESTUARINE SYSTEM OF THE EOCENE AMEKI 

GROUP 

09h30 - DALRYMPLE Robert W., JAMES Noel, SEIBEL Meg, BESSON David, PARIZE Olivier 

WARM-TEMPERATE, MARINE, CARBONATE SEDIMENTATION IN AN EARLY MIOCENE, TIDE-DOMINATED, INCISED VALLEY; 

PROVENCE, SE FRANCE 

09h50 - ILGAR Ayhan, TIMUR Erol, KARAKUS Erhan, KAYA Serap, TURKMEN Banu 

LATE MIOCENE INCISED VALLEY-FILL IN EASTERN TAURIDES, TURKEY: DEPOSITIONAL EVOLUTION IN RESPONSE TO SEA-LEVEL 

CHANGE AND DEPOSITIONAL PROCESSES 


Chairman: Yoshiki SAITO 

11h00 - YIN Yong 

THE LATE PLEISTOCENE–HOLOCENE STRATIGRAPHY AND SEDIMENTARY ENVIRONMENT OF THE TIDAL RADIAL SAND RIDGE 

SYSTEM, JIANGSU OFFSHORE, SOUTH YELLOW SEA 

11h20 - MICHAUD Kain, DALRYMPLE Robert W. 

TRANSGRESSIVE, HEADLAND-ATTACHED TIDAL SAND RIDGES IN THE RODA FORMATION, NORTHERN SPAIN 

11h40 - PELLETIER Jonathan, ABOUESSA Ashour, DURINGER Philippe, SCHUSTER Mathieu, RUBINO Jean-Loup 

THE GEOLOGICAL RECORD OF TIDAL DYNAMIC: DIVERSITY OF ASSOCIATED DEPOSITS AND MULTI-SCALE CYCLES FROM THE 

DUR AT TALAH FORMATION (UPPER EOCENE, SIRT BASIN, LIBYA) 

12h00 - CHOI Kyungsik, STEEL Ronald, OLARIU Cornel 

TIDAL RHYTHMITES IN THE UPPER CRETACEOUS NESLEN FORMATION, UTAH, USA: THEIR IMPLICATIONS FOR THE 

SEDIMENTOLOGY AND STRATIGRAPHIC ARCHITECTURE OF TIDAL-FLUVIAL CHANNEL 

12h30 - 14h00 Lunch at the restaurant "Café Mancel" 

Chairman: Allen ARCHER 

14h30 - WEILL Pierre, MOUAZE Dominique, TESSIER Bernadette 

INTERNAL ARCHITECTURE AND EVOLUTION OF BIOCLASTIC BEACH RIDGES IN A MEGATIDAL CHENIER PLAIN: WAVE FLUME 

EXPERIMENTS AND FIELD DATA 

14h50 - REYNAUD Jean-Yves, RUBINO Jean-Loup, PARIZE Olivier, DALRYMPLE Robert W., VENNIN Emmanuelle, FERRANDINI Michelle, 

FERRANDINI Jean, ANDRE Jean-Pierre, TESSIER Bernadette, JAMES Noel 

OFFSHORE TIDAL BIOCLASTIC BODIES IN EPEIRIC SEAS: MIOCENE EXAMPLES FROM SE FRANCE AND CORSICA 

15h10 - FLEMMING Burghard W. 

THE ORDOVICIAN TABLE MOUNTAIN GROUP, SOUTH AFRICA: THE TIDAL DEPOSIT THAT NEVER WAS 

15h30 - SUAREZ-GONZALEZ Pablo, QUIJADA I. Emma, BENITO M. Isabel, MAS Ramón 

DO STROMATOLITES NEED TIDES TO TRAP OOIDS? INSIGHTS FROM THE COASTAL-LAKE CARBONATES OF THE LEZA FM (EARLY 

CRETACEOUS, N SPAIN). 

15h50 - ILGAR Ayhan, KARAKUS Erhan, ESIRTGEN Tolga 

THE VARIABILITY OF ESTUARINE DEPOSITS IN A MICROTIDAL SETTING OF LATE MIOCENE MEDITERRANEAN (EASTERN TAURIDES, 

TURKEY): CONTROLLING FACTORS ON DEPOSITION 

Last coffee break and poster session

POSTERS 

BARRIOS Edixon Jose 

SEDIMENTOLOGICAL MODEL FOR C-4 RESERVOIR FROM VLA6/9/21 AREA, BASED ON INFORMATION OF CORE INTERPRETATION AND 

COMPARISON WITH THEORETICAL MODELS DEPOSITED UNDER SIMILAR SEDIMENTOLOGICAL CONDITIONS 

BAUCON Andrea, FELLETTI Fabrizio 

“DEEP TIME ON A TIDAL FLAT”: THE ANCESTRAL ICHNOASSOCIATIONS OF THE MODERN GRADO LAGOON (NORTHERN ADRIATIC, ITALY) 

CHANG Taesoo, KIM Jincheol, YOO Dong-Geun 

LATE QUATERNARY STRATIGRAPHIC EVOLUTION OF BAEKSU OPEN-COAST TIDAL FLAT, WEST COAST OF KOREA: REGIONAL 

UNCONFORMITY-BOUNDED TWO TIDAL DEPOSITS 

DIEZ-CANSECO Davinia, BENITO M. Isabel, DIAZ-MOLINA Margarita, KALIN Otto 

TIDAL INFLUENCE IN THE ‘LOWER RED UNIT’ OF THE TREMP FM IN SOUTH-CENTRAL PYRENEES (LATE CRETACEOUS-TERTIARY) 

GUGLIOTTA Marcello, FLINT Stephen, HODGSON David, VEIGA Gonzalo 

SEDIMENTOLOGY AND SEQUENCE STRATIGRAPHY OF THE FLUVIAL-TO-TIDAL TRANSITION ZONE IN THE UPPER LAJAS FORMATION 

(NEUQUEN BASIN, ARGENTINA) 

HUSTELI Berit, JENSEN Maria, OLAUSSEN Snorre 

TIDALLY RELATED HETEROGENITIES IN SANDBODIES SOUGHT PARAMETERIZED FOR REFINED RESERVOIR MODELLING 

JAMET Guillaume, DUGUE Olivier, DELCAILLAU Bernard, CLIQUET Dominique 

THE TIDALLY-INFLUENCED RIVER DEPOSITS OF THE PLEISTOCENE SEINE SYSTEM: THE EXAMPLE OF THE TOURVILLE-LA-RIVIERE 

TERRACE (NW FRANCE) 

KURCINKA Colleen, ICHASO Aitor, DALRYMPLE Robert W. 

TIDAL DELTAS IN THE LAJAS AND TILJE FORMATIONS: TIDE-DOMINATED OR TIDE-INFLUENCED? 

LE BOT Sophie, BERTEL F, LANGLOIS Estelle, FOREY Estelle, MEIRLAND Antoine, LAFITE Robert 

LITTORAL SEDIMENTATION WITHIN SPARTINE AND OBIONE COMMUNITIES IN THE SOMME ESTUARY (EASTERN ENGLISH CHANNEL). 

PRELIMINARY RESULTS 

LEMOINE Maxence, DELOFFRE Julien, LAFITE Robert, LESOURD Sandric, LESUEUR Patrick, CUVILLIEZ Antoine, FRITIER Nicolas, MASSEI 

Nicolas 

RHYTHMITES PRESERVATION IN MACROTIDAL ESTUARINE ENVIRONMENTS: FROM UPSTREAM TO DOWNSTREAM ESTUARY 

LOZACH Sophie, ABRAHAM Romain, BAFFREAU Alexandrine, DAUVIN Jean-Claude, MALENGROS Deny, POIZOT Emmanuel, TRENTESAUX 

Alain 

BENTHIC HABITAT DIVERSITY IN COARSE SEDIMENT UNDER HIGH MACROTIDAL ENVIRONMENT 

MAKINO Yasuhiko 

SEDIMENTATION OF THE 2011 GIANT TSUNAMI ON A SANDY BEACH ON THE PACIFIC COAST OF EASTERN JAPAN 

PARK Soo Chul 

LATE QUATERNARY STRATIGRAPHY AND MORPHODYNAMICS OF MACROTIDAL SAND BODIES IN THE WESTERN COAST OF KOREA 

ROSSI Valentina, STEEL Ronald, OLARIU Cornel, LEVA LOPEZ Julio 

COMPOUND TIDAL DUNES IN THE NEUQUEN JURASSIC RIFT BASIN 

SCASSO Roberto, CUITIÑO José Ignacio, DOZO Teresa, BOUZA Pablo 

MEANDERING TIDAL CHANNEL DEPOSITS IN THE FLUVIAL-TIDAL TRANSITION OF A MIOCENE ESTUARY IN PATAGONIA 

SON Chang Soo, BARTHOLOMAE Alexander, FLEMMING Burghard W., CHUN Seong Soo, LEE In Tae 

THE VARIATION OF THE SEDIMENTARY FACIES ON JADEBUSEN TIDAL BASIN IN GERMANY: SURFACE SEDIMENTS AND SEDIMENTARY 

STRUCTURES 

TANAKA Akiko 

COASTAL MONITORING USING L-BAND SYNTHETIC APERTURE RADAR (SAR) IMAGE DATA IN THE MEKONG AND HUANGHE (YELLOW 

RIVER) DELTA AREAS 

TESSIER Bernadette, BILLEAUD Isabelle, SORREL Philippe 

SEDIMENTARY RECORDS OF CLIMATE CHANGES IN MACROTIDAL TIDE-DOMINATED ESTUARIES 

VREL Anne, BOUST Dominique, LESUEUR Patrick, COSSONNET Catherine, DELOFFRE Julien, DUBRULLE-BRUNAUD Carole, MASSEI 

Nicolas, ROZET Marianne, SOLIER Luc, THOMAS Sandrine 

TIDAL ASYMMETRY: THE USE OF ARTIFICIAL RADIONUCLIDES IN SEDIMENTS (THE SEINE ESTUARY, FRANCE) 

WANG Dong, SONG Shengli, DING Hao, WU Jichun, ZHU Qingping, WANG Ling 

HYDROLOGIC CHARACTERISTICS OF THE YELLOW RIVER MOUTH, CHINA 

ZHANG Jicai, HUGHES Joseph, WANG Ping, HORWITZ Mark 

THE VARIATIONS OF SALINITY AND STRATIFICATION FOR MICRO-TIDAL AND MANGROVE-COVERED FROG CREEK SYSTEMS, FLORIDA

ABSTRACTS

Tidalites 2012, 8th International Conference on tidal environments, Caen, France – Abstract book 

FACTORS INFLUENCING SEDIMENT MOBILITY ON THE INTER-TIDAL FLATS OF 

THE UPPER GULF OF CALIFORNIA 

Luis G. ALVAREZ, Rafael RAMIREZ 

CICESE, Carretera Ensenada-Tijuana no. 3918, Zona Playitas, 22860, Ensenada, Mexico, 

lalvarez@cicese.mx 

The northwest end of the Gulf of California, north of 31º N, is known as the Upper Gulf of 

California (UGC). It is a semi-enclosed shallow basin, surrounded by arid alluvial plains and 

piedmont deposits. This high-energy macro-tidal sea has semi-diurnal tides with range 7-8 m 

during springs, and currents 1-3 m/s. Damming and diversion of the Colorado River have 

reduced freshwater and sediment supply to the UGC by more than 95% for over a century. On 

the west coast, an extensive coastal plain of tidal flats extends from high tide to about 12 below 

mean sea level. The intertidal flats are drained by numerous dendritic, linear, and even 

meandering channels. Sediments are mainly reddish-brown mud. Sand is restricted to intertidal 

sand flats, tidal channels and a narrow belt of steep beaches ((Thompson, 1969; Schreiber, 1969; 

Meckel, 1975; Baba, et al., 1991). 

Currents, tides, sediment properties and suspended sediment were measured on the 

intertidal flats during five short-term (1-3 days) time series in 2001 and 2008-2011. The aim was 

to identify for the first time the processes that dominate sediment transport. 

During spring tides, exposed intertidal flats are more that 5 km wide at the northwestern 

end of the UGC, decreasing to widths of ~1 km at the southern part, where the observations 

were made. The main morphological elements at the observation site are low-relief (


Study site. 

2


COMPARISON OF HYPERTIDAL SYSTEMS IN EUROPE, SOUTH AND NORTH 

AMERICA 

Allen ARCHER 

KANSAS STATE UNIVERSITY, Department of Geology, 66506, Kansas, Us, aarcher@ksu.edu 

Hypertidal ranges exceed 6 m and can range upwards to 15 m and potentially higher. 

Herein a comparison is made among systems that have the highest recognized tidal ranges on 

Earth. Settings in Europe include Bristol Bay and the Severn River estuary, southwestern UK 

and Mont-Saint-Michel Bay in Normandy, France. In South America, hypertidal ranges occur 

within tidal estuaries of Patagonia (southeastern portion of the Atlantic coast of Argentina). In 

North America hypertidal systems include: Turnagain Arm within Cook Inlet in south-central 

Alaska, USA, Leaf Lake in Ungava Bay, northern Quebec, Canada and the Salmon River estuary 

in the Bay of Fundy, Nova Scotia, Canada. 

When compared to micro-, meso- or macrotidal coasts, hypertidal systems are extremely 

rare. Hypertidal systems, however, do have enormous tidal ranges coupled with a tremendous 

potential for high rates of sedimentation and erosion. A complete understanding of the dynamics 

of these extreme systems is important for at least two reasons. First, they serve as modern 

analogs for ancient systems that were formed with extremely dynamic tidal systems. In addition, 

from a more pragmatic standpoint, tidal power is a relatively untapped nonpolluting and 

renewable source of energy. Currently operational tidal-power stations have been constructed 

entirely within hypertidal coastal settings. It is highly plausible that future developments will also 

be concentrated in hypertidal coastal settings. 

3


4


SEDIMENTOLOGICAL MODEL FOR C-4 RESERVOIR FROM VLA6/9/21 AREA, 

BASED ON INFORMATION OF CORE INTERPRETATION AND COMPARISON WITH 

THEORETICAL MODELS DEPOSITED UNDER SIMILAR SEDIMENTOLOGICAL 

CONDITIONS 

Edixon Jose BARRIOS 

PDVSA, Calle 77 Edificio 5 de Julio, 4002, Las Laras, Venezuela, barrioseg@pdvsa.com 

Sedimentary environments defined for a specific reservoir, are the result of the 

interpretation of data extracted from cores, cut in intervals with economic interest specifically on 

VLA6/9/21 area C-4 and C- 5 reservoirs from Misoa Formation have been studied and sitted 

with the models built in neighboring areas. A well sedimentological model will be the result of 

geological and coherent integration of information provided by cores and channel samples and / 

or wall, biostratigraphy, well logs, information about deepmeters and image logs and even 

engineering reservoir and then checked against all the models, which in turn will serve as input 

for the construction of other models such as geostatistics and simulation. 

Throughout history, Geologists in pro of creating a model according to the reality of 

reservoir, they have been required to propose models with poor or not information about cores 

and when they exist, in some cases with poor data or it´s has been recovered in sandy sections 

only. 

In recent studies in the area VLA6/9/21 was achieved taking into account the core data 

technically to support possible tidal influence for this reservoir in based of the presence of 

sedimentary structures, biostratigraphy and with the comparison with others model was proposed 

a model with deltaic sedimentation and tidal influences for the units C-4 and C5 based on the 

identification and recognition of distinctive features such as double-layer structures of clay, cone 

cone structure, pairs of clay, together with other data will be the ideal complement to think that the 

area at some point in geological time was under the influence of sedimentary processes 

associated with tides. In other way, several studies have mentioned possible presence of an 

estuary as a sedimentary behavior as responsability of sedimentation. It´s important to highlight 

that an estuary extends from the maximum bound of tidal influence zone to maximum bound of 

coastal processes influence of mouth, In some cases, it´s so difficult to difference where the 

fluvial action begins and where ends. 

An estuary is defined as a coastal body of water semi-closed connected to open sea and 

inside which there are water mixtures of different salinities, from the sea and the continent; 

enough reason to avoid defining sedimentary environments of a region without having enough 

information. If we consider that this area represent only a little part about all basin and in the 

same way the answer of well log it´s show us heterogeneities in all of them, It´s neccesary to 

highlight that Misoa Formation involve episodes of complex sedimentation, where is so difficult to 

recognize and identify a sedimentological model without uncertainty. 

Complex systems like this are so linked and depend on the transgressive periods because 

if in a delta occurs a transgression it´s could become an estuary, Similarly, falls in the eustatic 

level in an estuary, will make it a prograding system (under certain parameters such as rate 

accommodation, sediment supply, etc) therefore would be having like a delta. 

5


Escalona, A. and Mann, P. Sequence-stratigraphic, analisys of Eocene clastic foreland basin deposits in 

central Lake Maracaibo using high-resolution well correlation and 3D seismic data: AAPG, April 2006, v 90, 

N°-4. 

Galloway, W. and Hobday, D. Terrigenous clastic depositional system, Springer-Verlag, Berlin 1996. 

Galloway, W,.Genetic stratigraphic sequences in basic analysis: I Arquitecture and genesis of flodding 

surface bounded depositional units:, AAPG Bulletin, February 1989. 

Gonzalez de Juana, C., J. Azorena y X. C. Picard (1980) Geología de Venezuela y de sus cuencas 

petrolíferas, Foninves, Caracas. 

Pettijohn, F.; Potter, P.; Siever, R. Sand and Sandstones. 1987, Springer- Verlag, New York, Inc., 2th 

edition. 

6


ON THE FORMATION OF RIPPLES AND DUNES 

Jesper BARTHOLDY, Verner B. ERNSTSEN 

GEOLOGICAL SURVEY OF DENMARK AND GREENLAND, Oester Voldgade 10, 1350, Copenhagen, 

Denmark, jb@geo.ku.dk 

Ripples and dunes are commonly distinguished on the basis of their scaling or not-scaling 

with flow depth as well as dimensional criteria such as wavelength. Ripples are regarded as 

independent of water depth while dunes are generally considered to scale with depth. The simple 

fact that compound dunes exist contradicts the depth-scaling argument. If the largest compound 

dunes scale with water depth, where does that leave the smaller, superimposed ones? And, if 

these scale with water depth, how can the compound dunes be orders of magnitude larger? To 

overcome this contradiction, it has sometimes been argued that the smaller superimposed dunes 

scale with boundary layers related the larger compound bedforms, also this can be disproved by 

means of examples, e.g lower right of Fig. 1 where the large compound features are missing. 

Numerous experiments in small laboratory flumes the world over have demonstrated that 

ripples are not always independent of water depth. In terms of their size, all flow-transverse 

bedforms generated in small demonstration flumes with depths < 0.1 m are by definition ripples in 

spite of the fact that they clearly scale with water depth, as revealed by contracting water surfaces 

over their crests. As a consequence, the criteria by which ripples and dunes are supposed to be 

distinguished are inherently suspect. Fact is that if flow depth is small enough, any bedform will 

scale with it, simply because depth limitation forms a natural upper boundary, and serves as an 

upper limit for bedform growth of any kind. In research flumes, the maximum water depth is 

typical less than 0.5 m. As a result, dune heights will remain smaller than about 15 cm. It is 

therefore not surprising that the largest bedforms in flume studies are always found to scale with 

flow depth. By contrast, dunes observed on the ocean floor at depths of 10s-1000s of meters 

exhibit a wide range of sizes. These must evidently be controlled by factors other than water 

depth. The only meaningful explanation is that dunes are scaled with the mutual relationship 

between flow conditions and form response. These matters are examined on the basis of theory 

and experiments, and it is demonstrated that bedforms result from self-organizing processes 

acting across the interface between sand and water forming boundary layers directly dependent 

on bedform height. 

7


Multibeam registration of bedforms in the tidal inlet Knudedyb on the Danish west coast. The colors indicate 

the approximate water depth relative to the mean water level. The tidal range in the inlet is 1.7 m. The 

mean grain-size in the center of the channel varies from a maximum of about 0.650mm at the bedform 

crest to a minimum of about 0.200 mm in the troughs. 

8


ANALYSIS OF SUBTIDAL HABITATS IN THE GERMAN WADDEN SEA ON THE 

BASE OF HYDRO-ACOUSTIC REMOTE SENSING DATA 

Alexander BARTHOLOMAE, Peter HOLLER 

SENCKENBERG, Suedstrand 40, 26382, Wilhelmshaven, Germany, abartholomae@senckenberg.de, 

peter.holler@senckenberg.de 

Since the Wadden Sea area was awarded a World Nature Heritage the public pressure of 

habit protection grows distinctly. The European Water Framework Directive requires a standard 

mapping of marine habitats. Therefore quality tools to assess the recent stage and to monitor 

changes in the near future are needed. For the intertidal area airborne laserscanning and 

Synthetic Aperture radar (SAR) are the state of art (Bartholdy & Folving 1986, Brzank et al. 2008). 

In contrast to the intertidal area, optical approaches are less successful to cover the subtidal part 

of the Wadden Sea area. High suspension load coupled with less visibility reduce and /or inhibit 

wide-spread used optical based techniques. To compensate this deficit, alternative techniques 

have to be developed. From the pelagic area the quite well-known hydro-acoustic devices are 

now more and more adapted to shallow water operation (Hughes-Clarke et al. 1996). 

To work out standard procedures for sub-aquatic monitoring, three hydro-acoustic devices 

were tested to their resolution, their redundancy and their value of benefit detecting habitats in a 

three year lasting case study in the East Frisian Wadden Sea (Bartholomae et al 2011). In order 

to find out which are the system-specific limitations like foot-print sizes and coverage, seven test 

areas in water depths between 5 m to 15 m were simultaneously surveyed using singlebeam 

echosounder (SBS) (200 kHz), multibeam echosounder (MBES) (455 kHz) and Sidescan sonar 

(SSS) (380 kHz). Based on the principle of acoustic respond the return signals were analysed 

with acoustic seabed classification tools to determine the different characteristics of seafloor 

roughness. Up to five major acoustic classes have been specified. These classes cover sea 

surface sediments consisting of sand, shells debris, gravel, less mud and infrequently some peat 

at the seven study sites in the East Frisian backbarrier tidal flats. Repetitive surveys were carried 

out to investigate system specific variations and natural changes in the complex spatial pattern of 

the subtidal habitats. Based on the given technical specifications of the different acoustic devices 

the influence of footprint sizes was tested by applying different grid sizes in the data analysis. In 

order to generate similar footprint sizes for a water depth of 15m MBES data were calculated on a 

grid sizes of 33x17 pixel (0.9m x 3.7m ; 3.3 m²), SSS data with 17x9 pixels (0.8m x 2.4m ; 

1.92m²) which correspond to a SBS footprint of 2.98 m². This already limits the minimum water 

depth of operation for the oblique-angled geometries. 

The spatial distribution of the acoustic classes was tested by means of confidence levels of 

acoustic similarities within the classification results of each system as well as between the 

different acoustic devices. The fit of ground truth data to acoustic classes and the importance of 

the sediment specific surface roughness was tested by multidimensional scaling (MDS) and 

cluster analysis for bulk sediment composition and for the individual grain size distributions. 

Seasonal up to annual scaled times series were analysed with regard to habitat dynamics in 

exposed and sheltered areas of the Wadden Sea. 

The results of the case study are summarized in a comprehensive report which discusses 

the differences in backscatter based classification, local effects of natural and human impact to 

the specific sites and the system specific differences such as working-frequencies and footprint 

geometry. 

In general the backscatter based systems are much more sensitive to changes in surface 

roughness than of the sediment type itself. For the sediments in the Wadden Sea this sensitivity 

starts getting more relevant in dependence of the footprint size, the effect of smoothing decreases 

in shallower water depth. 

Results of habitat distributions and their site dependent differences and the system related 

limitation will be discussed in a condensed way. 

9


Ground truthing results for the classification of multi-beam echosounder data (5 classes) from the location 

Otzumer Balje 

Bartholdy, J. and Folving, S. 1986. Sediment classification and surface type mapping in the Danish 

Wadden Sea by remote sensing. Netherlands Journal of Sea Research, 20 (4), 337-345. 

Bartholomä, A., Holler, P., Schrottke, K. and Kubicki, A. (2011) Acoustic habitat mapping in the German 

Wadden Sea – Comparison of hydro-acoustic devices. J. Coast. Res.,Spec. Iss. 64, ICS 2011 Proc., 1-5. 

Brzank, A., Heipke, Ch., Goepfert, J. and Soergel, U., Aspects of generating precise digital terrain models 

in the Wadden Sea from lidar–water classification and structure line extraction. Journal of Photogrammetry 

and Remote Sensing, 63 (5), 510-528. 

Hughes-Clarke, J.E., Mayer, L.A. and Wells, D.W., 1996. Shallow water imaging multibeam sonars: A new 

tool for investigating seafloor processes in the coastal zone and on the continental shelf. Marine 

Geophysical Research, 18, 607-629. 

10


“DEEP TIME ON A TIDAL FLAT”: THE ANCESTRAL ICHNOASSOCIATIONS OF THE 

MODERN GRADO LAGOON (NORTHERN ADRIATIC, ITALY) 

Andrea BAUCON, Fabrizio FELLETTI 

DIPARTIMENTO DI SCIENZE DELLA TERRA, Università di Milano, 20133, Milano, Italy, 

andrea@tracemaker.com 

The Northern Adriatic Sea is a shallow, semi-enclosed sea lying on continental crust, being 

an ideal model for past epicontinental seas (Fig. 1A). In addition, recent studies suggests that its 

benthic subtidal ecosystem closely resembles Paleozoic-style ecology (McKinney, 2003, 2007; 

McKinney and Hageman, 2006). Although some objections were raised on the mentioned 

ecological aspects (Zuschin and Stachowitsch, 2009), the Northern Adriatic Sea is unanimously 

considered one of the few modern epicontinental seas comparable to some Paleozoic–Mesozoic 

shelves (McKinney, 2003, 2007; McKinney and Hageman, 2006; Zuschin and Stachowitsch, 

2009). 

The Grado-Marano lagoon is the northernmost transitional system of this peculiar 

geobiologic scenario. Here, barrier-island systems with vast tidal flats support a complex mosaic 

of sedimentary environments, which offer varied habitats for tracemaking organisms (Baucon, 

2008). Intriguingly, the intertidal flats are characterized by ancestral bioturbation styles coexisting 

with modern, Thalassinoides-dominated ones: 

• Microbial mat ichnoassociation. Intertidal microbial mats are characterized by horizontal, 

gently winding burrows without branching (Helminthoidichnites; tunnel diameter: 1 mm). These 

traces accurately follow the interface between the organic-rich and the mineral-rich layer of 

microbial mats (Fig. 1B). The observed Helminthoidichnites reflect the mining of the microbial mat 

from underneath: ‘undermat mining behaviour’ sensu Seilacher (1999). Similar behavioural 

strategies were particularly common within Proterozoic microbial mats, before of the Agronomic 

Revolution (Seilacher, 1999). Obviously, the Helminthoidichnites from Grado correspond to 

Proterozoic-style behaviour but the tracemakers are modern: insect larvae (undetermined 

Diptera). Intertidal insects (Heterocerus flexuosus) are also the authors of Macanopsis, an 

unbranched burrow with a lower clavate chamber and a convolute, tapered neck (maximum 

penetration depth: 5 cm; Fig. 1C). 

• Rippled sands ichnoassociation. Rippled sands are dominated by deep (20-30 cm) 

U-shaped burrows (Arenicolites) produced by sipunculans (Fig. 1D). Vertical burrows with 

constructional lining (Skolithos) are common especially on longshore bars; the 

suspension-feeding polychaete Megalomma is the tracemaker. With the exception of localized 

clusters with dense Thalassinoides, crustacean burrows are very rare. These elements closely 

resemble pre-Jurassic ichnoassociations, when decapod crustaceans were not dominating 

shallow marine environments. 

The mentioned ancestral features are explained by the peculiar intertidal environment of the 

Grado lagoon. Indeed, the studied microbial mats are characterized by extreme conditions: high 

cohesiveness, prolonged emersion time and noxious phosphate content. For these reasons, they 

represent a rich trophic niche available only to few non-marine specialists. On the other hand, 

rippled sands provide less extreme conditions, i.e. relatively high turbulence and low nutrients. 

However, decapod crustaceans prefer to settle within the adjacent sheltered, organic-rich 

habitats. 

The described ichnologic features, united to the peculiar physiographic and ecological 

context, make Grado an ideal analogue for past peritidal ichnological systems. Paraphrasing 

McKinney (2007), the Grado ichnosite allows to study “deep time on a tidal flat”. 

11


(A) Geographical setting and facies map. (B) Helminthoidichnites (He) and Macanopsis (Ma) are visible 

after peeling off the superficial, organic-rich level of the microbial mats. (C) Microbial mat with Macanopsis. 

The tracemaker (the coleopteran Heterocerus flexuosus) is arrowed; profile view. (D) Arenicolites (dashed) 

with its tracemaker, a sipunculan worm. 

Baucon, A. 2008. Neoichnology of a microbial mat in a temperate, siliciclastic environment. In: Avanzini M., 

Petti F. Italian Ichnology, Studi Trent. Sci. Nat. Acta Geol., 83: 183-203. 

Gerdes, G., 2003. Biofilms and macroorganisms, in: Krumbein, W.E., Paterson, D.M., Zavarzin, G.A. 

(Eds.), Fossil and Recent Biofilms: a Natural History of Life on Earth. Kluwer Academic Publishers, 

Dordrecht, pp. 197-216. 

McKinney, F.K., 2003. Preservation Potential and Paleoecological Significance of Epibenthic Suspension 

Feeder-Dominated Benthic Communities (Northern Adriatic Sea ). Palaios 18, 47-62. 

McKinney, F.K., 2007. The Northern Adriatic Ecosystem: Deep Time in a Shallow Sea. Columbia University 

Press, New York. 

McKinney, F.K., Hageman, S.J., 2006. Paleozoic to modern marine ecological shift displayed in the 

northern Adriatic Sea. Geology 34, 881-884. 

Seilacher, A., 1999. Biomat-related lifestyles in the Precambrian. Palaios 14, 86-93. 

Zuschin, M., Stachowitsch, M., 2009. Epifauna-Dominated Benthic Shelf Assemblages: Lessons From the 

Modern Adriatic Sea. Palaios 24, 211-221. 

12


A QUANTITATIVE TOOL FOR THE ICHNOLOGICAL ANALYSIS OF TIDAL 

ENVIRONMENTS: THE ICHNOGIS METHOD 

Andrea BAUCON, Fabrizio FELLETTI 

DIPARTIMENTO DI SCIENZE DELLA TERRA, Università di Milano, 20133, Milano, Italy, 

andrea@tracemaker.com 

Since its earliest roots in Renaissance times, trace fossil analysis relied on actualistic 

experiences for inspiring and testing theories and models. In fact, each of the major watersheds 

in the history of ichnology was initiated by advances in neoichnological knowledge: the 

paleoichnological knowledge of Leonardo da Vinci was inspired by modern burrowing and boring 

organisms (Baucon, 2010), the experiments of Nathorst disproved the botanical interpretation of 

trace fossils, the Senckenberg Laboratory marked the development of the modern approach in 

ichnology (Osgood, 1975). With the Internet and GPS among the faster-growing technologies of 

the decade, the previous historical considerations addresses traditional questions with novel 

approaches: How are traces distributed on a tidal flat? What are the association patterns (‘links’) 

between ichnotaxa? What is the relationship between traces and their tidal environment? 

With these questions in mind, we present a new method to capture, manage, analyze, and 

display geographically referenced ichnological data: IchnoGIS. This new method uses spatial 

location as the key index variable for all other information, recorded during different sampling 

stages (Fig. 1A): 

a) quadrat sampling. For each sampling site, a frame (quadrat) of a set size is placed on the 

substrate. Spatial coordinates, facies and ichnological attributes (i.e. abundance of each 

ichnotaxon) are recorded. 

b) trench sampling. Quadrat sampling emphasizes the recognition of distinct structures on 

the sediment surface, being unsuitable for burrows with poorly visible openings. Consequently, 

quadrat sampling is complemented by the study of vertical trenches, realized at regularly spaced 

sites. 

c) environmental and topographical sampling. Several environmental attributes can be 

recorded to determine the major control factors on trace distribution: PH, Reduction Potential 

(Eh), nutrients (nitrite, nitrate, phosphate), salinity, depth of the Redox Potential Discontinuity 

Layer, emersion time and substrate firmness, measured with the modified Brinell method (Gingras 

and Pemberton, 2000). 

Data analysis is based on the integration of network theory (Fig. 1B) with geostatistical 

techniques (Fig. 1C). More specifically, geostatistical analysis enables to measure the spatial 

structure of burrow distribution and allows to interpolate trace abundance in unsampled positions. 

Consequently, the IchnoGIS method leads to the definition of ichnological maps in which trace 

density is confronted to geomorphological gradients (Fig. 1C). 

Furthermore, network analysis exploits the fact that traces assemble in a complex web-like 

structure. Accordingly, an ichnological system can be conveniently described by network graph, 

which represents ichnotaxa and their connections (Fig. 1B). According to this approach, 

researchers can analyze not only the degree of association between different ichnotaxa, but also 

describe how an ichnotaxon is embedded in the whole system. Ichnoassociations can be found 

by applying specific pattern-finding algorithms. Finally, the integration of geostatistics and network 

theory allows to define the environmental significance of ichnoassociations and find out the 

factors controlling an ichnological system. 

In order to test the accuracy of the IchnoGIS method, we applied it on a modern tidal flat: 

the Grado lagoon (Northern Adriatic Sea, Italy). Our results show that the IchnoGIS method 

provides unprecedented research opportunities for ichnologists and sedimentologists, as it allows 

to determine accurately spatial distribution, association patterns and environmental significance of 

traces from the Grado lagoon. In particular, emersion time, hydrodynamism, substrate firmness 

and microbial binding are the major control factors determining the structure and distribution of 

trace associations. These structuring factors are used to define a predictive model of 

ichnoassociation composition, providing an immediate tool for paleoenvironmental reconstitution 

(Fig. 1D). 

13


(A) The IchnoGIS method. (B) The IchnoGIS method describes an ichnosite through a network graph 

(ichnonetwork). The ichnonetwork graph displays which ichnotaxon is associated to which other and 

records the intensity of each relation (weight of the connections). Data from the Grado lagoon (Adriatic Sea, 

Italy). (C) The IchnoGIS method allows to compare environmental data with ichnological maps. In 

particular, the figured example considers exposure (or emersion) time. Data from the Grado lagoon 

(Adriatic Sea, Italy). (D) The Grado ichnological model, as defined by the IchnoGIS method. Cr – Crab 

burrows ichnoassociation: dominated by crab burrows, sparse Arenicolites; Th - Thalassinoides 

ichnoassociation: dominated by Thalassinoides and small Arenicolites; Ar –Arenicolites ichnoassociation: 

dominated by large Arenicolites, occasional Skolithos and Thalassinoides; Sk – Skolithos ichnoassociation: 

dominated by large Skolithos, often lined; Ma – Macanopsis ichnoassociation: dominated by Macanopsis 

and Helminthoidichnites; Pa – Parmaichnus ichnoassociation: dominated by Parmaichnus 

Baucon, A., 2010. Leonardo Da Vinci, the Founding Father of Ichnology. Palaios 25, 361-367. 

Gingras, M.K., Pemberton, S.G., 2000. A field method for determining the firmness of colonized sediment 

substrates. Journal of Sedimentary Research 70, 1341-1344. 

Osgood, R.G., 1975. The history of invertebrate ichnology, in: Frey, R.W. (Ed.), The Study of Trace Fossils. 

Springer Verlag, New York, pp. 3-12. 

14


TIDAL BORE INDUCED SEDIMENTS IN INCISED VALLEYS, UTRILLAS FM, ALBIAN, 

SW IBERIAN RANGES, SPAIN 

M. CHAMIZO BORREGUERO*, N. MELENDEZ*, Poppe DE BOER** 

*GRUPO DE ANALISIS DE CUENCAS. DPTO. DE ESTRATIGRAFIA-INSTITUTO DE GEOCIENCIAS 

(UCM-CSIC), Universidad Complutense, Ciudad Universitaria, 28040, Madrid, Spain, 

manu.chamizo@hotmail.com, nievesml@geo.ucm.es 

**SEDIMENTOLOGY GROUP, DEPARTMENT OF EARTH SCIENCES, UTRECHT UNIVERSITY, 

Budapestlaan 4, 3584 CD, Utrecht, The netherlands, p.l.deboer@uu.nl 

Exceptionally well preserved tidal-bore deposits within Albian siliciclastics in the 

southwestern Iberian Basin, adjacent to the Tethys, are interbedded with sediments formed by 

ephemeral alluvial discharge, tidal reworking and aeolian processes. 

The study area is located in the southwestern domain of the Iberian Ranges (Eastern 

Spain) in the Serranía de Cuenca. The Iberian Ranges form a NW-SE striking intraplate fold belt 

and represent an uplifted (inverted) Mesozoic basin that was formed by crustal thinning during 

earlier rift stages. Moreover, the Serranía de Cuenca sub-basin was controlled by minor 

SSW-NNE extension faults that acted as thresholds during the middle Cretaceous sea-level rise 

(Meléndez, 1983; Capote et al., 2002). Above Lower Cretaceous synrift continental deposits, the 

siliciclastic Albian to Early Cenomanian Utrillas Sandstone Formation is laterally very extensive 

and crops out all over the Iberian Ranges. 

In five detailed sections recorded near the village of Uña, 14 sedimentary facies were 

distinguished and grouped into 5 facies associations: ephemeral alluvial, overbank, tidal flat, 

aeolian and tidal bore deposits. Ephemeral alluvial discharge and tidal reworking alternated with 

varying supremacy, and the continuous presence of ventifacts, feldspars as well as fine 

windblown sand reflects continued aeolian activity. 

Two main units are divided by a laterally continuous, deep and sharp incision attributed to a 

relative sea-level fall. The Lower Unit, deposited in the (fluvial) alluvial–tidal transition zone, 

records the evolution from a tidally reworked arid ephemeral alluvial system to tidal flats and 

aeolian dunes as the result of a progressive decrease of alluvial discharge resulting in an 

increase of the tidal and aeolian signature. 

The Upper Unit, covering the sharp and deep incision, shows a reactivation of alluvial 

discharge, although weaker than in the Lower Unit. The most remarkable characteristics of the 

Upper Unit are (i) two deep incision surfaces, one at the base of the Upper Unit and a second one 

higher in the succession, and (ii) the exceptional and conspicuous presence of high-energy 

flood-tide-induced deposits, brought in through the deep and likely dry incisions. Two such 

deposits, directly upon the incision surfaces, are interpreted as the product of tidal bores. The two 

deep incisions in the Upper Unit, at the base of the two tidal bore deposits, lack ephemeral 

alluvial deposits suggesting the absence or bypass of alluvial discharge. Thus, erosion and 

subsequent fill of these deep incisions are suggestive of two different, successive processes, i.e. 

(i) erosion, later followed by (ii) deposition, as is characteristic for incised valley fills (Boyd et al., 

2006). 

The successions ascribed to tidal bore activity are characterised by up to 9 m thick well 

sorted sands with carbonate cement and dinoflagellates. Main sedimentary structures are 

high-energy low-angle planar lamination and decimetre-scale gently tangential planar 

cross-bedding with occasional weak internal erosion surfaces. The palaeocurrent pattern is 

persistently inland. 

Tidal bore deposits in the Uña outcrop consist of marine sediments carried landinward by 

high-energy flood tides, where alluvial discharge is low or absent, as is the case nowadays for 

tidal bores (Lynch, 1982; Bartsch-Winkler and Lynch, 1988; Kjerfve and Ferreira, 1993; Chanson, 

2011). Examples from the fossil sedimentary record are rare. Martinius and Gowland (2011) 

reported on tidal bore deposits in the Late Jurassic Lourinhã Fm (Western Portugal). 

In the case presented here, the sub-basin formed a funnel-shaped estuary connected to 

the Tethys. In this way, the tide in the open marine domain may have been amplified by basin 

resonance, while the funnel-shaped estuary led to a further amplification of the flood tide resulting 

15


in landward-directed sediment transport and the formation of the up to 9 m thick successions of 

low-angle lamination and gently tangential planar cross-bedding. 

Detailed sketch of second incision and tidal bore deposits in Uña outcrop (Iberian Basin, Spain). 

Bartsch-Winkler, S. and Lynch, D.K. (1988) Catalogue of worldwide tidal bore occurrences and 

characteristics. U.S. Geol. Surv. Circ., 1022, 17. 

Capote, R., Muñoz, J.A., Simón, J.L., Liesa, L.C. and Arlegui, L.E. (2002) Alpine Tectonics I: The alpine 

system north of the Betic Cordillera. In: The Geology of Spain (Ed: W. Gibbson, T. Moreno). The Geological 

Society of London. 367-400. 

Chanson, H. (2011) Current knowledge in tidal bores and their environmental, ecological and cultural 

impacts. Environ. Fluid Mech., 11, 77–98. 

Kjerfve, B. and Ferreira, H.O. (1993) Tidal bores: first ever measurements. Cienc. Cult., 45, 135–138. 

Lynch, D.K. (1982) Tidal bores. Sci. Am., 247, 134–143. 

Martinius, A.W. and Gowland, S. (2011) Tide-influenced fluvial bedforms and tidal bore deposits (Late 

Jurassic Lourinhã Formation, Lusitanian Basin, Western Portugal) Sedimentology, 58, 285-324. 

Meléndez, M.N. (1983) El Cretácico de la Región de Cañete - Rincón de Ademuz (Provincias de Cuenca y 

Valencia) [Tesis Doctoral]. Seminarios de Estratigrafía, Serie Monografías 9. UCM. 

16


LATE QUATERNARY STRATIGRAPHIC EVOLUTION OF BAEKSU OPEN-COAST 

TIDAL FLAT, WEST COAST OF KOREA: REGIONAL UNCONFORMITY-BOUNDED 

TWO TIDAL DEPOSITS 

Taesoo CHANG, Jincheol KIM, Dong-Geun YOO 

KOREA INSTITUTE OF GEOSCIENCE & MINERAL RESOURCES, #124, Gwahang-No, Yuseong-Gu, 

305-350, Daejeon, Korea, tschang@kigam.re.kr 

Along the eastern margin of the Yellow Sea, numerous macrotidal flats are extensively 

developed. In the last two decades, lithostratigraphic studies of these tidal deposits have been 

based on sedimentological anlayses of vibrocores up to ~6 m long, and hence stratigraphically 

the tidal deposits were restricted mostly to the Holocene in age due mainly to lack of deep cores. 

Another reason for that was likely a general dearth of dateable materials and credibility of age 

dates prior to the Holocene. One of the important findings from the Korean tidalite researches in 

the past was the presence of the semi-consolidated, yellow oxidized layers overlain by Holocene 

tidal deposits with a stark erosion boundary defining them. Under the situation without any reliable 

age constraints for that layers, the pre-Holocene strata have been controversial. 

In a recent year, however, advanced dating technologies, i.e., OSL and 14C AMS, have 

enabled to ensure the age constraints of older tidal deposits dating back to late Pleistocene, and 

to understand the stratigraphic packages in response to local changes in sea level. Previous 

works showed that some tidal deposits at the Korean west sea coasts can be grouped into at 

least two unconformity-bounded sequences, which formed in response to late Quaternary 

sea-level fluctuations (Lim and Park, 2003; Choi and Dalrymple, 2004; Choi and Kim, 2006). 

However, some age dates determined by AMS, particularly ages around 40,000~50,000 yr BP, 

are still questionable, the ages leading to discrepancy between the curve reconstructed and the 

elevation of the deposits. In order to elucidate the chronostratigraphic problems, an OSL dating 

method was applied to the pre-Holocene tidal deposits recovered from the Baeksu tidal flat, 

Korea. In addition, the relationship between the seismic reflection boundary and the lithologic 

surface based on the analysis of seismic profiles and deep- drilled cores will be addressed. 

Sediment cores from an open-coast, Baeksu macrotidal flat, Korea, contain about 45 m 

thick two tidal deposits stratigraphically separated by a yellow, semi-consolidated mud layer and a 

gravel layer. Two tidal units, a Holocene unit and an underlying late Pleistocene unit, have 

recurred, as previously reported in the other tidal basin. In the course of core examination, the 

Baeksu open-coast tidal deposits can be grouped into distinct 6 facies associations, shoreface 

sands, sand flat, gravelly channel lags, paleosoil horizons, mudflat/salt marshes, and fluvial 

gravel lags with muds in descending order. The Baeksu tidal flats comprise at least two 

sequences which formed in response to fluctuations in local sea-level during the late Quaternary. 

The oxidized layer characterized by semi-consolidated, yellowish sediments separates them, 

producing a regional unconformity. Such an unconformity-bounding surfaces correlate well with a 

prominent mid-reflector, observed on seismic profiles. Consequently, the layer associated with 

the striking reflector may signify the emergence of the Yellow Sea shelf during the pre-Holocene 

lowstand. Each sequence consists of lower fluvial deposits and overlying tidal deposits. However, 

intertidal sands are commonly missing in lower sequence. The presence of two tidal deposits 

warrants that two cycles of major sea-level fluctuations are recorded, the similarity between 

Holocene and late Pleistocene tidal deposits indicating macrotidal regime recurred in the region. 

The extensive shallow shelf and relatively stable tectonic setting of the Yellow Sea appears to 

promote the repetition of tidal sedimentation in the Baeksu open-coast tidal flat. 

17


Columnar sections of drillcores and their stratigraphic evolution. Unit I and II are separated by a sharp 

erosional surface, interpreted here as a sequence boundary which defines between the upper Holocene 

and the lower pre-Holocene deposits. 

Choi, K.S., Dalrymple, R.W. (2004) Recurring tide-dominated sedimentation in Kyonggi Bay (west coast of 

Korea): similarity of tidal deposits in late Pleistocene and Holocene sequences. Marine Geology, 212, 

81-96. 

Choi, K.S., Kim, S.-P. (2006) Late Quaternary evolution of macrotidal Kimpo tidal flat, Kyonggi Bay, west 

coast of Korea. Marine Geology, 232, 17-34. 

Lim, D.I., Park, Y.A. (2003) Late Quaternary stratigraphy and evolution of a Korean tidal flat, Haenam Bay, 

southeastern Yellow Sea, Korea. Marine Geology, 193, 177-194. 

18


BAEKSU OPEN-COAST TIDAL FLAT OF THE KOREAN WEST SEA COAST 

REVISITED: A DEPOSITIONAL MODEL AND ITS PRESERVATION POTENTIAL 

Taesoo CHANG 

KOREA INSTITUTE OF GEOSCIENCE & MINERAL RESOURCES, #124, Gwahang-No, Yuseong-Gu, 

305-350, Daejeon, Korea, tschang@kigam.re.kr 

In a recent year, open-coast tidal flats and its ancient analogues have been increasingly 

received attention, as they are a hybrid depositional system controlled by the interaction of waves 

and tides. In a consequence, some attempts were made to distinguish between a classical tidal 

flat and wave-dominated tidal flat, and between tidal shoreface and open-coast tidal flat too (Yang 

et al., 2005, 2008; Basilici et al., 2011; Fan, 2012). Baeksu open-coast tidal flats were previously 

reported as such a typical hybrid coastal system, wave-dominated in winter and tide-dominated in 

summer due to the seasonal wind distribution. However, the arguments for this open-coast tidal 

flat model were raised and alternative interpretations suggested as two facies models, an 

intertidal shoreface for outer part and an estuarine tidal flat model for inner part (Chang and 

Flemming, 2006). In this regard, we revisited on the open-coast tidal flats in order to fulfill the 

arguments and to discuss a depositional model for hybrid tidal flats with respect to preservation 

potential. For this purpose, over 200 surface sediments were taken from intertidal to subtidal 

regions using a grab-sampler. Vibro-coring was carried out along the two transects placed across 

the reclaimed area. 

The Baeksu tidal flats are 6~10 km wide and ~10 km long and it opens directly to the Yellow 

Sea without any barriers and the coast-oblique subtidal sand bars boarder the seaward margin of 

the tidal flats. Near the high-tide line, the artificial dikes were built and the upper flats have been 

reclaimed over the century. Beyond the reclaimed area where the villages are located, the 

degraded coastal dune fields occur. The only topographic features on the flats are the low-relief, 

shore-parallel swash bars and tidal channels are restricted to upper mud flats and salt marshes. 

The tide is semidiurnal with a mean tidal range of 3.9 m, corresponding to the lower macrotidal 

regime. The wind regime is predominantly influenced by the monsoon, leading to strong 

seasonality. Significant wave heights vary between


Bathymetry of the study area with location of vibra-core and grab-sampling stations (dots) in the Baeksu 

open-coast tidal flats, West Coast of Korea. Water depths are in metres relative to Chart Datum 

Basilici, G., De Luca, P.H.V., Oliveirmares, E.P. (2011) A depositional model for a wave-dominated 

open-coast tidal flat, based on analyses of the Cambrian-Ordovician Lagarto and Palmares formations, 

north-eastern Brazil. Sedimentology, DOI: 10.1111/j.1365-3091.2011.01318.x. 

Chang, T.S., Flemming, B.W. (2006) Sedimentation on a wave-dominated, open-coast tidal flat, 

southwestern Korea: summer tidal flat-winter shoreface-discussion. Sedimentology, 53, 687-691. 

Fan, D. (2012) Open-coast tidal flats. In: Principles of Tidal Sedimentology (eds., R.A. Davis, R.W. 

Dalrymple), Springer, 187-229. 

Yang, B.C., Dalrymple, R.W., Chun, S.S. (2005) Sedimentation on a wave-dominated, open-coast tidal flat, 

southwestern Korea: summer tidal flat-winter shoreface. Sedimentology, 52, 235-252. 

Yang, B.C., Dalrymple, R.W., Chun, S.S., Johnson, M.E., Lee, H. (2008) Tidally modulated storm 

sedimentation on open-coast tidal flats, southwestern coast of Korea: distinguishing tidal-flat from 

shoreface storm deposits. In: Recent Advances in Models of Siliciclastic Shallow-Marine Stratigraphy (eds., 

G.J. Hampson, R.J., Steel, P.M., Burgess, R.W. Dalrymple), SEPM Spec. Publ., 90, 161-176. 

20


TIDAL AND CLIMATE CONTROLS ON THE MORPHOLOGICAL EVOLUTIONS AND 

THE INTERNAL ARCHITECTURE OF A TIDAL BAR: THE PLASSAC TIDAL BAR IN 

THE BAY-HEAD DELTA OF THE GIRONDE ESTUARY 

Eric CHAUMILLON*, Hugues FENIES**, Julie BILLY***, Jean-François BREILH* 

*UMR CNRS 7266 LIENSS, 2 rue Olympe de Gouges, 17000, La Rochelle, France, 

eric.chaumillon@univ-lr.fr, jbreil01@univ-lr.fr 

**CV ASSOCIES ENGINEERING, 7 Chemin de la Marouette, 64100, Bordeaux, France, 

hugues.fenies@orange.fr 

***CEFREM, UMR 5110, 52 Avenue Paul Alduy, 66860, Perpignan, France, juliebilly@gmail.com 

Estuarine tidal bars occur in the mouth and in the bay-head deltas of tide-dominated 

estuaries or mixed tide-and-wave dominated estuaries. Tidal bars deposited in estuary mouths 

are composed of relatively clean sands whereas tidal bars deposited in bay-head deltas can 

contain large quantities of mud. Estuarine tidal bars have an elongated or a lobate morphology, 

but relatively few studies have been conducted on the lobate category. This study is focused on a 

lobate tidal bar, the Plassac tidal bar, located in the bay-head delta of the Gironde Estuary. 

This work is based on: (1) successive bathymetric data (1905-2010) which allow to observe 

the geomorphological evolution of the bar (century scale), (2) detailed imaging of the bedforms 

that cover the surface of the bar (over a few days in 2010, Figure 1) which allow to analyze the 

sediment dynamic. Those well-constrained evolutions and governing processes, combined with 

very high resolution seismic and core data are then used to understand the internal architecture 

of the tidal bar and the fluvial sediment influx within the bay-head delta at a time scale of a 

century. 

The sediment transport pattern, inferred from the lee face orientations of subaqueous dunes 

observed on very high resolution bathymetric data acquired in 2010 (Figure 1), together with 

results from previous studies, allows explaining the five main mechanisms for the tidal bar 

evolution identified from 29 bathymetric maps since 1905: flood ramp infill, partial ebb shield 

breaching, lateral accretion of the ebb spits and ebb shield lengthening, generated by the merging 

of mini-flood lobes on the outer sides of the ebb spits. Lateral accretion seems to be a 

key-process of sediment accretion for lobate tidal sand bars. Most of the evolutions are explained 

by tidal processes, but fluvial influence is evidenced by correlating the presence of mini flood 

lobes (migrating seaward from the upper reaches of the bay-head delta) and the lengthening of 

the tidal bar with periods of high fluvial discharge. A 25 years periodicity in both the fluvial 

discharge and the tidal bar width, length and volume variations is evidenced and suggest the 

climate control on the tidal bar evolution. 

Seismic and core data show that the bar was deposited onto a basal bounding surface 

which consist of a discontinuous sub horizontal reflector correlated with sand and clay 

alternations and which may represent the main flooding surface within the Gironde Estuary. 

Within the sandbar, the master bedding corresponds to strong amplitude reflectors (clinoforms) 

correlated with continuous inclined mud-rich strata. Correlation with bathymetric data shows that 

clinoform orientations are not indicative of tide-induced sand transport direction but record the 

progressive lateral accretion of the sandbar generated by fluvial sand influx. Thus it appears that 

the internal architecture of the bar is dominated by lateral accretion of sand packages, isolated 

from one another by extensive inclined mud layers. A major strong amplitude inclined reflector, 

observed in the eastern ebb spit of the sandbar, is correlated with a 20 cm thick bed made of 

angular mud pebbles and was deposited between 1991 and 1993. Considering the period of time 

between 1958 and 2008, the years 1991 to 1993 were characterized by the largest number of 

autumn river floods and preceded by the years 1989 to 1991, characterized by the largest number 

of days of low river stage. A 3-step depositional process is proposed to explain the heterogeneity 

present within the internal architecture of the tidal bar: (1) during periods of low river stage, the 

turbidity maximum of the Gironde Estuary is located upstream, in the bay head delta, leading to 

mud deposition on the sandbars; (2) subsequent periods of floods (especially autumn floods 

occurring immediately after the dry summer season), lead to erosion of the mud drape lying on 

the sandbar and to deposition of a mud clasts layer rapidly buried by massive sand transport. 

From this study it appears that sandbars emplaced in bay head deltas of estuaries are 

heterolithic bodies dominated by tides and influenced by fluvial processes. The fluvial influence 

implies that they have a good potential to record high frequency climate changes. During periods 

of low rainfall and low river stage, sand supply to the tidal bar is reduced and mud deposition 

occurs on the tidal bar, whereas during high rainfall and associated floods, seaward sand 

transport increases and leads to tidal bar lengthening, lateral accretion processes and rapid 

burying of antecedent morphological features and strata. 

21


High resolution digital elevation model (1.3 m grid) of the Plassac Tidal Bar Plassac Tidal Bar in 2010 

(From Billy J., Chaumillon E., Féniès H. and Poirier C., Geomorphology, in press). 

22


TIDAL RHYTHMITES IN THE UPPER CRETACEOUS NESLEN FORMATION, UTAH, 

USA: THEIR IMPLICATIONS FOR THE SEDIMENTOLOGY AND STRATIGRAPHIC 

ARCHITECTURE OF TIDAL-FLUVIAL CHANNEL 

Kyungsik CHOI*, Ronald STEEL**, Cornel OLARIU** 

*FACULTY OF EARTH SYSTEMS AND ENVIRONMENTAL SCIENCES, CHONNAM NATIONAL 

UNIVERSITY, 300 Yongbong-Dong, Buk-Gu, 500-757, Gwangju, Korea, tidalchoi@hotmail.com 

**JACKSON SCHOOL OF GEOSCIENCE, UNIVERSITY OF TEXAS AT AUSTIN, 1 University Station 

C9000, 78712, Austin, Usa 

Upper Cretaceous Neslen Formation in the Floy Canyon, Utah is dominated by multiple 

stackings of tidal-fluvial channel deposits that consist of inclined heterolithic stratification (IHS) 

(Figure top). Each channelized unit is 3 – 10 m thick and has an upwardly fining succession with 

a sharp and erosional base and a gradational top of coaly mud. IHS has variable dips ranging 

from 2 and 5 degree and consists of rippled fine to medium sandstone and interlaminated 

siltstone to mudstone. On the basis of facies association and stratigraphic occurrence, four types 

of tidal rhythmites (TR) are identified within the IHS (Figure down). TR is composed of mostly 

siltstone and less commonly very fine sandstone, exhibiting neap-spring tidal cycles and diurnal 

inequalities. TR is either planar laminated or rippled. Ripples are commonly unidirectional and 

migrating updip of IHS. Type 1 TR is composed of rhythmically laminated very fine to siltstone 

that alternates with non-cyclic rippled sandstone, occurring near the base of channel. Rippled 

sandstone has a highly variable thickness and geometry with an erosional base. Type 2 TR 

consists of alternating rippled sandstone and laminated mudstone, wherein the former represents 

spring tides and the latter neap tides. Type 2 TR is common in the lower to upper part of IHS unit. 

Type 3 TR is defined by rhythmically climbing ripple lamination, exhibiting rhythmic changes in 

cross-laminae thicknesses. Type 3 TR is mainly present at the top of IHS unit. Type 4 TR is made 

up of laminated siltstone that is either planar or inclined, occurring in the middle to upper part of 

IHS. The prevalence of updip migrating ripples on the IHS suggests that rhythmic tidal deposition 

occurred in a highly sinuous and actively migrating channel, where mutually evasive tidal current 

is well established. Type 1 and Type 2 TR represent subtidal point bar deposition while Type 3 

and Type 4 TR reflect intertidal point bar deposition. 

23


Top: Outcrop photograph (A) and linedrawings (B) showing multiple stacking of IHS (inclined heterolithic 

stratification) units of 2-5 m thick, which is developed in the Upper Cretaceous (Campanian) Neslen 

Formation, Horse Canyon area, Utah, USA. Down: Tidal rhythmites (TR) from Neslen Formation. (A) Type 

1 TR showing gradual change of laminae thicknesses reflecting neap-spring tidal cycle, which is found in 

the interbbeded rippled sandstone and rhythmically laminated sandstone. (B) Type 2 TR consists of rippled 

sandstone beds that exhibit well-defined cyclicity in ripple heights that varies sinusoidally. (C) Rhythmically 

climbing rippled sandstone illustrating a gradual change in ripple height and wavelength (Type 3 TR). (D) 

Thinly and faintly laminated sandstone with rhythmic lamination thickness variation (Type 4 TR). White 

arrows indicate neap-stage laminae. 

24


RAPID INFILLING OF MACROTIDAL ESTUARY DURING EARLY HOLOCENE IN 

YEOCHARI TIDAL FLAT, GYEONGGI BAY, WEST COAST OF KOREA 

Kyungsik CHOI, Jae Hoon JUNG, Joo Hee JO 

FACULTY OF EARTH SYSTEMS AND ENVIRONMENTAL SCIENCES, CHONNAM NATIONAL 


Recent drilling campaign unveiled up to 12 m thick tidal rhythmites (TR) in the lower part of 

Holocene successions at Yeochari tidal flat, west coast of Korea (Figure top). Various tidal 

rhythms are encoded in the TR, which include diurnal inequality, synodic neap-spring cycle, 

fortnightly inequality, and semi-annual cycle (Figure down). Reduced number of laminae in a 

neap-spring tidal cycle, accentuated anomalistic cycle, fine-grained nature and close association 

with organic-rich muds are all suggestive of upper intertidal origin of the TR. Abnormally thick 

neap-spring tidal cycles are interpreted to be associated with monsoon discharge period. 

Recurrence of TR bounded by organic-rich muds indicates that base-level has been fluctuated 

during the deposition of the TR. Sedimentation rate inferred from the TR ranges from 1.7 

cm/month to 10 cm/month with the maximum annual rate reaching up to 0.3 m. Stratigraphic 

analysis with AMS dating indicates that TR-deposition occurred in the topographic lows between 

main channels during early Holocene (10~8 ka) when sea-level rose at the maximum rate of 2 cm 

per year. Given the stable tectonic condition of study area, the generation of accommodation 

space due to the rapid base-level rise combined with antecedent topography that effectively 

facilitated protection from storms seems to have played a key role in the creation and 

preservation of unusually thick and delicate tidal records during Holocene transgression. 

25


Graphic summary of columnar section of BH 16. Tidal rhythmites demonstrate various tidal cyclicities 

including diurnal inequality, synodic neap-spring cycle, anomalistic neap-spring cycle, and presumably 

semi-annual cycle. White arrows indicate neap-tides laminae. Note well-developed rhythmites are mainly 

present in the early Holocene unit (8 ka~9 ka), which was formed during rapid transgression. Depths are 

meters below present mean sea level. 

26


MORPHODYNAMICS OF TIDAL CHANNELS IN THE MACROTIDAL YEOCHARI 

TIDAL FLAT, GYEONGGI BAY, WEST COAST OF KOREA: IMPLICATION FOR THE 

ARCHITECTURE OF INCLINED HETEROLITHIC STRATIFICATION 

Kyungsik CHOI, Chang Min HONG, Chung Rok OH, Jae Hoon JUNG 

FACULTY OF EARTH SYSTEMS AND ENVIRONMENTAL SCIENCES, CHONNAM NATIONAL 


Morphodynamics of intertidal channels were monitored using a total station and RTK GPS 

in the Yeochari tidal flat, Gyeonggi Bay, Korea. Along the transect YC-1, four channels (CH-1, 

CH-2, CH-3, and CH-4 from seaward to landward) are present in the lower intertidal flat (Figure 

1). They are 240-570 m wide and 1.2-2.4 m deep at bankful stage. Three-year-long observations 

reveal that channels migrate at a noticeable rate with strong seasonality. In particular, CH-4 

migrated about 200 m in 30 months. During summertime in 2010 and 2011, it migrated as much 

as 40 m in a month, respectively, which leads to rapid accumulation up to 40 cm in the point bar 

position of channel. In contrast, migration rate decreased down to 5 m per month between fall to 

spring. Difference in channel migration between summer and the rest of year can be explained by 

the occurrence of enhanced ebb currents due to increased runoff discharge during summertime. 

Point-bar geometry alternates between a concave-up profile in summertime and convex-up profile 

in the rest of season (Figure 3). Varying degree of rill erosion in the upper point bar results in the 

seasonal morphologic change. Pronounced rill erosion and high suspended sediment 

concentration in summertime led to rapid accumulation of sediment at channel base, creating a 

concave-up point-bar geometry. Continued sedimentation with little rill erosion resulted in a 

convex-up point-bar geometry during the rest of season. Present study suggests that the external 

architecture of inclined heterolithic stratification of intertidal origin is controlled by seasonality in 

precipitation. 

27


Top: Diagram of transect YC-1 showing morphologic features of Yeochari tidal flat. Upper tidal flat has a 

concave-up profile. Small channels are present in the concave to convex-up middle tidal flat. Lower tidal flat 

is characterized by channels and interchannel areas covered by migrating dunes. Down: Temporal 

morphologic variation of channel profiles at CH-4, displaying a distinct seasonality. Point bar attains a 

concave-up profile during summertime, whereas it has a convex-up profile during the rest of season. Such 

seasonal morphologic change resulted from monsoon-driven runoff discharge. 

28


WARM-TEMPERATE, MARINE, CARBONATE SEDIMENTATION IN AN EARLY 

MIOCENE, TIDE-DOMINATED, INCISED VALLEY; PROVENCE, SE FRANCE 

Robert W. DALRYMPLE*, Noel JAMES*, Meg SEIBEL*, David BESSON**, Olivier PARIZE*** 

*DEPT. GEOL. SCI. & GEOL. ENG., Queen'S University, K7L 3N6, Kingston, Ontario, Canada, 

dalrymple@geol.queensu.ca, james@geol.queensu.ca, meseibel@gmail.com 

**SHPEC/DHMD, 5 Avenue Buffon, 4064, Orleans Cédex 2, France, david-besson@hotmail.fr 

***AREVA NC, 1 Place Jean Millier, 92084, Paris la Défense, France, olivier.parize@areva.com 

The Miocene in southern France was generally a time of tidal sedimentation. Some of the 

most spectacular tidal deposits occur in a series of incised valleys that were cut into older 

sediments during a succession of sea-level lowstands, and back-filled during sea-level rises by 

tidal deposits with variable amounts of bioclastic carbonate material. We have examined one of 

these valleys in detail, using a combination physical and carbonate sedimentological approaches, 

to obtain a more holististic paleoenvironmental reconstruction. 

The Saumane-Venasque paleovalley is oriented north-south and cuts across the westerly 

end of the Vaucluse Mountains that were rising at the time of valley incision and filling. The valley 

is narrow (2-5 km wide) and has several tributaries entering from the east and west. The portion 

of the valley between Saumane and Venasque is filled with well-cemented limestones, but the 

more northerly part of the valley is empty, presumably because it was filled with less permeable, 

finer-grained material that was not as tightly cemented. Paleogeographic reconstructions indicate 

that the estuary contained one, gently sinuous, main channel that was up to 25 m deep and 

flanked by shoals that were cut by smaller channels tied to the tributary valleys. The general 

morphology of the system was broadly similar to that the modern-day Scheldt estuaries in The 

Netherlands. However, the preserved valley-filling deposits may represent a flood-tidal delta (the 

system was overwhelmingly flood dominated as indicated by the pervasive presence of 

northward-direct cross bedding) that passed landward into a muddy “lagoon” that existed in the 

exhumed (empty) valley to the north. 

The water in this “estuary” was warm-temperate, with normal marine to mildly brackish 

salinities. The absence of significant river input during valley filling led to the deposition of 

extensive calcarenites that are pervasively cross-bedded. All of the limestones are variably rich in 

quartz, glauconite, and minor phosphate. The principle biofragments are echinoids, bryozoans, 

coralline algae, barnacles, and benthic foraminifers. Particles are largely parautochthonous, 

produced in seagrass meadows on the flanking shoals, on rocky substrates along the valley walls 

that were colonized by macroalgae (kelp), and within the subaqueous dune fields that 

characterized the channels and their flanks. Some of the grains could have been brought into the 

estuary from areas farther seaward by the flood-dominant currents. 

The valley fill is compound, and is partitioned into two sequences and three subsequences 

(Fig. 1; Besson, 2005; Seibel, 2009). Many packages have a similar upward progression of 

deposits, the complete succession consisting of six stages: 1) a basal erosional surface that is 

locally bored and glauconitized, which represents the sequence boundary; 2) a discontinuous unit 

of lagoonal lime mudstone or wackestone; 3) an overlying thin (< 1 m) conglomerate that is the 

tidal ravinement surface; 4) a decameter-thick TST series of pervasively cross-bedded 

calcarenites that formed within the main estuary channel; 5) a several meter–thick maximum 

flooding interval (MFI) of argillaceous, bioturbated muddy quartzose limestones that accumulated 

in an open-marine setting, in water depths of ~ 50 m after the interfluves were inundated; and 6) a 

local thin HST of fine-grained calcarenite. Tidal currents during stages 2 and 3 were accentuated 

by the constricted topography, but the tidal currents did not decrease immediately after flooding of 

the interfluves, but continued to be strong as water depths increased, forming formset dunes up 

to 7 m in height on top of the valley fill (sensu strito). These strong tidal currents in deep water 

are presumably due to far-field influences associated with the transgressive expansion of the 

seaway in the Rhodanian foreland basin farther north. 

There is a temporal change in the composition of the overall succession with quartz, 

barnacles, encrusting corallines, and epifaunal echinoids decreasing in abundance upward, 

whereas bryozoans, articulated corallines, and infaunal echinoids increase in numbers upward 

through the sequence set. This trend is interpreted to be the result of changing oceanographic 

conditions as the valley was filled, bathymetric relief was reduced, rocky substrates were replaced 

as carbonate factories by seagrass meadows and subaqueous dunes, and the setting became 

29


progressively more open marine. These cool-water limestones are characteristic of a suite of 

similar calcareous sand bodies, located elsewhere in southern France and beyond, that 

developed in environments with little siliciclastic or freshwater input during times of high amplitude 

sea-level change, wherein complex inboard antecedent topography was flooded by a rising 

ocean. 

((Upper) Simplified vertical succession of deposits within the Saumane-Venasque incised-valley fill. 

(Lower) Simplified cross section of the Saumane-Venasque incised-valley fill. (Modified after Besson, 

2005). 

Besson, D., 2005, Architecture du bassin Rhodano-Provençal Miocéne (Alpes, S.E. 1220 France): relations 

entre déformation, physiographie et sédimentation dans un 1221 basin molassique d’avant-pays. Ecole 

Nationale Supérieure des Mines de Paris, 1222 Paris, 250 pp. 

Seibel, M.J., 2009, Deposition and diagenesis of the Miocene Saumane-Veasque limestones, southeastern 

France. Unpubl. M.Sc. thesis, Queen's University, Kingston, ON, 144 p. 

30


LIVE UNDER TIDAL REGIME: THE ROLE OF THE BRITTLE-STAR OPHIOTHRIX 

FRAGILIS BEDS FROM THE EASTERN BAY OF SEINE IN THE FINE PARTICLE 

DEPOSIT-SUSPENSION MECHANISMS 

Jean-Claude DAUVIN*, Khadija BERYOUNI**, Sophie LOZACH*, Yann MEAR**, Anne MURAT**, 

Emmanuel POIZOT** 

*UMR CNRS 6143 M2C, UNIVERSITE DE CAEN, 24 rue des Tilleuls, 14000, Caen, France, 

jean-claude.dauvin@unicaen.fr 

**GEOCEANO, Cnam/intechmer bp 324, 50110, Tourlaville, France 

In the English Channel, the brittle-star Ophiothrix fragilis is a common epifauna species 

mainly found in strong tidal current characterized by pebbles benthic habitats (Holme, 1984). In 

the Bay of Seine, O. fragilis is however living on gravel and coarse sandy sediments and more 

locally, it occurs in areas with unexpected amount of fine particles for such high hydrodynamic 

areas (Mear et al., 2006; Lozach et al., 2011). This species forms dense aggregation supporting 

high density populations (1,500 to 7,000 ind.m-2) and both ophiuroid aggregation morphology and 

behaviour of juveniles play an important role in formation of relatively large patches in term of 

surface area on the seafloor. Moreover, living in dense aggregations may reduce displacement by 

strong currents (Warner and Woodley, 1975). Adults, although mobile, are not highly active, but 

O. fragilis can be a crawling epibenthic species; individuals will crawl back and forth across water 

currents until a conspecific was found (Broom, 1975). Some migration of adults from nearby 

populations may be possible. Where dense Ophiothrix aggregations are found on bedrock 

surfaces they may monopolize the substratum, virtually to the exclusion of other epifauna. In 

contrasts, beds on soft bottom may contain a rich associated fauna, with a dominance of large 

suspension-feeders. In addition, O. fragilis plays a major role in pelago-benthic transfer of 

particles from the water column to the benthic habitats due to its suspension feeding activity 

(Davoult and Gounin, 1995). 

At the scale of the Bay of Seine patches Gentil and Cabioch (1997) suggest that O. fragilis 

show spatial changes along the years due the variability of the recruitment; but, in the Dover 

Strait, some had remained stable in the long term (Davoult and Gounin, 1995). By contrasts, in 

the Plymouth area, dense Ophiothrix beds showed large long-term fluctuations from the end of 

the 19th century, to the 1970’s (Holme, 1984). Later, for the Bay of Seine, Lozach et al. (2011) 

have showed that the patches of abundances presented several spatial scales of organisation, 

from small scales (differences between grab replicates), local scales (differences between sites) 

and regional scales (differences between areas in the Bay of Seine). 

The accumulation of benthic data during the last 25 years in the eastern part of the Bay of 

Seine from several scientific programmes permits to revisit the spatio-temporal structure patterns 

of the Ophiothrix fragilis population in this area. The objective of this communication is to analyse 

the temporal changes of the O. fragilis aggregation from 1986 to 2010 in a tidal area affected by 

the Seine estuary and submitted to potential sediment supply from the dumping site of Le Havre 

harbour dredging operations. During all surveys, there was a similar pattern, i.e. persistence of 

stations with high abundances of Ophiothrix and stations with the absence of Ophiothrix showing 

that there was a high heterogeneity of the spatial population pattern. Finally, it is possible to 

propose a conceptual model for the evolution of the Ophiothrix fragilis beds offshore Antifer 

harbour in an area under the influence of natural and anthropogenic constraints (Figure 1). In 

addition to the fine particles input from the Seine estuary and the Octeville deposit area of Le 

Havre habour, when a dense population of brittle-star is established on this gravely substrate, the 

silting increases due to biological influences. 

31


Schematic model of evolution of the seabed in the Bay of Seine under the four actions of Seine River 

discharges, tidal currents, swell and high Ophiothrix fragilis populations 

Broom, D.M., 1975. Aggregation behaviour of the brittle-star Ophiothrix fragilis. Journal of the Marine 

Biological Association of the United Kingdom 55, 191-197. 

Davoult, D., Gounin, F., 1995. Suspension feeding activity of a dense Ophiothrix fragilis (Abildgaard) 

population at the water-sediment interface: Time coupling of food availability and feeding behaviour of the 

species. Estuarine Coastal and Shelf Science 41, 567-577. 

Gentil, F., Cabioch, L., 1997. Les biocénoses subtidales macrobenthiques de la Manche, conditions 

écologiques et structure générale. In: Dauvin J.C., (édit.) 1997. Les biocénoses marines et littorales 

françaises des côtes Atlantique, Manche et Mer du Nord, synthèse, menaces et perspectives. MNHN, 

Paris, 68-78. 

Holme, N.A., 1984. Fluctuations of Ophiothrix fragilis in the Western English Channel. Journal of the Marine 

Biological Association of the United Kingdom 64, 351-378. 

Lozach, S., Dauvin, J.C., Méar, Y., Murat, A., Dominique Davoult, D., Migné, A., 2011. Sampling Epifauna, 

a Necessity for a Better Assessment of Benthic Ecosystem Functioning: An Example of the Epibenthic 

Aggregated Species Ophiothrix fragilis from the Bay of Seine. Marine Pollution Bulletin 62, 2753-2760. 

Méar, Y., Poizot, E., Murat, A., Lesueur, P., Thomas, M., 2006. Fine-grained sediment spatial distribution 

on the basis of a geostatistical analysis: Example of the eastern Bay of the Seine (France). Continental 

Shelf Research 26, 2335-2351. 

Warner, G.F., Woodley, J., 1975. Suspension-feeding in the brittle star Ophiothrix fragilis. Journal of the 

Marine Biological Association of the United Kingdom 55, 199-210. 

32


MILANKOVITCH-SCALE ORBITALLY FORCED TIDAL CYCLICITY 

Poppe DE BOER 

DEPT OF EARTH SCIENCES, P.o. box 80.021, 33508TA, Utrecht, The netherlands, P.L.deBoer@uu.nl 

Milankovitch-scale variations in insolation affect climate and oceanography, and contribute 

to the generation of cyclic sedimentary successions, especially at critical latitudes. Common 

oceanographic principles show that also the ocean tide responds to variations in the orbital 

parameters (de Boer and Trabucho-Alexandre, 2012). Variations of the ocean tide, due to 

changing eccentricity (at present 0•0165; theoretical maximum 0•0728) and precession affect a 

variety of oceanographic and related sedimentary processes. Having the same frequency, their 

effects may be mixed up with, blurred by, or add to the insolation effects. Gravitation-dependent 

variations of the tide are related to the third power of the distance to the Sun. Insolation only has 

a quadratic relation. Thus the tidal effects should be felt especially in periods of high eccentricity. 

Variations of the ocean tide due to the, much shorter, 18•6 year lunar nodal cycle, which 

has no insolation counterpart by which they may be obscured, produce relatively small, order of 

5%, variations of tidal amplitude and tidal currents. This leads to significant effects in sedimentary 

environments that are sensitive to variations in the strength of the tide. For example, progradation 

and retreat of tropical coastlines (Gratiot et al., 2008), ebb-tidal delta behaviour and erosion and 

sedimentation on adjacent barrier islands (Oost et al., 1993), the morphodynamics of estuaries 

(Wang and Townend, 2012), mean-sea-level changes (Peterson, 1988), and Arctic climate and 

fishery stocks (Yndestad et al., 2008) have been related to the effects of the Lunar Nodal Cycle. 

Orbital variations of the tide on Milankovitch time scales are stronger than those due to the 

18•6 year lunar nodal cycle. They also should affect sedimentary systems. In the Quaternary and 

other ice-house periods, rapid sea-level changes may blur such effects. In greenhouse periods 

when sea-level changes are slower by 2 to 3 orders of magnitude, the preservation potential of 

sedimentary signals of orbitally forced variations of the ocean tide likely is greater. In such 

periods, variations of the ocean tide may affect the behaviour of barrier coastlines, delta lobe 

switching, carbonate platform evolution and processes in the open ocean related to circulation 

intensity. Especially in cases in which the period of autocyclic changes approaches that of 

precession or eccentricity, orbital variations of the tide may tune cyclic changes in tide-influenced 

sedimentation patterns. 

In analogy with the lunar nodal cycle, semi-precession cycles are to be expected not only at 

low latitudes, as is the case with insolation, but also at high latitudes. 

33


de Boer, P.L. and Trabucho-Alexandre, J. (2012) Orbitally forced sedimentary rhythms in the stratigraphic 

record: is there room for tidal forcing? Sedimentology, 59, 379-392. 

Gratiot, N., Anthony, E.J., Gardel, A., Gaucherel, C., Proisy, C. and Wells, J.T. (2008) Significant 

contribution of the 18.6 year tidal cycle to regional coastal changes. Nature Geoscience, 

doi:10.1038/ngeo127, 1-4. 

Oost, A.P., Dehaas, H., IJnsen, F., Vandenboogert, J.M. and de Boer, P.L. (1993) The 18.6 Yr Nodal Cycle 

and Its Impact on Tidal Sedimentation. Sedimentary Geology, 87, 1-11. 

Peterson, R.G. (1988) Comparisons of sea level and bottom pressure measurements at Drake Passage. 

Journal of Geophysical Research, 93, 12439-12448. 

Wang, Z.B. and Townend, I.H. (2012) Influence of the nodal tide on the morphological response of 

estuaries. Marine Geology, 291–294, 73-82. 

Yndestad, H., Turrel, W.R. and Ozhigin, V. (2008) Lunar nodal tide effects on variability of sea level, 

temperature and salinity in the Faroe-Shetland Channel and the Barents Sea. Deep-Sea Research I, 55, 

1201-1217. 

34


TIDAL INFLUENCE IN THE ‘LOWER RED UNIT’ OF THE TREMP FM IN 

SOUTH-CENTRAL PYRENEES (LATE CRETACEOUS-TERTIARY) 

Davinia DIEZ-CANSECO*, M. Isabel BENITO*, Margarita DIAZ-MOLINA*, Otto KALIN** 

*STRATIGRAPHY DPT.-COMPLUTENSE UNIV. OF MADRID-IGEO (CSIC-UCM), José Antonio Novais 2, 

28040, Madrid, Spain, davigeo2@gmail.com 

**PALEONTOLOGY DPT.-COMPLUTENSE UNIV. OF MADRID-IGEO (UCM-CSIC), José Antonio Novais, 

2, 28040, Madrid, Spain 

Interpreting transitional depositional environment is a difficult task when the ocurrence of 

sedimentary features associated with continental environments, such as reddish-coloured 

mudstone with abundant paleosols are profuse, and there is scarcity or lack of sedimentary 

features and/or fossil content indicative of marine influence. This study presents an example of a 

transitional environment recorded in the Late Cretaceous red deposits of the Tremp Fm in the 

south-central Pyrenees, which traditionally have been considered as continental, but display 

evidence of tidal influence. 

The studied area is located in the south-central Pyrenees, at the eastern part of the 

northern flank of the east–west-trending Tremp syncline, near Suterranya. This syncline exposes 

Late Cretaceous-Tertiary deposits reflecting deepening to the west, with a transition from 

continental to shelf and turbidite facies. In this area, Late Cretaceous-Tertiary succession is 

represented by the Arén Fm, composed mainly of sandstone, which is overlain by the Tremp Fm 

composed of predominantly mudstone and subordinate sandstone (Fig. 1 a). These formations 

contain various worldwide known dinosaur fossil sites (Fig. 1 b), which are among the youngest in 

the world (López-Martínez et al., 2001). The Cretaceous–Tertiary boundary is enclosed within the 

lower part of Tremp Fm, although its precise location has not been well established yet. 

The stratigraphic succession at Suterranya includes the top of the Aren Fm and the lower 

portion of the Tremp Fm. The Aren Fm consists of shallow-marine sandstones interpreted as 

beach ridge deposits (Diaz-Molina et al., 2007). This is followed by the Tremp Fm, commonly 

known as the “Garumnian facies”. In the sections studied, the Tremp Fm consists of greyish 

mudstones with abundant pedogenic features (‘Grey Unit’), interpreted as lagoonal or estuarine 

facies.These are followed by reddish to yellowish silty mudstones interbedded with channelized 

sandstone and conglomerate (‘Lower Red Unit’), that have been interpreted as fluvial and flood 

plain deposits (Rossell et al., 2001; Riera et al., 2009). These deposits are overlain by lacustrine 

limestones, which have been attributed to the Danian (López-Martínez et al., 2006). 

Interestingly, several indications of a marine influence have been detected in both the 

‘Lower Red Unit’ and the lacustrine carbonate facies. For example, despite the abundant 

pedogenetic features, such as carbonate nodules precipitaction, reddish to yellowish mottling and 

rhizolites (Fig. 2 a), the reddish-yellowish silty mudstones are intensely burrowed (Fig. 2 a and b) 

and contain abundant planktonic foraminifers and calcareous nannoplankton, which do not show 

any sign of having been reworked from older formations (Fig. 2 c, d, e and f). Moreover, the 

lacustrine limestones overlying reddish-yellowish siliciclastic deposits contain abundant benthonic 

foraminifers. 

Sandstone bodies in the ‘Lower Red Unit’ are made up of coarse- to fine-grained hybrid 

arenites, with interbedded silty mudstones and conglomerates. Their geometry is tabular or 

convex upwards and they are interpreted as point bar bodies. Individual point bar bodies may 

reach 2 m in thickness and typically display Inclined Hetherolitic stratification (IHS, Fig. 3), in 

cases intensely burrowed and pedogenetically altered, mainly at the top. Point bar bodies of the 

same meander loop are separated by discordances or meander loop reactivation surfaces. The 

convex-upward-shaped bodies represent longitudinal sections trough point bars. IHS deposits are 

interpreted as products of point bar lateral accretion, formed in meandering channels with tidal 

influence (sensu Thomas et al., 1987). 

Both, marine fauna found in the silty mudstones and the presence of HIS in sandstone 

bodies strongly suggest that the ‘Lower red Unit’ of the Tremp Fm consists of mudflat deposits 

incised by meandering channels with tidal influence. Moreover, the presence of abundant 

foraminifers in the overlaying lacustrine limestones corroborates the interpretation of a marine 

influence in the ‘Lower Red Unit’ of the Tremp Fm. This is in line with the tidal flat environmental 

setting for dinosaur nesting proposed by Sanz et al. (1995) and López-Martínez et al. (2000). 

35


1/ (a) Mudstone with interbedded sandstone of Tremp Fm. (b) Dinosaur bone remain in the Tremp Fm. 2/ 

Reddish-yellowish silty mudstone facies (‘Lower Red Unit’, Tremp Fm). (a) Burrows and reddish to 

yellowish mottling. (b) Detail of a single burrow. (c and d) Planktonic foraminifers. (e and f) Calcareous 

nannoplankton. 3/ Two superimposed point bars bodies (‘Lower Red Unit’, Tremp Fm). Note IHS in the 

lower body. 

Díaz Molina, M., Kälin, O., Benito, M.I., López-Martínez, N., Vicens, E., 2007. Depositional setting and early 

diagenesis of the dinosaur eggshell-bearing Arén Fm at Bastús, Late Campanian, south-central Pyrenees. 

Sedimentary geology 199, 205–221. 

Lopez-Martinez, N., Moratalla, J.J., Sanz, J.L., 2000. Dinosaur nesting on tidal flats. Palaeogeography, 

Palaeoclimatology, Palaeoecology 160, 153–163. 

Lopez-Martinez, N., Canudo, J.I., Ardèvol, L., Pereda Suberbiola, X., Orue-Etxebarría, X., Cuenca-Bescós, 

G., Ruiz Omeñaca, J.I., Murelaga, X., Feist, M., 2001. New dinosaur sites correlated with Upper 

Maastrichtian pelagic deposits in the Spanish Pyrenees: implications for the dinosaur extinction pattern in 

Europe. Cretaceous Research 22, 41–61. 

López-Martínez, N., Arribas, M.E., Robador, A., Vicens, E., Ardèvol, Ll. Los carbonatos danienses (Unidad 

3) de la Fm Tremp (Pirineos Sur-centrales): Paleogeografía y relación con el límite Cretácico-Terciario. 

Revista de la Sociedad Geológica de España 19 (3-4). 

Rosell, J., Linares, R. & Llompart, C., 2001. El “Garumniense prepirenaico”. Rev. Soc. Geol. Esp. 14 (1-2). 

Sanz, J.L., Moratalla, J.J., Díaz-Molina, M., Lopez-Martinez, N., Kälin, O., Vianey-Liaud,M., 1995. Dinosaur 

nests at the sea shore. Nature 376, 731–732. 

Thomas, R.G., Smith, D.G., Wood, J.M., Visser, J., Calverlyrange, E.A., Koster, E.H., 1987, Inclined 

heterolithic stratification; terminology, description, interpretation and significance: Sedimentary Geology v. 

53, p. 123–179. 

Riera, V., Oms, O., Gaete, R., Galobart, À., 2009. The end-Cretaceous dinosaur succession in Europe: the 

Tremp basin record (Spain). Palaeogeography, Palaeoclimatology, Palaeoecology 283, 160–171. 

36


DEPOSITIONAL ARCHITECTURE AND ICHNOLOGY OF THE TIDALLY-INFLUENCED 

ESTUARINE SYSTEM OF THE EOCENE AMEKI GROUP 

Ogechi EKWENYE*, Gary NICHOLS*, Sunny NWAJIDE**, Gordian OBI*** 

*DEPARTMENT OF EARTH SCIENCES, Royal, TW20 0EX, London, United kingdom, 

sedogechy@yahoo.com, Gary.Nichols@rhul.ac.uk 

**SITP, Shell Development Company Limited, 320242, Nigeria, sunny_nwajide@yahoo.com 

***DEPARTMENT OF GEOLOGY, Anambra State University, 430261, Anambra, Nigeria, 

gordianobi@yahoo.com 

The Eocene siliciclastic sedimentary facies of the Ameki Group in the south-eastern Nigeria 

records sedimentary response to an initial regression, followed by marine incursion 

(transgression) into the pro-Niger Delta basin. Detailed studies of several well-exposed sections 

of the Eocene Ameki Group (Figure 1) within an outcrop area of over 1,800 km2 show that 

deposition took place in a setting that varied from coastal to shallow marine. Detailed 

sedimentological and ichnological studies indicate that the overall setting was of a tidally 

influenced estuarine system. This interpretation is similar to the description of tide-dominated 

estuary (Dalrymple, 1992; Kitazawa, 2007), where a complete preservation of transgressive 

valley-fill sediments consist of fining upward sequence from fluvial sands and/or gravel to 

interbedded sands and muds deposited in the tidal fluvial transition of inner estuary. This is 

followed by upward coarsening fine grained sand flats sediments and cross bedded sandstone of 

elongate tidal sand bars. 

Six facies associations (FA1 to FA6) are documented in the study area with well preserved 

sediments interpreted as fluvial channel, tidally influenced fluvial channel, tidal channel, tidal flats, 

tidal sand bar and tidal/shallow marine embayment deposits. Facies distribution in the Ameki 

Group is similar to that of the Cobequid Bay-Salmon River macrotidal estuary, Bay of Fundy 

(Dalrymple, et. al. 1990), where the tidal channels and tidal sand bars are bordered by tidal flats. 

Architectural element analysis is applied to determine the basic building blocks of the estuarine 

succession and to show the spatial arrangement and continuity of sandstone bodies. The 

architectural elements are grouped into channels, non-channels and heterolithic elements. 

Two major temporal controls were responsible for the formation of the non-cyclic and cyclic 

rhythmites and other tidally-influenced depositional structures observed in the study area. Tidal 

depositional cycles include semi-diurnal tidal rhythmites are recognised in tidal bundles and 

millimetre-centimetre scale heteroliths whereas decimetre-metre scale cyclic successions indicate 

seasonal depositional cycles. Similar interpretation is observed in the works of Hovikoski et al., 

2008, where they discussed the tidal and seasonal controls of the Upper Miocene sediments of 

the Acre sub-basin, Brazil. The tidal deposits are associated with ichnofacies assemblages of 

Skolithos, Cruziana, mixed Skolithos-Cruziana, Glossifungites and Teredolites ichnofacies that 

show variation in intensity and diversity across the facies. The depositional architecture of the 

Eocene Ameki Group has been most probably controlled by relative sea-level changes, sediment 

supply, basin accommodation and regional tectonics consequent upon the location of the Niger 

Delta at the edge of a trailing continental plate. 

37


Geologic map of the study area showing the outcrop locations in the Ameki Group 

Dalrymple, R.W. 1992, Tidal depositional systems in Walker, R. G. and James, N. P., eds., Facies Models: 

response to sea level change: Geological Association of Canada, p.195-218. 

Dalrymple, R.W., Knight, R. J., Zaitlin, B. A. and Middleton, G.V., 1990, Dynamics and facies model of a 

macrotidal sandbar complex, Cobequid Bay-Salmon River estuary (Bay of Fundy): Sedimentology, v. 37. p. 

577-612. 

Hovikoski, J., M. Rasanen, and Gingras, M, Ranzi, A, and Melo, J., 2008, Tidal and seasonal controls in the 

formation of Late Miocene inclined heterolithic stratification deposits, western Amazonian foreland basin: 

Sedimentology, v. 55, p. 499-530. 

Kitazawa, T., 2007, Pleistocene macrotidal tide-dominated estuary–delta succession, along the Dong Nai 

River, southern Vietnam: Sedimentary Geology, v. 194, no. 1–2, p. 115-140. 

38


SEDIMENTATION PROCESSES AND SEDIMENTARY CHARACTERISTICS OF TIDAL 

BORES IN THE QIANTANG ESTUARY, EAST-CENTRAL CHINA 

Daidu FAN, Shuai SHANG, Jinbiao TU, Guofu CAI, Yijing WU 

STATE KEY LAB OF MARINE GEOLOGY, 605# Ocean Building, 1239 Siping Road, 200092, Shanghai, 

China, ddfan@tongji.edu.cn 

A tidal bore is a unique Earth surface process, characterized by its highly destructive 

energy, predictable periodicities and magnitudes, and the production of characteristic 

sedimentary features. Tidal bores and associated rapid flood flows are highly turbulent flows of 

the upper-flow regime with a velocity over several meters per second. Reynolds (Re) and Froude 

(Fr) numbers, respectively, are larger than 104 and 1.0, making them significantly different from 

regular tidal flows but analogous to turbidity currents. Until now, understanding of tidal-bore 

depositional processes and products has been limited because of the difficulty and hazards 

involved with gauging tidal bores directly. The Qiantang bore is known as the largest breaking 

bore in the world. Field surveys were carried out in May 2010, along the north bank of the 

Qiantang Estuary to observe the occurrence of peak bores, including regular observations of 

current, water level and turbidity at the main channel. Several short cores were sampled on the 

intertidal flats to study the characteristic sedimentary features of tidal bores. 

Hydrodynamic and sedimentological studies show that the processes of sediment 

resuspension, transport and deposition are controlled primarily by the tidal bores, and the 

subsequent abruptly accelerated and decelerated flood flows, which only account for one tenth of 

each semidiurnal tidal cycle in the estuary. The asymmetry between the flooding and ebbing 

phases of tides in the Qiantang Estuary is extraordinary. For example, an ebb duration of more 

than 10 hours is approximately four times the flood duration of more than 2 hours observed during 

the spring tides at Daquekou. The maximum near-bottom (1 m above the bed) velocities for this 

period were 0.7 and 2.1 m/s for the ebb and flood flows, respectively, with the latter being three 

times the former. The maximum turbidity variation usually occurs at the same moment as the 

passage of the bore-head, and a few minutes ahead of the maximum flooding regime. The 

hydraulic observations at Daquekou showed that the suspended concentration jumped sharply 

from a minimum value in the range of 0–50 NTU to 1300–1800 NTU within one or two minutes 

before and after the bore. During the following stage, vast amounts of suspended sediments 

should be deposited rapidly because of a sharp deceleration of flood flows. This lasted only 30 

minutes with a drastic drop of turbidity from ~1800 NTU to ~450 NTU according to our single field 

observation. After these first two stages, absolute values of flow speeds and their variation 

magnitudes were relatively small. A maximum speed of 0.7 m/s occurred at the rapid ebbing 

stage, but its general competence to resuspend sediments was presumably low and the 

suspended sediment concentration was not observed to increase significantly either. The 

suspended sediment concentration fluctuated between 300 NTU and 500 NTU for a long time 

following the slow flooding stage, and declined toward zero from the late slow ebbing stage to the 

slack stage. In short, sedimentation in the bore-affected section of the river is mainly controlled by 

the tidal bore and closely related processes, including the abrupt rise in water level, and the rapid 

increase and decrease in flow velocities during and immediately after the passing of the tidal 

bore. 

Rapid sedimentation occurs at the sharply decelerated flooding stage, producing poorly 

sorted deposits characterized by massive bedding, graded bedding and basal scour structures. 

Soft-sediment deformation structures are also developed, including convoluted bedding and 

dewatering structures. These occur because of the liquefaction of newly deposited beds that 

contain abundant pore water, triggered by the passage of the bore above. The C-M graphic 

interpretation demonstrates that the sediments are mainly transported as suspended loads with 

only a slight amount of bed load under fierce vortex turbulence in the bore-affected river section. 

The differences between tidal-bore and regular tidal deposits are evident not only in sedimentary 

structures, with the former having characteristic thick massive beddings and the latter commonly 

developing with tidal beddings (lenticular, wavy and flaser beddings), mud couplets, and 

spring-neap tidal cycles, but also in the grain size composition. Scattering plots of any two 

grain-size parameters have the potential to differentiate the three kinds of tidal deposition: TBD 

(tidal bore deposit), TSD (tidal sandy deposits) and TMD (tidal muddy deposit), with some general 

trends in terms of mean grain size with TBD>TSD>TMD, sorting of TMD>TBD>TSD (larger value 

indicating poorer sorting), and both skewness and kurtosis with TSD>TBD>TMD. 

39


Acknowledgement: This work was jointly supported by National Natural Science Foundation 

of China (40876021, 41076016), State Key Lab of Marine Geology (MG200907), SOA Key Lab of 

Marine Sedimentology & Environmental Geology (MASEG200802), the Special Research Fund 

for the Doctoral Program of Higher Education (20090072110004) and the Fundamental Research 

Funds for the Central University. 

Photographs of short cores with sampling locations and characteristic sedimentary structures indicated 

(JS1–JS5, DQK1, DQK2). Green and pink circles or squares denote the sampling locations on muddy and 

sandy layers, respectively, with sample numbers marked nearby; horizontal pink arrows denote tidal-bore 

depositional layers; green and blue arrows point to scour structures and water-escape structures, 

respectively; S and N represent the spring and the neap tides, respectively (in Fan et al., 2012). 

40


INFLUENCE OF TIDE VS WAVE ON SEDIMENT DYNAMICS AND DUNE INTERNAL 

ARCHITECTURE ON A MACROTIDAL INNER CONTINENTAL SHELF (EASTERN 

ENGLISH CHANNEL) 

Yann FERRET*, Sophie LE BOT**, Robert LAFITE**, Olivier BLANPAIN**, Thierry GARLAN*** 

*MARUM - CENTER FOR MARINE ENVIRONMENTAL SCIENCES, Leobener Strasse 2, 28359, Bremen, 

Germany, yferret@marum.de 

**UMR CNRS 6143 M2C, UNIVERSITE DE ROUEN , Place Emile Blondel, 76821, Mont Saint Aignan, 

France 

***SHOM, 13 rue du Chatellier, 29200, Brest, France 

Seabed of continental shelf environments is regularly covered with a multitude of bedforms 

formed in response to interactions between fluid dynamics and sediment. These mobile 

sedimentary features have been widely studied in order to prevent damages on human activities 

and anthropogenic structures. In coastal areas, submarine dune dynamics is mainly controlled by 

tidal currents and wind and wave forcings (e.g. Le Bot et al., 2004; Idier et al., 2011). However, it 

is generally not obvious to distinguish which forcing is predominant in dune dynamics. 

In a previous study mainly based on seismic measurement analyses, Ferret et al. (2010) 

highlighted that both long-term tidal oscillations and inter-annual to decennial variability of storm 

activity could be responsible for the dynamics and internal architecture of dunes (height: 2-10.5m, 

wavelength: 250-1800m) in the Eastern English Channel. If storms are considered as major 

events, authors assume that they can be strong enough to reverse dune migration direction, and 

form second-order erosive reflectors (Figure 1). The present study aims to verify this assumption 

by quantifying the wave influence on the dynamics of heterogeneous sediment (mixture of sand 

and gravel). The final objective is to get wave thresholds above which an inversion of the direction 

of sediment transport is calculated. 

For this purpose, two oceanographic surveys, conducted in 2007 and 2008, allow to realize 

current measurements (ADP and ADV) and sediment samples, in order to calculate sediment 

fluxes and to quantify sediment dynamics. In this study, only bedload sediment transport is 

considered since it is generally accepted as the dominant transport mode responsible for dune 

dynamics. Calculations have been realized for tide- and wave-combined conditions by using a 

non-uniform sediment transport formulae developed by Wu et al. (2000), and considered to be the 

most suitable for the heterogeneous sediments in the Channel (Blanpain, 2009). 

Calculated sediment fluxes are almost only concerned with fine and medium sands. From 

measurements, we see that storm waves (HS>2m) can: (1) initiate bedload sediment transport 

where it is inexistent under fair tidal conditions (neap tides), or (2) strongly increase the quantities 

of sands transported by tidal currents (medium sands in particular). Sediment fluxes are up to ten 

times higher compared to mild conditions. Moreover, we also noted that waves can reverse the 

direction of the residual sediment transport induced by tide, and subsequently be responsible for 

the formation of second-order reflectors. 

Strong storm events have not been experienced during this time. Indeed, significant wave 

heights are not very high, and wavy conditions took place only for several hours. In order to 

quantify the impact of waves on sediment transport, sediment fluxes have been calculated over a 

spring tide semi-diurnal cycle by simulating different wave conditions: Hs from 0m (tidal forcing 

only) to 6m (decennial wave height). Thus, it has been possible to identify a wave height 

threshold above which direction of sedimentary fluxes is reversed: it varies from 1.7 to 2.8 m, 

according to the studied sector. These values are lower than local annual wave height (4.2 m), 

indicating that several second-order reflectors are formed per year. Compared to the formation 

occurrence estimated from seismic records for second-order reflectors (4 to 18 years ; Ferret et 

al., 2010), it is obvious that only few of them are preserved due to strong eroded volumes. 

41


Example of typical dune internal architecture observed off the Normandy coast (Eastern English Channel): 

(A) 3•5 kHz seismic profile and (B) its interpretation. 1 and 2 indicate first- and second-order reflectors. 

Blanpain, O. 2009. Dynamique sédimentaire multi-classe : de l'étude des processus à la modélisation en 

Manche. PhD thesis, Université de Rouen. 315 pp. 

Ferret, Y., Le Bot, S., Tessier, B., Garlan, T. and Lafite, R. 2010. Migration and internal architecture of 

marine dunes in the Eastern English Channel over 14 and 56 year intervals: the influence of tides and 

decennial storms. Earth Surface Processes and Landforms 35: 1480-1493.. 

Idier, D., Astruc, D. & Garlan,T. 2011. Spatio-temporal variability of currents over a mobile dune field in the 

Dover Strait. Continental Shelf Research 31 (19–20): 1955-1966. 

Le Bot, S. and Trentesaux, A. 2004. Types of internal structure and external morphology of submarine 

dunes under the influence of tide- and wind-driven processes (Dover Strait, northern France). Marine 

Geology, 211(1-2): 143-168. 

Wu, W., Wang, S.S.Y. and Jia, Y. 2000. Non-uniform sediment transport in alluvial rivers. Journal of 

Hydraulic Research, 38: 427-434. 

42


THE ORDOVICIAN TABLE MOUNTAIN GROUP, SOUTH AFRICA: THE TIDAL 

DEPOSIT THAT NEVER WAS 

Burghard W. FLEMMING 

SENCKENBERG, Suedstrand 40, 26382, Wilhelmshaven, Germany, bflemming@senckenberg.de 

In the Ordovician Cape Basin, South Africa, the Table Mountain Group commences at its 

base with a ca. 800-m-thick conglomeratic coarse-grained sandstone (Piekenierskloof Formation), 

followed by 440 m of interbedded quartzarenites and silt-/mudstones locally containing marine 

trace fossils (Graafwater Formation), and 1,800 m of medium- to coarse-grained, supermature 

quartzarenites (Peninsula Formation), which frequently display floating pebbles and which are 

occasionally interrupted by several decimetre-thick pebble beds. Within a few thin sequences the 

quartzarenites display marine trace fossils (Rust, 1973). The latter is capped by a 120-m-thick 

sequence comprising sandstones, conglomerates and a diamictite (Pakhuis Formation). The 

succession as a whole has been interpreted as representing, from north to south, a prograding 

alluvial fan, braid plain/fan delta to shallow-marine deposit in a mesotidal setting (Fig. 1a; Visser, 

1974; Tankard et al., 1982), the latter being supposedly well exposed in the up to 800-m-thick 

sedimentary succession preserved in the Cape Peninsula which is located along the western 

margin of the Cape Basin (Tankard and Hobday, 1977; Hobday and Tankard, 1978; Tankard et 

al., 1982). 

A closer look at the criteria, however, reveals that, as far as the exposures on the Cape 

Peninsula are concerned, the above interpretation is mostly based on circumstantial evidence, 

none of the sedimentary structures described in the literature being exclusively or uniquely 

diagnostic of tidal environments, although it is undisputed that sporadic trace fossils documented 

from a few discrete horizons were produced by marine organisms. With the exception of these 

horizons, the majority of sedimentary structures and other features overwhelmingly favour an 

alluvial braid-plain/fan-delta setting which experienced a number of marine incursions. Among the 

structures and features are sand-filled mud cracks more typically associated with desiccation after 

episodic flooding rather than regular tidal emergence (Turner, 1986); the ubiquitous occurrence of 

floating pebbles in cross-bedded sets; the intercalation of several decimetre-thick pebble beds; 

stacked linguoid bars typical of distal braid-plain environments; the frequency and scale of 

deformation structures, including overturned large-scale cross-beds (up to 10 m high!); the 

absence or very rare occurrence of true herringbone structures; the total absence of neap-spring 

tidal bundle sequences even in large cross-bedded sets; and last but not least, the large 

thickness of the sedimentary succession which is quite atypical of tidal deposits. On account of 

these inconsistencies, the tidal origin of the lower Table Mountain Group deposits was already 

questioned by Fuller (1984), Turner (1986), Flemming (1988), and Hiller (1992). 

In order to reconcile the entire suite of observed sedimentary structures and other features 

with an appropriate depositional environment, it is proposed that the Table Mountain Group 

sediments were deposited to the south of an escarpment on a very broad (several 100 km wide), 

gradually sloping coastal plain with the shoreline situated south of the Cape Peninsula, but with 

some deeper channels within the reach of the high tide (Fig. 1b). Initially, the coastal plain was 

encroached by alluvial fans fed by material derived from Precambrian rocks exposed in the not 

too distant hinterland to the north, as revealed by the mineralogical composition. The proximal, 

conglomeratic deposits of these fans define the Piekenierskloof Formation. The distal parts ended 

in shallow, playa-type water bodies which seasonally dried up to produce the mud-cracked 

successions of the Graafwater Formation which were capped by thin sand sheets during 

subsequent flood seasons (Turner, 1986). This basal sequence, which was occasionally 

inundated by the sea, was then (quite suddenly) overridden by huge supplies of glacial outwash 

sands derived from the margin of the polar ice sheet which, in Ordovician times, was located 

several thousand kilometres to the north. 

The large transport distance explains the supermature nature of the sands, while the large 

water masses released from the glaciers in summer are compatible with the overall high-energy 

depositional character. Large downstream migrating bedforms in up to several 10s of metres 

deep channels incised into the middle to distal fan-delta deposits produced the up to several 

metres thick cross-bedded sets. The distal braid-plain probably merged with the coastal ocean to 

the south. Subsidence and temporary interruptions in sediment supply were associated with 

occasional marine transgressions across the lower fan-delta, the invading marine organisms 

leaving their traces in discrete marine-influenced sedimentary successions. During Silurian times 

the southward shifting ice sheet eventually emplaced the diamictite at the top of the succession. 

43


a) Schematic illustration of the depositional environments proposed by Tankard et al. (1982) for the lower 

Table Mountain Group sedimentary succession. b) Alternative braid-plain/fan-delta interpretation proposed 

here. The Cape Peninsula would be located in a middle to distal position on the fan. 

Flemming, B.W., 1988. Evidence for a fluvial rather than tidal origin of the lower Table Mountain Group 

sedimentary succession (Ordovician Cape basin, South Africa). Terra Cognita, 8, p. 30. 

Fuller, A.O., 1984. A contribution to the conceptual modelling of pre-Devonian fluvial systems. Trans. Geol. 

Soc. SA. Afr. 88, 189–194. 

Hiller, N., 1992. The Ordovician System of South Africa: a review. In: Webbey, B.D., Laurie, J.R. (eds), 

Global perspectives on Ordovician geology. Balkema, Rotterdam, pp. 473–485. 

Hobday, D.K., Tankard, A.J., 1978. Transgressive-barrier and shallow-shelf interpretation of the lower 

Paleozoic Peninsula Formation, South Africa. Geol. Soc. Am. Bull. 89, 1733–1744. 

Tankard, A.J., Hobday, D.K., 1977. Tide-dominated back-barrier sedimentation, early Ordovician Cape 

Basin, Cape Peninsula, South Africa. Sediment. Geol. 18, 135–159. 

Tankard, A.J., Jackson, M.P.A., Eriksson, K.A., Hobday, D.K., Hunter, D.R., Minter, W.E.L., 1982. Crustal 

evolution of Southern Africa – 3.8 billion years of Earth history. Springer-Verlag, New York, 523 pp. 

Turner, B.R., 1986. Environmental significance of desiccation cracks in the Early Ordovician Graafwater 

Formation, Cape Peninsula, South Africa. Geocongress ’86, Geol. Soc. S. Afr., Extended Abstracts, pp. 

433–435. 

Rust, I.C., 1973. The evolution of the Paleozoic Cape Basin, southern margin of Africa. In: Nairn, A.E.M., 

Stehli, F.G. (eds), The ocean basins and margins, I. The South Atlantic. Plenum Press, New York, pp. 

247–276. 

Visser J.N.J., 1974. The Table Mountain Group: a study in the deposition of quartz arenites on a stable 

shelf. Trans. Geol. Soc. S. Afr. 77, 229–237. 

44


OBSERVATIONAL EVIDENCE FOR THE INWARD TRANSPORT OF SUSPENDED 

MATTER BY ESTUARINE CIRCULATION IN THE WADDEN SEA 

Goetz FLOESER*, Hans BURCHARD**, Rolf RIETHMUELLER* 

*HELMHOLTZ ZENTRUM, Max-Planck-strasse 1, 21502, Geesthacht, Germany, floeser@hzg.de, 

riethmueller@hzg.de 

**BALTIC SEA RESEARCH INSTITUTE, Seestrasse 15, 18119, Warnemuende, Germany, 

hans.burchard@io-warnemuende.de 

Observational evidence is presented that corroborates several predictions of the theory of 

estuarine circulation in the Wadden Sea. Current velocity data from moored ADCPs and ship 

cruises, turbulence measurements and SPM transport measurements from several locations in 

the Wadden Sea were analyzed. As a general result, the vertical current profiles and turbulence 

indicators show features concurring with the predictions of the theory. One more consequence is 

that these current features must lead to a residual outflow of Wadden Sea waters in the upper 

part and a residual inflow of water in the lower part of the water column, thus giving a generic 

explanation for the obvious net import of suspended sediments from the German Bight into the 

Wadden Sea. 

The predictions of Burchard’s theory (Burchard, 2008) concerning estuarine circulation 

concern a) current velocity profiles, b) turbulence indicators like mass diffusion and turbulent 

kinetic energy dissipation, c) the salinity difference between surface and bottom waters and d) the 

entire suspended matter transport in the water column. For all items, confirmations could be 

found in several locations of the Wadden Sea. 

For the case of current velocity, measurements from moored (from 2002 through 2009) and 

ship-bound ADCPs were analyzed along with conductivity and temperature measurements from 

which the density gradient was derived. The current velocity profiles were averaged and fitted to a 

logarithmic function. The curvatures of ebb and flood current were used and compared to the 

predictions. 

Becherer et al. (2011) analyzed turbulence measurements from a campaign in the Lister 

Deep in April 2008 and found a confirmation of the theory’s predictions: destratification during 

flood and increased stratification during ebb. 

In May 2011, a ship campaign was done in the backbarrier Wadden Sea area of Spiekeroog 

Island with concentrated measurements of current velocity, suspended matter and turbulence 

measurements. 

With these results from several regions of the Dutch and German Wadden Sea, we 

consider our hypothesis of the presence of estuarine circulation in the Wadden Sea as confirmed. 

Future investigations will concentrate on the effect of this kind of circulation on vertically resolved 

suspended matter transport. 

45


Map of the locations where data were collected in the German and Dutch Wadden Sea 

Becherer, J., Burchard, H., Flöser, G., Mohrholz, V., and Umlauf, L. (2011). Evidence of tidal straining in 

well-mixed channel flow from microstructure observations. Geophysical Research Letters 38, L17611 

Burchard, H., Flöser, G., Staneva, J.V., Badewien, T.H., Riethmüller, R. (2008). Impact of density gradients 

on net sediment transport into the Wadden Sea. J. Phys. Oceanogr., 38, 566-587. 

Flöser, G., Burchard, H., Riethmüller, R. (2011). Observational evidence for estuarine circulation in the 

German Wadden Sea. Cont. Shelf Res. 31, 1633-1639. 

46


EVOLUTION AND STRATIGRAPHY OF A HOLOCENE MICRO-TIDAL BARRIER 

SYSTEM IN THE NORTHERN WADDEN SEA 

Mikkel FRUERGAARD, Thorbjørn Joest ANDERSEN, Lars Henrik NIELSEN, Peter N. 

JOHANNESSEN, Morten PEJRUP 


Denmark, mif@geo.ku.dk 

Introduction 

Barrier islands only occupies about 15% of the world’s coastlines but along the Atlantic and 

Gulf coasts of the United States and the NW European Wadden Sea coast they are a very 

common feature. Barrier islands are considered very important areas both economically and 

recreational and they are often densely populated. Many modern barrier islands may however be 

threatened by the rising global eustatic sea level and there is an increasing concern for the future 

development of barrier islands (FitzGerald et al., 2008). Several studies have investigated the 

evolution of barrier islands (e.g. Heron et al., 1984; Moslow and Heron, 1981) in relation to the 

Holocene sea level rise. Common for many of these studies are that 14C dating was applied to 

establish the time frame of barrier island sedimentation. This is often problematic due to the low 

content of applicable organic material in many barrier island deposits. This study uses optically 

stimulated luminescence (OSL) dating, which enables direct age-determination of sandy deposits 

and together with sedimentological facies interpretations aims to set up a model accounting for 

the development of the barrier island in relation to the Holocene sea level rise. 

Research area 

The Skallingen-Langli complex is located in the Northern part of the Danish Wadden Sea 

(Fig. 1). The complex consists of the NW-SE situated barrier-peninsula of Skallingen (c. 22 km2) 

and the smaller island of Langli (c. 1 km2) situated in the back-barrier area east of Skallingen. 

The area is influenced by semidiurnal tides with a mean tidal range of about 1.3 m and the west 

coast of Skallingen is subject to a moderately-high energy wind climate from the North Sea with a 

mean annual wave height of about 1 m (Nielsen and Nielsen, 2006). Extreme storms occasionally 

contribute to the astronomical tidal range with more than 4 m of wind set-up. 

Method 

Five wells ranging in depth from 10 to 22 m were cored and 92 sediment samples were 

collected to create a detailed absolute chronology using OSL dating (Madsen et al., 2005). This 

method determines the time of the last light exposure of the sediment which generally 

corresponds to the time of deposition. OSL dating is especially suited when working with sandy 

sediments deposited within the last ~100.000 years. Sedimentological descriptions of the cores 

were carried out and the interpretation of the depositional environments were based on key 

characteristics as lithology, grain-size, structures, amount of bioturbation, amount and maximum 

size of pebbles and trace fossils. 

Results 

Based on sediment facies logs from the core wells 10 depositional units each representing 

a depositional environment have been identified in the Skallingen-Langli barrier complex. These 

are: Transgressive lag, flood tidal delta, aggradational shoal and shoreface, tidal inlet/channel, 

mudflat, sand flat, reed swamp/organic rich soil, washover fan, beach ridge and beach, and 

aeolian. The Holocene deposits overlay sandy outwash plain deposits of Pleistocene age. The 

Holocene evolution of the barrier complex began with basal peat accumulation in a reed swamp 

about 8400 years ago. Approximately 8000 years ago the sea flooded the reed swamp and 

formed a transgressive flooding surface. The first transgressive lag sediments accumulated 6600 

years ago followed by rapid accumulation of flood tidal delta sediments until about 4500 years 

ago. At core site S1 beach sediments accumulated 5000 years ago and at core site L1 flood tidal 

sedimentation was succeeded by beach sedimentation about 4500 years ago. Between 4500 and 

2000 years ago core site S2, S4 and S5 became exposed to wave erosion due to shoreline 

transgression and in the same period the sedimentation at core site L1 decreased or ceased and 

the site became flooded. The modern Skallingen-Langli complex formed during the last c. 1000 

years with back-barrier sedimentation at core site L1 followed by aeolian sedimentation from 450 

to 300 years ago. The modern Skallingen formed as an aggradational intertidal to supratidal 

marine shoal 370 years ago possibly during or shortly after a major storm in 1634 AD. The last c. 

300 years washover and aeolian sediments have accumulated on Skallingen. 

47


Conclusions 

1 A high-resolution absolute chronology has been obtained for 5 sediment cores with ages 

ranging from 32300 ± 300 to 100 ± 10 years. The chronology documents the temporal evolution 

from wide spread outwash plain to the Skallingen-Langli barrier island complex. 

2 Two major surfaces have been identified in the internal architecture of the complex. A 

transgressive surface formed due to the marine flooding of the pre-Holocene surface. This 

surface marks the lithological change from glacio-fluvial sand or terrestrial accumulated peat to 

marine or estuarine mud and sand. The second major surface is a marine wave ravinement 

surface formed by shoreline erosion due to the transgression of the shoreline and is only present 

in the seaward part of the Skallingen-Langli complex. 

3 The sea-level rise and rapid shoreline retreat shifted the area of sedimentation in a 

landward direction during the marine transgression of the low-relief Pleistocene substratum 

causing a distinct time lag between flooding and the initial estuarine sedimentation. 

4 The Holocene sedimentation preserved in the complex is characterised by restricted 

periods (centuries) of rapid accumulation and periods of non-deposition or erosion. Widespread 

erosion was especially associated with the shoreline transgression which resulted in a large 

hiatus of c. 4000 years in the seaward part of the sedimentary complex. 

5 The formation of the modern Skallingen may have been the result of an extreme storm 

impacting the Northern Wadden Sea in 1634. 

6 The application of a high resolution OSL chronology in the analysis of the evolution of the 

Skallingen-Langli complex has been a key tool in the identification of the depositional units and 

bounding unconformities due to the homogenous sedimentology characteristic for this system. 

The study demonstrates that small changes in lithology and structures can represent major 

discontinuities in the stratigraphy and changes in the depositional systems. A high resolution 

geochronology is therefore critical in the interpretation of complex stratigraphic architecture, in the 

construction of the sequence stratigraphic framework of barrier systems, and in the unravelment 

of the sea-level history. 

Acknowledgement 

This study was founded by Geocenter Denmark, grant no. 603-0000 REFLEKS, by a PhD 

grant from the Department of Geography and Geology, University of Copenhagen and by the 

Danish Council for Strategic Research grant no. 09-066869 COADAPT. 

(A) Location of research area. (B) LiDAR-based digital elevation model (DEM) and Landsat image (ETM+ 

May 31 2003). All surface elevations above 8 m DVR90 are reproduced in white in the DEM. Notice the 

marked terrain elevation difference between Skallingen and the area bordering Skallingen towards the 

north. 

FitzGerald, D.M., Fenster, M.S., Argow, B.A. and Buynevich, I.V. (2008) Coastal impacts due to sea-level 

rise. Annu Rev Earth Pl Sc, 36, 601-647. 

Heron, S.D., Moslow, T.F., Berelson, W.M., Herbert, J.R., Steele, G.A. and Susman, K.R. (1984) Holocene 

Sedimentation of A Wave-Dominated Barrier-Island Shoreline - Cape Lookout, North-Carolina. Mar Geol, 

60, 413-434. 

Madsen, A.T., Murray, A.S., Andersen, T.J., Pejrup, M. and Breuning-Madsen, H. (2005) Optically 

stimulated luminescence dating of young estuarine sediments: a comparison with Pb-210 and Cs-137 

dating. Mar Geol, 214, 251-268. 

Moslow, T.F. and Heron, S.D. (1981) Holocene Depositional History of A Microtidal Cuspate Foreland Cape 

- Cape Lookout, North-Carolina. Mar Geol, 41, 251-270. 

Nielsen, N. and Nielsen, J. (2006) Development of a washover fan on a transgressive barrier, Skallingen, 

Denmark. J Coastal Res, 1, 107-111. 

48


INFLUENCE OF THE TIDAL BORE ON SEDIMENT TRANSPORT IN THE 

MONT-SAINT-MICHEL ESTUARY, NW FRANCE 

Lucille FURGEROT, Dominique MOUAZE, Bernadette TESSIER, Sylvain HAQUIN, Laurent 

PEREZ, Félix VIEL 

UMR CNRS 6143 M2C, UNIVERSITE DE CAEN, 24 rue des Tilleuls, 14000, Caen, France, 

lucille.furgerot@unicaen.fr, dominique.mouaze@unicaen.fr, bernadette.tessier@unicaen.fr, 

sylvain.haquin@unicaen.fr, laurent.perez@unicaen.fr 

The Mont Saint Michel estuary is a megatidal setting (tidal range up to 14 m). It is 

characterized by a strong tidal asymmetry during spring tides, with the flood stage much shorter 

and quicker than the ebb, reaching commonly a velocity of 2m/s into the estuarine channels. 

In estuaries with tidal ranges greater than 6 m, the difference of elevation between the rising 

tide and the river creates a discontinuity of velocity and pressure, called tidal bore (or “mascaret” 

in French). Visually, a tidal bore can be described as a wave or series of waves propagating 

upstream. 

This study takes place into a national project “ANR Mascaret”. Part of the field work we 

performed recently on the tidal bores that propagate into the Mt St Michel estuary, aims in 

studying the impact of the bore fluid dynamics on sediment transport. This is an important issue 

for a better understanding of the complex fluid-sediment interactions and for the operation of 

restoration of the Mont-Saint-Michel's maritime character 

(http://www.projetmontsaintmichel.fr/index_uk.html). We present herein the results of 

measurements of Suspended Sediment Concentration (SSC) sampled into the tidal bores. 

Previous measurements of SSC using OBS (Optical Backscattering Sensor) in the outer estuary 

indicate maximum values of 6g/L close to the seafloor (Desguée et al., 2011). In order to get 

more accurate values associated with tidal bore propagation into the inner estuary, we measured 

SSC using different techniques (optic, acoustic, direct sampling) 

The measurements were performed into the See River (View map of figure), some 8 km 

upstream from the outer estuary. Velocities were measured by using ADV (Acoustic Doppler 

Velocimeter). For SSC estimates we used three means. SSC was measured thanks to an OBS, 

by direct sampling into the water column, and was calculated by acoustic inversion method (from 

ADV raw signals). 

Manual pumps were used for direct sampling. Successive samples (less than 400ml) were 

taken approximately every 30 seconds during about 5 minutes immediately after the passage of 

the tidal bore, and then every 1 to 2 minutes during the thirty following minutes. SSC were then 

deduced in the laboratory after weighing and drying. ADV signal inversion is a common method 

for SSC calculation (Hosseini et al., 2006; Sottolichio et al., 2010). The critical step of the method 

is the calibration phase in the laboratory. It allows correlating sediment concentration and 

backscattering intensity. This is a difficult operation since the response of the ADV is very 

sensitive to high sediment concentrations. The OBS was calibrated in the same conditions, to 

correlate the output voltage with concentration of suspended matter. 

Preliminary results demonstrate that SSC obtained by direct samplings in the water column 

and ADV signal inversion are fairly different, although SSC evolution show similar patterns (See 

graphs). We assume that the problem is related to the ADV signal inversion method since direct 

samplings can be considered as the most reliable technique. This may be due to the properties of 

the local sediment, carbonated silt (called locally tangue) or to the high turbulence levels 

generated by the tidal bore passage. 

Anyhow, it appears that the SSC values obtained into the inner estuary are well above the 

average SSC measured by using OBS in the external estuary, i.e. 30-40 g/L vs. 6 g/L. 

Complementary analyses are in course using the data of a new field survey performed in 

May 2012, with simultaneous samplings at different heights in the water column. In addition to 

SSC estimates, grain-size analyses are also done on the samples. The objective is to define 

accurately vertical profiles of SSC and the sediment transport evolution associated with a tidal 

bore passage. 

49


Location of the study area and evolution of suspended sediment concentration (SSC) into an ondular tidal 

bore (top) and a breaking tidal bore (bottom) (SSC measured and SSC calculated from the amplitude of the 

ADV signal) 

Desguée, R., Robin, N., Gluard, L., Monfort, O., Anthony, E.J., Levoy F. (2011). Contribution of 

hydrodynamic conditions during shallow water stages to the sediment balance on a tidal flat: 

Mont-Saint-Michel Bay, Normandy, France. Estuarine, Coastal and Shelf Science 94:343-354 

Hosseini, S.A., Shamsai, A., Ataie-Ashtiani, B. 2006. Synchronous measurements of the velocity and 

concentration in low density turbidity currents using an Acoustic Doppler Velocimeter. Flow Measurement 

and Instrumentation 17: 59–68 

Sottolichio, A., Hurther, D., Gratiot, N., Bretel, P. 2011. Acoustic measurements of turbulence in highly 

turbid waters of a macrotidal estuary. Continental Shelf Research:31:S36-S49. 

50


THE 18.6 YEAR TIDAL CYCLE INFLUENCE ON THE COUESNON RIVER 

BEHAVIOUR, MONT-SAINT-MICHEL BAY (FRANCE) 

Lucile GLUARD, Franck LEVOY 

UMR CNRS 6143 M2C, UNIVERSITE DE CAEN, 24 rue des Tilleuls, 14000, Caen, France, 

lucile.gluard@unicaen.fr, franck.levoy@unicaen.fr 

River meandering in fluvial environment are well documented. But few studies describe their 

behaviour in salt marches areas where both tidal currents and river discharge were the main 

acting processes (Fagherazzi et al., 2004). This study aims at a better understanding of their 

behaviour on sand flat surfaces, through the example of the Couesnon river that wander at the 

foot of the Abbey, in the inner part of the Mont-Saint-Michel Bay. Such results are useful in the 

actual context of coastal anthropisation, or in a local context, to help stake-holders in the project 

of re-establishment of the marine nature of the Mont-Saint-Michel. 

A large aerial or satellite image dataset from 1969 to 2007, and a DEM constructed from a 

LiDAR survey in February 2009, are used to observe the channel position of the river at each 

date. Those positions are linked to annual high tide levels, annual river discharges and wind data. 

The analysis of the Couesnon channel migration shows that the river changes its channel 

planform in a global dynamic, well correlated with the 18.6 year lunar nodal tidal cycle, called the 

Saros cycle. When the channel migrates to the East, the Saros cycle is on an ascendant phase. 

When the channel migrates to the West, the Saros cycle is on a descendant phase. Extreme East 

or West positions of the river channel take place during high or low phases of the Saros cycle, 

respectively. 

This dynamic reflects the sedimentary inputs variation that contributes to a sand bank 

changes, in the West side of the study site. This sand bank grows and moves to the East during 

an ascendant phase of the 18.6 year lunar nodal tidal cycle. Its location forces the Couesnon 

channel to migrate to the same direction. During the descendant phase of the Saros cycle, the 

sand bank loses its influence, and the Couesnon channel answers to intern parameters, in 

particular river discharge. Regardless of the Saros cycle phase, at medium time scale (i.e. year to 

few years), the discharge controls also the sinuosity of the channel planform. The influence of the 

18.6 year lunar nodal tidal cycle has already been described in salt marsh environments (Wells et 

Coleman, 1981; Oost et al., 1993; Dronkers, 2005; Gratiot et al., 2008; Weill et al., 2011). 

However, this is a result to the local site of the Mont-Saint-Michel Bay that contributes to the 

understanding of its global functioning. 

51


Extreme Couesnon channel locations. a/ channel and salt marsh locations in 1980; b/ channel and salt 

marsh locations in 1989; c/ channel and salt marsh locations in 1995; d/ channel and salt marsh locations in 

2003. MSM : Mont-Saint-Michel Abbey. 

Dronkers J. (2005). Natural and human impacts on sedimentation in the Wadden Sea: an analysis of 

historical data. Rapport du Ministerie van Verkeer en Waterstaat, 51 p. 

Fagherazzi S., Gabet EJ, Furbish DJ. (2004). The effect of bi-directional flow on tidal channel planforms. 

Earth Surface Processes and Landforms 29, p. 295-309 

Gratiot N., Anthony EJ., Gardel A., Gaucherel C., Proisy C., Wells JT. (2008). Significant contribution of the 

18,6 year tidal cycle to regional coastal changes. Nature geoscience1, p. 169-172 

Oost AP., de Haas H., Ijnsen F., van der Boogert JM., de Boer PL. (1993). The 18,6 yr nodal cycle and its 

impact on tidal sedimentation. Sedimentary Geology 87, p. 1-11 

Weill P., Tessier B., Mouazé D., Bonnot-Courtois C., Norgeot C. (2011). Shelly cheniers on a macrotidal flat 

(Mont-Saint-Michel Bay, France)- Internal architecture revealed by ground penetrating radar. Sedimentary 

Geology (in press) 

Wells JT., Coleman JM. (1981). Periodic mudflat progradation, northeastern coast of south america : a 

hypothesis. Journal of Sedimentary Petrology 51 (4), p. 1069-1075 

52


ASSESSMENT OF SILTATION AT THE DREDGED CHANNEL IN THE 

HUANGMAOHAI ESTUARY, PEARL RIVER DELTA, CHINA 

Wenping GONG 

SCHOOL OF MARINE SCIENCE, SUN YAT-SEN UNIVERSITY, 135 of Xingangxi Road, 510275, 

Guangzhou, China, gongwp@mail.sysu.edu.cn 

The Huangmaohai Estuary is located in the southwest part of the Pearl River Delta, one of 

the fastest developing regions in China. The estuary features a large open water body, relatively 

deep navigation channel, and sheltered environment from wave attack, which makes it an ideal 

place for harbor construction. A draft plan is being undertaken to deepen its navigation channel 

from 7 m to 12.5m due to the development of large vessels for transportation. The assessment of 

changes in hydrodynamics, saline intrusion and sediment transport is a necessity for the 

environmental concern, and also the prediction of siltation situation after this expansion is of 

great importance for the maintenance of the drafted deep channel. 

In this study, a three-dimensional baroclinic model EFDC (Environmental Fluid Dynamics 

Code, the model domain is shown in Fig .1) is utilized to investigate the changes in 

hydrodynamics and sediment transport, induced by the planned project. The model is modified to 

account for the combined effect of wave and currents. After careful calibration and verification in 

terms of water level, water current, salinity and suspended sediment concentration in dry and wet 

seasons, the model is applied to study the siltation under different scenarios of channel 

deepening. The results indicate the importance of baroclinic effect on circulation, convergence of 

sediment transport and siltation at the channel. The inclusion of wave effect is also shown to be 

critical for sediment resuspension at the shoals and sedimentation at the channel, especially 

during storm conditions. 

The siltation in the channel is unraveled to show large seasonal variability and is mainly 

associated with the changes in external forcings and the associated sediment load. In the wet 

season, large sediment load from the upstream, combined with the establishment of strong 

baroclinic circulation, cause the majority of the siltation in the channel, among which storm effect 

plays an important role. In the dry season, with decreasing of the sediment load, and enhanced 

wind and wave, the channel is shown to be under erosion. 

53


The study site and model grid 

Hamrick, J.M., 1992. A three-dimensional environmental fluid dynamics computer code: theoretical and 

computational aspects. Special Report 317. Virginia Institute of Marine Science, Gloucester Point, VA. 

Hamrick, J.M., 1996. User's manual for the environmental fluid dynamics computer code. Special Report 

331. Virginia Institute of Marine Science, Gloucester Point, VA. 

54


SEDIMENTOLOGY AND SEQUENCE STRATIGRAPHY OF THE FLUVIAL-TO-TIDAL 

TRANSITION ZONE IN THE UPPER LAJAS FORMATION (NEUQUEN BASIN, 

ARGENTINA) 

Marcello GUGLIOTTA*, Stephen FLINT*, David HODGSON**, Gonzalo VEIGA*** 

*SCHOOL OF EARTH, ATMOSPHERIC & ENVIRONMENTAL SCIENCES, UNIVERSITY OF 

MANCHESTER, Oxford Road, M13 9PL, Manchester, Uk, marcello_gugliotta@virgilio.it 

**SCHOOL OF ENVIRONMENTAL SCIENCE, UNIVERSITY OF LIVERPOOL, 4, Brownlow Street, L69 

3BX, Liverpool, Uk 

***CENTRO DE INVESTIGACIONES GEOLOGICAS (UNIVERSIDAD NACIONAL DE LA PLATA – 

CONICET), Calle 1 N°644, B1900TAC, La Plata, Argentina 

The change from fluvial to estuarine settings is marked by the interaction of unidirectional 

fluvial currents and tidal currents. In modern systems the sedimentary process changes in the 

transition zone can be monitored. However, our understanding of how the fluvial-to-tidal transition 

zone is recorded in stratigraphic successions is poorly constrained. The lower reaches of many 

rivers are influenced by marine process, including tidal currents and brackish water. Because the 

resulting interaction of fluvial and marine processes occurs in low-lying areas near the coast, 

there is a high likelihood that these facies will be preserved in many sedimentary basins. This 

study is focused on the sedimentological characteristics of the fluvial-to-tidal transition zone in 

order to develop a better set of criteria for determining palaeogeographic position. Specific points 

to be addressed include: how does grain size change through the transition?; in what order do the 

various marine indicators begin to be expressed moving down palaeoriver?; how does the 

transition change as a function of parasequence stacking pattern (forward-stepping vs 

aggradational vs back-stepping)? 

Preliminary results from a detailed outcrop case study of the Middle Jurassic Lajas 

Formation of the Neuquén Basin are presented. The Lajas Formation comprises about 600 m of 

succession, spanning approximately 4.5 My and it is distinctive as tide-influenced sedimentation 

persisted through complete base level cycles and was not restricted to transgressive systems 

tracts or to the fills of incised valleys (McIlroy et al., 2006). 

The Lajas Formation contains fluvial deposits and is overlain transitionally by the fluvial 

Challacó Formation, providing an ideal opportunity to explore the stratigraphic distribution of 

preserved sedimentary facies, and reservoir and seals, in the fluvial-to-tidal transition. 

The study is focused initially on the “Bajada de los Molles” area, in which the transition 

between tidal and fluvial deposits is clearly and continuous exposed for about 0.5 km along the 

outcrop. Several erosion surfaces, correlatable across the entire outcrop, mark abrupt 

stratigraphic changes in facies that allow interpretations of changes in palaeoenvironment. 

Multiple measured sections have been correlated to constrain strike-parallel change in facies. 

In general, tidal and fluvial channel deposits are characterized by rather different grain size 

ranges. Tidal channels are filled by fine to medium sandstone and some abandoned mud-filled 

channels are also present. Fluvial channel fills are coarser (medium to coarse sandstone) and 

may have basal pebbles layers. Palaeocurrent data indicate westerly flowing rivers but the 

marginal marine/marine deposits show a wide range of paleocurrent directions and scales of 

crossbedding. Generally the Lajas Formation prograded from the southern and the eastern 

margins of the basin, but the subordinate tidal current and wave processes generated 

centimetre-scale cross-bedding in different directions. 

As well as grain size and palaeocurrents additional indicators allow the distinction of 

fluvial-dominated from tidal-dominated deposits and better define the range of the fluvial-to-tidal 

transitional zone. These indicators include tidal bundles, drapes of mud and coaly material, shells, 

bioturbation (marine) and large-scale cross bedding, abundant silicified wood, plant debris and 

thin carbonaceous shales (fluvial). 

ACKNOWLEDGEMENTS 

This work is part of the LAJAS Project, a joint study by the Universities of Manchester, 

Liverpool, University of Texas at Austin and Queen's University, Ontario. The project is sponsored 

by BHPBilliton, Statoil, VNG Norge and Woodside 

55


The “Bajada de los Molles” outcrop (40 Km South of Zapala) showings the upper part of the Lajas 

Formation an excellent example of fluvial-to-tidal transitional facies. 

MCILROY, D., FLINT, S.S., HOWELL, J.A. & TIMMS, N.E. 2006. Sedimentology of the tide dominated 

Lajas Formation, Jurassic, Neuquén Basin, Argentina. In: VEIGA, G. D., SPALLETTI, L.A., HOWELL, J.A. 

& SCHWARZ, E. (eds) The Neuquén Basin: a Case Study in Sequence Stratigraphy and Basin Dynamics. 

Special Publication of the Geological Society, London, 252, 83-107. 

56


THE EFFECT OF HIGH-ENERGY EVENTS ON EBB-TIDAL DELTA SEDIMENTOLOGY 

AND MORPHOLOGY – A PROCESS-BASED MODEL STUDY 

Gerald HERRLING, Christian WINTER 

MARUM - CENTER FOR MARINE ENVIRONMENTAL SCIENCES, Leobener Strasse 2, 28359, Bremen, 

Germany, gherrling@marum.de, cwinter@marum.de 

The environment of ebb-tidal deltas between barrier island systems is characterized by 

complex morphology with tidal sand bars and shoals bordering the main channel, near-shore 

oblique sand bars and shoreface-connected ridges (FitzGerald et al., 1984). These morphological 

features are in a dynamic equilibrium with the prevailing hydrodynamic forces and reveal 

characteristic surface sediment grain-size distributions. In this study the western tidal inlet and the 

shoreface of an East Frisian barrier island in the southern North Sea, has been chosen as an 

exemplary study area for an identification of relevant hydrodynamic drivers of ebb-tidal delta 

morphology and sedimentology. ANTIA (1993) studied the shoreface-connected ridges off 

Spiekeroog island with lengths of more than 10km and heights of up to 6m that are aligned with 

the direction of major storms (NW-SE). Surface sediments at the crests and upper seaward 

slopes are characterized by fine to medium sands, while coarser grain sizes are found in the 

troughs - in contrast to the contrary sedimentological patterns of near-shore tidal sand bars. SON 

et al. (2011) showed that surface sediments of the ebb-delta shoal, the swash bars and the inlet 

channel are characterized by medium sands with a fair amount of coarser shell hash. Both 

authors suggest that high-energy storm conditions play a significant role on sediment dynamics 

and morphology. This hypothesis has been tested in this study. By application of a process-based 

morphodynamic model the effect of high-energy events and long-term fair-weather conditions on 

(1) morphological changes and (2) the spatial surface sediment grain-size distribution has been 

differentiated. 

Model simulations have been carried out to compare the effect of an exemplary major storm 

surge event in the North Sea (Nov. 9th 2007) and a period of representative fair-weather 

conditions. A fully coupled, three-dimensional, multi-fractional morphodynamic model (Delft3D, 

Deltares) was set-up with a high spatial-resolution grid size of 30-60m. The interaction of wave 

forces, tidal currents and bed evolution is realized by fully bidirectional-coupled wave-current 

transport simulations. A bed layer model (van der Wegen et al., 2011) is applied permitting the 

re-distribution of multiple sediment fractions in accordance to the imposed hydrodynamic forces. 

The model simulation was started with a uniform distribution of five sand fractions with grain-sizes 

of 150, 200, 250, 350 and 450 microns throughout the model domain. Each sand fraction 

depletes or increases in the bed cell according to erosion or deposition processes in the sediment 

transport formulation (van Rijn, 1993). Very fine sands (


The model predicted re-distribution of five surface sand fractions between 150 and 450 microns allows the 

evaluation of the 50% sediment grain-size percentile (d50 in µm); very fine sand fractions and cohesive 

sediments were excluded in the present study, thus no grain-size sorting was modeled on the back-barrier 

tidal flats. 

Antia E.E. (1993): Surficial grain-size statistical parameters of a North Sea shoreface-connencted ridge: 

patterns and process implication, Geo-Mar Lett. 13: 172-181. 

FitzGerald DM., Penland S., Nummedal D. (1984): Control of barrier islands shape by inlet sediment 

bypassing: East Frisian Islands, West Germany. Mar. Geol. 60: 355-376. 

Son C.S., Flemming B.W., Bartholomä A. (2011): Evidence for sediment recirculation on an ebb-tidal delta 

of the East Frisian barrier-island system, southern North Sea, Geo-Mar Lett. 31: 87-100. 

Van Rijn L.C. (1993): Principles of Sediment Transport in Rivers, Estuaries and Coastal Seas. Aqua 

Publications, The Netherlands. 

Van der Wegen M., Dastgheib A., Jaffe B.E. (2011): Bed composition generation for morpho-dynamic 

modeling: case study of San Pablo Bay California, USA, Ocean Dynam. 61: 173-186. 

58


TIDALLY RELATED HETEROGENITIES IN SANDBODIES SOUGHT 

PARAMETERIZED FOR REFINED RESERVOIR MODELLING 

Berit HUSTELI, Maria JENSEN, Snorre OLAUSSEN 

UNIS, C/o Unis pb 156, 9171, Longyearbyen, Norway, berit.husteli@unis.no 

Beneath Longyearbyen, in Central Western Svalbard, an Upper Triassic to Lower Jurassic 

reservoir is targeted to store CO2 produced by the local energy plant. The 700 – 1000 m deep 

location of the reservoir will allow the gas to remain in its fluid state. To ensure the success and 

safety of the future storage, detailed modeling of the fluids future behavior is needed. 

Sedimentary heterogenities is difficult to include in the current practice of reservoir modeling. This 

project will, through detailed core and outcrop analysis coupled with Lidar data, contribute to 

improve future reservoir modeling and fluid behavior prediction. Additionally, it will contribute to a 

refined understanding of the sedimentary environment that prevailed in the Svalbard archipelago 

during the Triassic and Early Jurassic. 

Detailed core descriptions will be presented, in addition to outcrop studies of equivalent 

rocks ten kilometres north of the proposed point of injection. Edgeøya, east of Spitsbergen will be 

the focus of fieldwork in equivalent strata in August 2012. The facies distributions will be 

compared with Tertiary deposits and other deposits of similar origin for a better understanding of 

the dynamics of such an environment. The results will provide an overview of the range of variety 

that can be expected from these marginal marine sedimentary successions influenced by tidal 

energy fluctuations. The identified variation in geometry, grain size and porosity/permeability will 

yield quantified parameters that can be applied to develop a reservoir model which can 

successfully forward, and reverse model the targeted CO2 reservoir. 

The study is part of the project Geological input to Carbon storage (GeC) and 

Longyearbyen CO2 project. The Climit program of the Norwgian Research Council funds the 

study. The results will be presented in publications as part of a PhD terminating in March 2015. 

59


Correlation of retrieved cores from the CO2-storage project. The upper sandbody from Triassic/Lower 

Jurassic is the targeted reservoir. 

60


LATE MIOCENE INCISED VALLEY-FILL IN EASTERN TAURIDES, TURKEY: 

DEPOSITIONAL EVOLUTION IN RESPONSE TO SEA-LEVEL CHANGE AND 

DEPOSITIONAL PROCESSES 

Ayhan ILGAR, Erol TIMUR, Erhan KARAKUS, Serap KAYA, Banu TURKMEN 

GENERAL DIRECTORATE OF MINERAL RESEARCH AND EXPLORATION, Balgat, 06520, Ankara, 

Turkey, ayhan_ilgar@yahoo.com 

The incised valley-fills located within the reefal limestones of Middle Miocene age crop out 

in the southwestern part of the Adana Basin in eastern Taurides (Figure 1A, B). These deposits 

show funnel-shaped geometry extending 18 km in north-south direction. The valley-fill deposits 

comprise wide variety of facies types and composed of five facies associations including 

bay-head delta, tidal-flat, central basin lagoon, ebb-tidal delta and barrier-island. Based on these 

facies associations, the valley-fill is regarded as the typical microtidal wave-dominated estuary. 

Bay-head delta deposits which are located on the landward edge of the estuary to the north, 

consist of fluvial topset and basinward inclined foreset beds of conglomerates (Figure 1C). The 

sediments of the delta are mainly derived from the pre-estuarine reefal limestones. The tidal-flat 

sediments, which are also situated on the northern margin of the incised-valley, are composed of 

mudstones, siltstones, sandstones and subordinate conglomerates. These deposits show flaser, 

lenticular and wavy bedding, planar paralel stratification, current ripples, bi-directional cross 

stratification and well-sorted point bar deposits of tidal channels (Figure 1D). The central basin 

lagoon deposits mainly comprise the bioturbated, massive mudstones and subordinate lenticular 

siltstones (Figure 1E). The ridge-shaped barrier-island deposits which extend in east-west 

direction, are located on the southern part of the incised-valley. These deposits consist of planar 

paralel stratified, well sorted coarse sandstones and granule conglomerates (Figure 1F). The 

ebb-tidal delta deposits which are composed of fine to coarse sandstones, developed in the 

basinward side of the barrier-island. These deposits are characterized by planar cross-stratified 

dunes (Figure 1G) and tidal channel deposits, up to 60 cm and 190 cm in thickness, respectively. 

The mammalian fossil of Tetralophodon longirostris found in ebb-tidal delta deposits indicates a 

Late Miocene (early-middle Turolian (MN 11-12) age. 

The Neogene palaeogeographic evolution of the Adana Basin were greatly controlled by the 

relative sea-level changes. The interruption of marine sedimentation related to the falling of 

sea-level in eastern Taurides occurred at latest Middle Miocene. This event exposed the deposits 

of reefal limestones and caused to the formation of incised-valleys by fluvial erosion in the 

southwestern part of the Adana Basin. Subsequent marine flooding during the early Late Miocene 

sea-level rise converted the incised-valley into an wave-dominated estuarine environment in the 

regional microtidal setting of Miocene Mediterranean. The wave processes controlled the 

deposition by constructing a barrier-island at the mouth of the incised-valley which caused to the 

formation of a sheltered environment behind the barrier-island. The mudstones of the central 

basin lagoon deposited on this protected environment. The bay-head delta prograded southward 

from the landward edge of the estuarine to the central basin lagoon. In spite of the low tidal range 

of microtidal setting, the confinement of the tidal currents within the incised-valley caused to the 

enhancement of the tidal wave. So, the sufficient tidal prism provided tidal sedimentation in the 

incised-valley as tidal-flat and ebb-tidal delta deposits. It is thought that the ebb-tidal delta 

deposits were protected from the strong wave or storm erosion by confinement in the 

incised-valley. 

61


(A) Topographic map of Anatolia, showing the major tectonic boundaries and location of the Adana Basin 

between Taurus Orogenic Belts to the northwest and Misis Structural High to the southeast. (B) Simplified 

geological map of the Mut and Adana basins, showing the position of the wave-dominated estuary at the 

southwestern part of the Adana Basin. (C) Bay-head delta deposits consist of fluvial topset and basinward 

inclined foreset beds of conglomerates on the central basin lagoon mudstones. (D) The tidal-flat sediments 

are composed of flaser, lenticular and wavy beddings, planar paralel stratification, current ripples, 

bi-directional cross stratification and well-sorted point bar deposits of tidal channels. (E) The central basin 

lagoon deposits mainly comprise the bioturbated, massive mudstones and subordinate lenticular siltstones. 

(F) The ridge-shaped barrier-island deposits consist of planar paralel stratified, well sorted coarse 

sandstones and granule conglomerates. (G) The ebb-tidal delta deposits which developed in the basinward 

side of the barrier-island, are characterized by planar cross-stratified dunes and tidal channel deposits. 

62


THE VARIABILITY OF ESTUARINE DEPOSITS IN A MICROTIDAL SETTING OF LATE 

MIOCENE MEDITERRANEAN (EASTERN TAURIDES, TURKEY): CONTROLLING 

FACTORS ON DEPOSITION 

Ayhan ILGAR, Erhan KARAKUS, Tolga ESIRTGEN 

GENERAL DIRECTORATE OF MINERAL RESEARCH AND EXPLORATION, Balgat, 06520, Ankara, 

Turkey, ayhan_ilgar@yahoo.com 

The Adana Basin is one of the largest Neogene basin which is located on the northeastern 

edge of the Mediterranean in southern Turkey formed between the Taurus Orogenic Belts to the 

northwest and Misis Structural High to the southeast (Figure 1A). The latest Middle Miocene 

sea-level fall caused to the formation of incised-valleys in different part of the Adana Basin which 

were filled by discrete facies associations of fluvial to estuarine settings during the subsequent 

sea-level rise. 

The incised-valleys show funnel-shaped geometry extending in north-south direction. 

Although the incised-valleys were situated in the same coast of the basin in the earliest Late 

Miocene, two contrasting estuarine sediments were deposited on these valleys. One of them 

consisting of bay-head delta, tidal-flat, central basin lagoon, ebb-tidal delta and barrier-island 

facies associations reflects a wave-dominated estuarine setting in the western part of the basin 

(Figure 1B). The other incised valley-fill is located 55 km to the east of the basin (Figure 1B) and 

starts with the fluvial deposits of meandering rives at the bottom of the valley. Fluvial sandstones 

and mudstones are overlain by fine to very coarse grained marine sandstones rich in oyster 

fossils at the boundary. The marine sandstones include amalgamated trough and planar 

cross-stratifications, sigmoidal beds, lateral accretion sand bodies and isolated herringbone 

cross-stratifications which forming sand bars. The dunes, up to 150 cm in thickness, show mainly 

bi-directional bar developments bounded by reactivation surfaces with fine pebble pavement and 

thin bedded parallel stratified sandstones between them (Figure 1). These features of tidal dune 

and bars are confined in an incised-valley and form a tide-dominated estuarine deposits. 

The coeval occurrence of the wave- and tide-dominated estuarine deposits in a microtidal 

palaeo-oceanographic setting of Mediterranean in Late Miocene reflects an important 

palaeogeographic and structural implications. The western incised-valley was open to the normal 

marine processes and the deposition was controlled by the wave action at the mouth of the valley 

and fluvial processes at the head of the estuary. Tidal processes relatively little affected the 

sedimentation and caused the deposition of the ebb-tidal delta and tidal-flat sediments. However, 

the tidal processes were the main controlling factor on eastern incised-valley. This distinction 

occurred related to the enhancement of the tidal prism on eastern estuarine which was located at 

the northern margin and inner part of the Adana Basin embayment. This embayment was 

tectonically constructed by Misis Structural High which protected the deposits in Adana Basin 

from erosional effects of strong wave and storm action. The development of the embayment also 

caused to a resonance and consequent amplification of the tidal wave which was resulted in a 

tide-dominated estuarine of a microtidal setting in the incised-valley. 

63


(A) Topographic map of Anatolia, showing the major tectonic boundaries and location of the Adana Basin 

between Taurus Orogenic Belts to the northwest and Misis Structural High to the southeast. (B) Simplified 

geological map of the Mut and Adana basins, showing the positions of the wave-dominated estuary at the 

southwestern part of the Adana Basin and tide-dominated estuary at the northern margin of the Middle 

Miocene Adana Basin embayment. (C, D, E, F, G) Tidal dunes and sand bars formed by various types of 

trough and planar cross-stratifications. These tidal bars are confined in an incised-valley and form 

tide-dominated estuarine deposits. 

64


SEDIMENTOLOGY OF A FLUVIALLY DOMINATED, TIDALLY INFLUENCED POINT 

BAR: THE LOWER CRETACEOUS MIDDLE MCMURRAY FORMATION, LOWER 

STEEPBANK RIVER AREA, NORTHEASTERN ALBERTA, CANADA 

Bryce JABLONSKI*, Robert W. DALRYMPLE** 

*HEAVY OIL TECHNOLOGY CENTRE, STATOIL CANADA, 3600, 308-4 Ave. sw, T2P 0H7, Calgary, 

Canada, brjab@statoil.com 

**DEPARTMENT OF GEOLOGICAL SCIENCES, QUEEN'S UNIVERSITY, Miller Hall, K7L 2E2, Kingston, 

Otario, Canada, dalrymple@geol.queensu.ca 

The Lower Cretaceous (Aptian-Albian) McMurray Formation exposed along the lower 

Steepbank River in northeastern Alberta, Canada, exhibits world-class examples of inclined 

heterolithic stratification (IHS; Thomas et al., 1987) that is formed of alternating sand and mud 

layers. Individual sand layers reach 30 cm thick and consist of fine-grained sand that contains 

unidirectional climbing current-ripple lamination and, less commonly, dune-scale cross bedding. 

There is no evidence of tidal activity in most beds, but thin silt drapes are present in rare cases. 

Bioturbation is typically absent, but some beds contain scattered vertical burrows (Cylindrichnus 

predominates), or discrete layers with abundant burrows that are interpreted to represent 

amalgamation of two sand beds. These attributes indicate that the sand beds were deposited 

rapidly by river floods, in water that was either fully fresh or only very slightly brackish. The 

intervening mud layers range from less than a centimeter to approximately 10 cm in thickness. In 

contrast to the sand layers, they are intensely burrowed (again Cylindrichnus predominates, with 

lesser numbers of Planolites and Gyrolithes). Tidal-rhythmite lamination is visible in some 

occurrences where lamination has not been obliterated by burrowing. These fine-grained beds 

were deposited during times of low river discharge, under conditions of weak to moderate tidal 

activity. The water was brackish, but the very restricted ichnological diversity indicates that 

salinity levels were low. Each sand-mud couplet is, thus, interpreted to represent one year. 

These couplets are organized into a larger-scale cyclicity termed “meter-scale cycles” 

(MSCs; thicknesses 0.5-3 m). The basal part of each cycle consists of amalgamated sand layers, 

whereas the upper part of a cycle contains thicker mud interbeds. The thickness of the sand 

beds decreases upward through a cycle. The number of recognizable sand beds within these 

cycles ranges from 3-20. These cycles are thus “decadal” in duration and presumably reflect 

interannual variations in river discharge. These MSCs are an important architectural element of 

these point bars and can be correlated over long distances around each bend. 

Previous workers have interpreted these outcrops as having accumulated in an “estuarine” 

environment. We believe that they were formed in the fluvially dominated, tidally influenced 

portion of the tidal-fluvial transition (Fig. 1; i.e., in the innermost part of the transition). This is 

based on the fact that river-flood deposits are volumetrically predominant in the succession, and 

that river-flood deposition occurred under conditions of essentially unidirectional flow and nearly 

fresh water. Tidal action and brackish-water conditions only penetrated this far up the river during 

times of low river discharge. We suggest that the presence of a clear river-generated seasonality 

in a deposit is an indication that deposition occurred in a fluvially dominated setting. As one 

moves seaward through the fluvial-marine transition, one can expect this river-generated 

seasonality to decrease in prominence, while features generated by marine processes (e.g., tidal 

sedimentary structures and bioturbation) increase in abundance (Fig. 1). 

65


Schematic map of the fluvial-tidal transition displaying the variation in depositional conditions and structures 

as a function of the relative importance of fluvial and tidal energy. Through the transition, there is a change 

in the relative abundance of tidal sedimentary structures (e.g., tidal bundles, tidal rhythmites), the amount of 

bioturbation, and the prominence of bedding related to seasonal variations in river discharge. The 

migration of the salinity and tidal nodes (i.e., the limit of salinity and tidal intrusion up the river) in response 

to seasonal variations in river discharge is also shown. 

Thomas, R.G., Smith, D.G., Wood, J.M.,Visser, J., Calverley-Range, E.A., Koster, E.H., 1987. Inclined 

heterolithic stratification -terminology, description, interpretation and significance. Sedimentary Geology v. 

53, pp. 123–179. 

66


THE TIDALLY-INFLUENCED RIVER DEPOSITS OF THE PLEISTOCENE SEINE 

SYSTEM: THE EXAMPLE OF THE TOURVILLE-LA-RIVIERE TERRACE (NW 

FRANCE) 

Guillaume JAMET*, Olivier DUGUE*, Bernard DELCAILLAU*, Dominique CLIQUET** 


guillaume.jamet@unicaen.fr, olivier.dugue@unicaen.fr, bernard.delcaillau@unicaen.fr. 

**DRAC SRA, 13 Bis, rue Saint-Ouen, 14000, Caen, France, dominique.cliquet@culture.gouv.fr 

Since the 20th century, the Pleistocene Seine terraces system from Les Andelys to Le 

Havre was mainly studied using geomorphological tools (Lautridou et al., 1999). The lower Seine 

Valley was formed by the Plio-Pleistocene fluvial incision and shows presently large enclosed 

meanders. Few studies focused on fluvial to tidal environment transition during Pleistocene. An 

understanding of both continental and marine processes at the lower Seine Valley scale is 

needed to comprehend the stepped terraces system. On the one hand, the Seine River has 

incised a 125 m-deep and 2-4 km-wide valley. The substratum is composed of Cretaceous chalks 

with flints overlain by an irregular Cenozoic sedimentary cover (clay-with-flints and sands) and 

Plio-Pleistocene fluvio-marine facies (Lozere sand Formation and Saint Eustache sand 

Formation). The braided Pleistocene Seine River flow was able to erode, transport and rework 

bed material over large distances. On the other hand, alternating glacial and interglacial 

conditions during the Pleistocene period resulted in large shoreline fluctuations between the 

coastal watersheds of the Bay of Seine (Seine, Touques, Dives and Orne) and the Channel. 

During the interglacial periods (i.e., Marine Isotopic Stages 5e, 7 or 11), several marine incursions 

occurred along different courses of the Seine fluvial system. Consequently, the Pleistocene Seine 

Valley started to trap silty and sandy sediments supplied by the river. 

New sedimentological investigations on the Tourville-la-Rivière low terrace were conducted 

100 km away from the Seine estuary. Such sedimentary studies based on recently-discovered 

outcrop profiles exhibit mixed fluvial and tidal deposit that settled down during the Middle 

Pleistocene. The lower unit (fig.) of the vertical sequence shows 6 to 8 m-thick fluvial deposits 

overlying the Senonian chalky bedrock (± 4 m NGF). These deposits are mainly composed of 

coarse sands and gravels organised in fluvial bars. The latter fluvial architecture corresponds to a 

braided river system. This alluvial sequence is overlain by sands with flazer and wavy beddings (± 

13 m NGF) and a well-developed pedocomplex closed to a schorre system. The middle unit is 

characterized by homogeneous tidal sand deposits previously interpreted as fluvial environment 

(± 20 m NGF) (Lautridou et al., 1984). The upper unit evolves toward a slope deposits composed 

of sands, local head deposits and palaeosols (reworked Eemian Bt horizon, present-day soil). 

This sedimentological change in fluvial architecture started by high river discharges under 

periglacial conditions followed by the drowning of the Seine valley. Those new investigations 

complemented by numerical dating (IRSL, 196 ±23 ka BP; e.g. Balescu et al., 1996) and results 

of previous palaecological data, have allowed to discuss the cut-and-fill terrace processes of the 

Seine River during the Saalian (MIS 7). Those important results can be used to improve the 

palaeogeographic reconstruction of the Seine River during the Quaternary. 

67


Evolution of the fluvial-tidal transition units during MIS 7: The Tourville terrace (NW France) 

Balescu S., Lamothe M., Lautridou J.-P., 1996 - Luminescence evidence of two Middle Pleistocene 

Interglacial events at Tourville (Northern France). Boreas, 26, p. 61-72. 

Lautridou J.-P., Lefebvre D., Lécolle F., Carpentier G., Descombes J.-C., Gaquerel C., Huault M.-F., 1984 - 

Les Terrasses de la Seine dans le méandre d’Elbeuf, corrélations avec celles de la région de Mantes. 

Bulletin de l’Association Française pour l’Etude du Quaternaire, 1.2.3, p. 27-32. 

Lautridou J.-P., Auffret J.-P., Baltzer A., Clet M., Lécolle F., Lefèbvre D., Lericolais G., Roblin-Jouve A., 

Balescu S., Carpentier G., Cordy J.-M., Descombes J.-C., Occhietti S., Rousseau D.-D., 1999 - Le fleuve 

Seine, Le fleuve Manche. Bulletin de la Société Géologique de France, 170, (4), p. 545-558. 

68


THE SEDIMENTARY DEVELOPMENT OF A HOLOCENE TO RECENT BARRIER 

ISLAND, DANISH WADDEN SEA 

Peter N. JOHANNESSEN, Lars Henrik NIELSEN, Ingelise MØLLER, Lars Henrik NIELSEN, 

Thorbjørn Joest ANDERSEN, Morten PEJRUP 


Denmark, pjo@geus.dk 

The Rømø barrier island is situated in the northern part of the European Wadden Sea. It 

has been intensively studied on the basis of recent depositional systems and morphology, seven 

25 m long sediment cores, 35 km ground penetrating radar (GPR) reflection profiles with a 

maximum signal penetration of c. 15 m and a resolution of c. 20–30 cm (Nielsen et al., 2009), and 

dating of 70 core samples using optically stimulated luminescence (OSL). 

The area has experienced a relative sea-level rise of c. 15 m during the last c. 8000 years. 

The Recent tidal amplitude reaches c. 1.8 m. During strong wind set up the water level increases 

considerably and the highest measured water level is 4.9 m above mean sea level. 

The barrier island is c. 14 km long and c. 4 km wide and is separated from the mainland by 

a c. 8 km wide lagoon. At the northern and southern parts of the island, tidal inlets occur with a 

width of 400–1000 m and depths of 7–30 m. Salt marsh areas, up to 2 km wide, are fringing the 

lagoonal coast of the island. Active eastward migrating aeolian dunes cover large parts of the 

island. 

The Rømø barrier island system is a very sand rich system as it receives coast parallel 

transported sand from north and south along the shoreface and is resting on fluvial sand. 

The combination of cores, GPR and studies of the Recent morphology and depositional 

processes is a powerful tool to identify palaeo-sedimentary environments (Johannessen et al., 

2008). On GPR sections from the central part of the island a series of beach ridges, up to 2.5 m 

high, often with swales in between are underlying the modern aeolian dune sands. Washover 

fans, up to 2.5 m thick, are often seen in the GPR sections immediately east of the beach ridges 

and can be followed c. 250 m eastwards and may have steep slipfaces. Shoreface sands may be 

followed eastward to beach ridges and show westward progradation. Swash bars are 

occasionally seen on the shoreface close to the beach ridges. In the northernmost area of the 

island the GPR sections are dominated by co-sets with westerly and easterly dipping foresets, 

indicating bipolar current directions (Møller et al., 2008). These sediments were probably 

deposited in a deep, broad tidal inlet north of the initial barrier island similar to what is observed at 

the island today. 

Facies analysis on the cores and correlations between wells show that barrier island 

sediments and related shoreface sand and lagoonal sediments are up to 20 m thick and overlie 

Weichselian fluvial sand. The first 5000 years the barrier island aggraded and the last 3000 years 

it prograded despite the relative rising sea level rise of c. 15 m during the last c. 8000 years. This 

shows, that if there is a surplus of sand in a tidal area, barrier islands may aggrade even if there 

is a rise in sea level. If the rate of sea level rise decreases then the barrier island may prograd. 

With this unique dataset with extremely large amounts of OSL datings from core sediments 

it has been possible to construct detailed palaeogeographic maps of the barrier island 

development through time. 

69


Orthophoto of the Rømø barrier island. The location of Ground Penetrating Radar reflection profiles and 

seven core wells are shown. Very wide tidal sand flat characterise the north-western and south-western 

parts of Rømø. 

Johannessen, P.N., Nielsen, L.H., Nielsen, L., Møller, I., Pejrup. M., Andersen, J.T., Korshøj, J.S., Larsen, 

B. and Piasecki, S. (2008) Sedimentary facies and architecture of the Holocene to Recent Rømø barrier 

island in the Danish Wadden Sea. Geological Survey of Denmark and Greenland Bulletin, 15, 49-52. 

Møller, I., Nielsen, L., Johannessen, P.N., Nielsen, L.H., Pejrup, M., Andersen, T.J., and Korshøj, J.S. 

(2008) Creating the framework of sedimentary architecture of a barrier island in the Danish Wadden Sea. 

Proceedings of 12th International Conference on Ground Penetrating Radar, Birmingham, UK, 8 pp. 

Nielsen, L., Møller, I., Nielsen, L.H., Johannessen, P.N., Pejrup, M., Korshøj, J.S. and Andersen, T.J. 

(2009) Integrating ground-penetrating radar and borehole data from a Wadden Sea barrier island. Journal 

of Applied Geophysics, 68, 47-59. 

70


TIDAL RAVINEMENT SURFACE IN A TIDE-DOMINATED ESTUARY: PLEISTOCENE 

NHA BE ESTUARY, SOUTHERN VIETNAM 

Toshiyuki KITAZAWA 

FACULTY OF GEO-ENVIRONMENTAL SCIENCE, RISSHO UNIVERSITY, 1700 Magechi, 360-0194, 

Kumagaya, Saitama Pref., Japan, kitazawa@ris.ac.jp 

The features of tidal ravinement surface (TRS: Allen, 1991; Allen and Posamentier, 1993) in 

macrotidal tide-dominated estuary are discussed based on ancient deposits. TRS is an important 

sequence stratigraphic boundary in an incised-valley system, because a TRS is developed only 

inside of an incised valley and is not on interfluves (Zaitlin et al., 1994) in contrast to a wave 

ravinements surface. A TRS is created in a transgressive tide-dominated estuary by 

amalgamation of channel scours as a result of the landward migration of the tidal channels 

separating tidal sand bars (Dalrymple et al., 1992). The sedimentological feature and distribution 

of TRS formed in a tide-dominated estuary have not been known well because only a few 

examples have been descried. Although TRSs are observed in numerous incised-valley systems, 

the term TRS is commonly used for amalgamated truncations at the base of tidal inlet channels 

cutting a barrier island and at the base of flood tidal delta in wave-dominated or wave- and 

tide-dominated estuaries. 

The solid subject in this study is the Middle to Upper Pleistocene Ba Mieu and Thu Duc 

Formations exposed around the Nha Be River, southern Vietnam. The Ba Mieu Formation was 

deposited during marine isotope stage (MIS) 7 to 6, and the Thu Duc Formation was deposited 

during MIS 5 (Kitazawa et al., 2006). The formations are deposited in tide-dominated 

incised-valley systems consists of estuary and delta (Kitazawa and Tateishi, 2005; Kitazawa, 

2007). TRS in the formations is divided into 3 types based on the environment. 

1) Intertidal-TRS is formed by landward migration of meandering tidal channels in intertidal 

zone around the bay head. The tidal channels are filled with mud clasts fed from the channel 

bank. Intertidal-TRS is not laterally continuous relative to incised-valley bottom and the other 

TRSs because the tidal channels are small and sometimes abandoned. 

2) Bar-channel-TRS is formed by landward migration of braided tidal channels in a marine 

sand body consists of tidal sand bars and sand flat around the central portion of the estuary. The 

channels filled with sand and gravel are amalgamated with each other and continuous laterally. 

The continuity depends on the extent and migrating distance of the marine sand body. 

3) Subtidal-TRS is formed by landward migration of major subtidal channels. It erodes 

away former existing transgressive deposits, and gravel and mud clasts are only preserved as lag 

deposits. The continuity depends on the extent and migration distance of the subtidal erosional 

zone. 

At inland portion, fluvial and salt marsh deposits overlie the basement rocks, and 

intertidal-TRS is only scattered in tidal flat deposits. In more seaward portion, sand flat and mixed 

flat deposits are interfingered, that is the landward limit of the bar-channel-TRS at the maximum 

flooding period. Bar-channel-TRS and subtidal-TRS are amalgamated with each other and 

remarkable on outcrops. This amalgamated TRS is laterally continuous (at least 15 km), 

therefore, it is recognized as an important sequence stratigraphic boundarie regionally developed 

within the tide-dominated estuary. The transgressive deposits below the bar-channel TRS thin 

seaward because of the tidal erosion during later transgression, and are almost eroded away in 

the most seaward portion. As a result, bar-channel-TRS and subtidal-TRS commonly erode the 

underlying depositional sequence or basement rocks and is recognized as a sequence boundary. 

In other words, an incised valley formed by fluvial erosion during a lowstand period is again 

eroded and deepen by tidal channels during the transgression. 

The relative extent of TRS to the estuary length is wide in the Pleistocene tide-dominated 

Nha Be Estuary in comparison to wave- and tide-dominated Gironde Estuary. It is caused by the 

relative extent of tidal scour, that is, the existence of marine sand body and subtidal erosional 

zone. 

71


Classification of TRS in a tide-dominated estuary section. 

Allen, G.P., 1991. Sedimentary processes and facies in the Gironde estuary: a recent model for macrotidal 

estuarine systems. In: Smith, D.G., Reinson, G.E., Zaitlin, B.A., Rahmani, R.A. (Eds.), Clastic Tidal 

Sedimentology. Canadian Society of Petroleum Geologists, Memoir 16, pp. 29–400. 

Allen, G.P., Posamentier, H.W., 1993. Sequence stratigraphy and facies model of an incised valley fill: the 

Gironde Estuary, France. Journal of Sedimentary Petrology 63, 378–391. 

Dalrymple, R.W., Zaitlin, B.A., Boyd, R., 1992. Estuarine facies models: conceptual basis and stratigraphic 

implications. Journal of Sedimentary Petrology 62, 1130–1146. 

Kitazawa, T., 2007. Pleistocene macrotidal tide-dominated estuary–delta succession, along the Dong Nai 

River, southern Vietnam. Sedimentary Geology 194, 115–140. 

Kitazawa, T., Nakagawa, T., Hashimoto, T., Tateishi, M., 2006. Stratigraphy and optically stimulated 

luminescence (OSL) dating of a Quaternary sequence along the Dong Nai River, southern Vietnam. Journal 

of Asian Earth Sciences 27, 788–804. 

Kitazawa, T., Tateishi, M., 2005. Geometry and preservation process of tidal sand bar deposits of Middle 

Pleistocene macrotidal tide-dominated delta succession, southern Vietnam. Journal of Sedimentological 

Society of Japan 61, 27–38. 

Zaitlin, B.A., Dalrymple, R.W., Boyd, R., 1994. The stratigraphic organization of incised-valley systems 

associated with relative sea-level change. In: Dalrymple, R.W., Boyd, R., Zaitlin, B.A. (Eds.), Incised-valley 

Systems: Origin and Sedimentary Sequences, SEPM Special Publication 51, pp. 45–60. 

72


TIDAL DELTAS IN THE LAJAS AND TILJE FORMATIONS: TIDE-DOMINATED OR 

TIDE-INFLUENCED? 

Colleen KURCINKA*, Aitor ICHASO**, Robert W. DALRYMPLE* 


c.kurcinka@queensu.ca, dalrymple@geol.queensu.ca 

**SHELL CANADA LTD., 400 - 4th ave sw, T2P 2H5, Calgary, Alberta, Canada, aitorichaso@hotmail.com 

The Lower Lajas Formation (Jurassic) located in the Neuquen Basin of western Argentina is 

thought to represent a deltaic system that accumulated in a back-arc basin (post-rift) (Howell et 

al., 2005). The funnel-shaped geometry of the basin accentuated the tidal currents while 

restricting wave influence. The basal portion of the Lajas Formation records tide-dominated 

deltaic deposits, which grade into a tide-dominated coastline, and eventually into the overlying 

fluvial and floodplain deposits of the Challaco Formation (McIlroy et al., 2005). The broadly 

time-equivalent Tilje Formation (Jurassic, offshore Norway) also consists of stacked tidally 

influenced deltaic deposits that accumulated in a rift-basin setting. Both successions have been 

interpreted as tide-dominated by previous workers (Martinius et al., 2001; McIlroy et al., 2005). 

Tide-dominated deltas are poorly known relative to other delta types. The modern 

tide-dominated deltas that have been studied in some detail (e.g.. the Amazon and Fly river 

deltas) are large and mud dominated, while many of the ancient analogues tend to be sandy and 

on a much smaller scale (e.g.. the Frewens Sandstone). Recent work has suggested that such 

sandy tide-dominated deltas may contain abundant oppositely dipping crossbeds, sigmoidal 

cross-bedding, reactivation surfaces, abundant heterolithic facies, tidal bundles, and double 

drapes as their more distinctive characteristics (Willis, 2005), whereas tidal rhythmites and fluid 

muds are widespread in modern muddy deltas. In much new work on coastal systems, there is a 

growing realization, however, that reliance on end-member models can be misleading, as most 

areas experience an interplay of two or more depositional processes. Thus, it is relevant to ask 

what the deposits of a tide-influenced delta are like and how they might differ from those of a 

tide-dominated system. Presumably, tidal features will be present, but they are likely to be mixed 

with wave- and/or river-generated structures. Tanavsuu-Milkeviciene and Plink-Bjorklund (2009), 

for example, have suggested that the presence of fluvial deposits in the delta plain is an indicator 

of tidal influence rather than tidal dominance. However, the range of possible mixed-energy deltas 

is large and there are very few examples in the ancient that can be used for comparison. 

Recent work (Ichaso, 2012) on the Tilje Formation in offshore Norway (for which the Lajas 

Formation has been used as an outcrop analog) suggests that these deltaic deposits contain a 

significant and pervasive indication of fluvial influence. Evidence of seasonal variations in river 

discharge is present in the heterolithic, mouth-bar and delta-front areas, in the form of 

decimeter-scale variations in the grain size, abundance of fluid-mud layers and the intensity of 

bioturbation. Wave-generated structures are only rarely present in progradational successions, 

but are more common in areas away from the active distributaries and during times of delta-lobe 

abandonment. This assemblage of structures indicates that this system was formed by a 

mixed-energy delta that would plot approximately half-way between the tide- and river-dominated 

end-members on the “delta triangle”, rather than at the tide-dominated apex. Preliminary 

investigations of the Lajas Formation deltas (Figure 1) suggest that tidal action might also have 

been over-estimated in this system, and that river influence may be significant. While organic 

drapes, some of them double, are present in the toesets of some dunes, they are not ubiquitous. 

Other compelling tidal indicators are absent or sparse, and paleocurrent data indicate primarily 

seaward-directed crossbeds. Similarities exist between the Lajas Formation and the 

tide-influenced Frewens Sandstone, as the Frewens is also strongly ebb-dominated. However, 

the Frewens Sandstone contains widespread tidal indicators in the form of true double mud 

drapes, heterolithic deposits, and local current reversals (Willis, 1999). It can be suggested that 

the Lajas Formation, much like the Tilje Formation, is a mixed tide-river delta and its position on 

the deltaic triangle should also be moved. More work is needed on both modern and ancient 

tide-dominated and mixed-energy deltas in order to determine the expected range of deposit 

types in mouth-bar and delta-front settings. 

Howell, J.A., Schwarz, E., Spalletti, L.A., and Viega, G.D. 2005. The Neuquen Basin: an overview.In: 

Spalletti, L., Veiga, G., Howell, J.A. & Schwarz, E. (eds.), The Neuquén Basin: A Case Study in Sequence 

Stratigraphy and Basin Dynamics. Geological Society, London, Special Publications. 

73


Ichaso, A. 2012. Spatial and temporal controls on the development of heterolithic, lower Jurassic tidal 

deposits (upper Are and Tilje Formations), Haltenbanken area, offshore Norway. Unpublished Ph.D thesis, 

Queen’s University, p. 252. 

Martinius, A.W., Kaas, I., Næss, A., Helgesen, G., Kjærefjord, J.M., and Leith, D.A. 2001. Sedimentology of 

the heterolithic and tide-dominated Tilje Formation (Early Jurassic, Halten Terrace, offshore mid-Norway). 

In: Martinsen, O.J. and Dreyer, T. (eds.), Sedimentary environments offshore Norway – Paleozoic to recent 

(Eds), Norwegian Petroleum Foundation Spec. Publ. 10, 103-144. 

McIlroy, D., Flint, S.S., Howell, J.A. & Timms, N.E. 2005. Sedimentology of the tide-dominated Lajas 

Formation, Jurassic Neuquén Basin, Argentina. In: Spalletti, L., Veiga, G., Howell, J.A. & Schwarz, E. 

(eds.), The Neuquén Basin: A Case Study in Sequence Stratigraphy and Basin Dynamics. Geological 

Society, London, Special Publications. 

Tanavsuu-Milkeviciene, K., and Plink-Bjorklund, P. 2009. Recognizing tide-dominated versus 

tide-influenced deltas: the Middle Devonian strata of the Baltic Basin. Sedimentology 79, 887-905. 

Willis, B.J., 1999. Architecture of the tide-influenced river delta in the Frontier Formation of central 

Wyoming, USA. Sedimentology 46, 667-688. 

Willis, B.J., 2005, Deposits of tide-influenced river deltas. In: Giosan, L., and Bhattacharya, J.P. (eds.), 

River Deltas—Concepts, Models and Examples. SEPM Special Publication 83, p. 87-129. 

74


LITTORAL SEDIMENTATION WITHIN SPARTINE AND OBIONE COMMUNITIES IN 

THE SOMME ESTUARY (EASTERN ENGLISH CHANNEL). PRELIMINARY RESULTS 

Sophie LE BOT*, F BERTEL*, Estelle LANGLOIS*, Estelle FOREY*, Antoine MEIRLAND**, 

Robert LAFITE* 

*UMR CNRS 6143 M2C, UNIVERSITE DE ROUEN , Place Emile Blondel, 76821, Mont Saint Aignan, 

France, sophie.lebot@univ-rouen.fr 

**GEMEL PICARDIE, 115 Quai Jeanne D’arc, 80230, Saint-Valéry-Sur-somme, France 

Like many estuaries in the English Channel, the Somme estuary follows an infill pattern 

(Tessier et al., 2011). Land reclamation (embankments, polders) increase reinforces the natural 

accretion process (Bastide, 2011). The infilling leads to important modifications of environment 

uses (e.g. fisheries, navigation). 

The Somme estuary is macrotidal but wave-dominated due to high energy wave conditions. 

They induce strong littoral drift leading to the development of a gravel barrier at its mouth, on the 

southern part (Anthony and Héquette, 2007; Marion et al., 2009). The tidal regime is semi-diurnal 

and flood-dominated. The tidal range reaches 9-10 m in spring conditions. Fluvial discharge of the 

Somme river is weak (5-60 m3/s) (Dupont et al., 1994), inducing an infilling of the estuary almost 

exclusively with sands of marine origin (Dupont, 1981) and bioclasts from endemic benthic 

production (Desprez et al., 1998). 

Sedimentation rate in the Somme estuary is about 700 000 m3/yr, corresponding to a mean 

seabed elevation between 1.3 and 1.8 cm/yr (Verger, 2005; Bastide, 2011). These rates are 

similar to those recorded in the Authie estuary located some tens of kilometers to the North 

(0.71-1.6 cm/yr; Marion, 2007). Vegetation plays a major role in the estuarine sedimentation, 

since it constitutes an hydrodynamic barrier that favours sediment deposition. In particular, 

Spartina townsendii and Halimione portulacoides communities play a significant effect on 

sedimentation rate. These species are respectively observed on the low marsh (between slikke 

and schorre) flooded by mean tides and on the mid-marsh flooded by spring tides. In European 

salt marshes, sedimentation rates are in the range of 15 cm/yr in pioneer zones with Spartina and 

4.7 cm/yr in mid salt marsh vegetation with Halimione (Ranwell, 1964; Brown et al., 1998; 

Langlois et al., 2001). 

In order to analyze sediment characteristics in Spartina and Halimione communities, short 

cores (30-40 cm) have been collected on three sites of the estuary selected as representative of 

different hydro-sedimentary conditions (exposed and sheltered sites). Three replicates have been 

sampled per site. A visual description of the cores has been realised to determine sediment 

layering and layer thicknesses (Figure 1). Grain-size analyses have been conducted on 

sub-samples in specific core layers. Topographic surveys, carried out using an airborne scanning 

LIDAR from the CLAREC team and a high resolution laser electronic station, have been used to 

assess the erosive or accumulative sedimentary trend through the winter 2011-2012. 

A grain-size varibility is observed at different scales: the vegetation communities scale, the 

estuary scale (inter-site variability) and the replicate scale (intra-site variability). Spartina. 

communities are associated with a sandy dominant sedimentation (122 and 185 mm), whereas 

Halimione communities are merely silty dominated (38 and 84 mm; Figure 1) under the influence 

of decantation processes. This may be explained by differences in exposure of the communities 

to the main marine forcing agents, mainly controlled by altitude, that influences tidal immersion 

time, position along the cross-shore profile and vegetation density, both controlling the energy 

dissipation of the forcing agents. In the estuary, a grain size fining trend is observed from sites 

open on the marine environment to sheltered sites, due to various exposure degrees to tide and 

wave action. The three study sites belong to different estuarian sub-units, defined by Dupont 

(1981) as variously influenced by actions of the forcing agents.Site-effect is therefore important as 

confirmed by the contrasted topographic evolution recorded during winter 2011-2012. Within a 

site, sedimentary record is homogeneous exception made of the number and depth of layers. 

Rythmicity is observed in core sedimentation, due to the repetition of a two-layer pattern. In 

Halimione communities, the two-layer pattern (0.7-5.8 cm) is composed of one dark layer (0.3-1 

cm), often rich in stems, and one clear silty layer (0.4-4.7 cm). Stem-rich dark layers may indicate 

the period of the falling leaves of Halimione. The two-layer pattern would therefore represent 

annual sedimentation, what is consistant with mean annual sedimentation rates previously 

recorded (Verger, 2005; Marion, 2007; Bastide, 2011). In Spartina communities, the the two-layer 

pattern displays various compositions and thicknesses. They are composed of: (i) one layer 

(0.75-9 cm) made of fine sands and one layer (0.4-3.4 cm) made of very fine sands, (ii) two 

0.75-cm layers, dark or light, made of very fine sands, or (iii) one sandy layer (2.8-11.4 cm) 

alternating with a shelly layer (0.9-1.4 cm). Compared to the mid-marsh where Halimione is 

75


observed, the stronger sedimentation variability in Spartina community is probably to relate to a 

higher variability of the hydrodynamic conditions due to: (i) a stronger exposure degree of the 

low-marsh where Spartina is observed, (ii) a variability in exposure degree according to the 

location of the site within the Somme estuary, and/or (iii) the vegetation cover (dense in the case 

of Halimione, scarse in the case of Spartina). 

Core sampled in the Halimione community (core 0Z1A). From left to right : photo, scheme, sub-samples, 

visual description. The colour of sub-samples inform on their grain-size: mode of 38, 84 and 96-116 mm 

respectively for orange, red and brown colours. 

Anthony and Héquette, Sediment. Geol. (2007) 

Bastide, PhD Thesis (2011) 

Brown et al., Mar. Poll. Bull. (1998) 

Desprez et al., in Auger et al. (Ed.) (1998) 

Dupont, PhD Thesis (1981) 

Dupont et al., Mar. Geol. (1994) 

Langlois et al., Journ. Veget. Science (2001) 

Marion, PhD thesis (2007) 

Marion et al., Estuar. Coast. Shelf Science (2009) 

Ranwelle, Journ. Ecology (1964) 

Tessier et al., Sediment. Geol (2011) 

Verger, Belin Ed. (2005) 

76


FACIES MODEL OF A FINE-GRAINED, TIDE-DOMINATED DELTA: LOWER DIR ABU 

LIFA MEMBER (EOCENE), WESTERN DESERT, EGYPT 

Berit LEGLER*, Howard JOHNSON**, Gary HAMPSON**, Benoit MASSART**, Christopher 

JACKSON**, Matthew JACKSON**, Ahmed EL-BARKOOKY***, Rodmar RAVNAS**** 

*UNIVERSITY OF MANCHESTER, SEAES, Oxford Road, Williamson Building, M9 13PL, Manchester, Uk, 

berit.legler@manchester.ac.uk 

**IMPERIAL COLLEGE LONDON, Prince Consort Road, SW2 7AZ, London, Uk 

***SHELL EGYPT, El-Horreya, 2681, Cairo, Egypt 

****NORSKE SHELL, Tankvegen 1, 4056, Tananger, Norway 

Existing facies models of tide-dominated deltas largely omit fine-grained, mud-rich deltaic 

successions. Sedimentary facies and sequence stratigraphic analysis of the Late Eocene Dir Abu 

Lifa Member (Western Desert, Egypt) aims to bridge this gap. The succession was deposited in a 

structurally controlled, shallow, macrotidal embayment and deposition was supplemented by 

fluvial processes but lacked wave influence. 

The Dir Abu Lifa Member, studied along a 12 km-long, continuously exposed cliff face 

through an exceptionally well-preserved succession of tidal deposits containing a plethora of tidal 

indicators (c. 80 m thick and divided into seven facies associations: FA1-7). The majority of the 

succession (FA1-6) was deposited in a tide-dominated environment, which was supplemented by 

fluvial processes but lacked wave influence. Two main genetic units are identified: (1) 

non-channelised tidal bars (FA1-2); and (2) tidal channels (FA3-6). The non-channelised tidal 

bars comprise coarsening upwards parasequences (c. 4-12 m thick), which passed upwards from 

shallow, brackish water mud-dominated bays (c. 5-15 m water depth) and into sandy heterolithic 

tidal bar forms, including large, forward-facing accretion surfaces, sometimes with evidence of 

emergence at the top (rooted with thin coals). The tidal channels are preserved as both singleand 

multi-storey bodies, but displaying different types of bar and infill: (1) FA3 channels were 

filled by laterally migrating, elongate tidal bars (with Inclined Heterolithic Strata - IHS; c. 5-25 m 

thick), (2) FA4 channels were filled by large, forward-facing sigmoidal bars (with Sigmoidal 

Heterolithic Strata - SHS; up to 10 m thick), (3) FA5 channels were filled by side bars displaying 

oblique to vertical accretion (c. 4-7 m thick), and (4) FA6 channels were filled by 

vertically-accreting mud (c. 1-4 m thick). Palaeocurrent data, supported by a wide range of other 

tidal indicators, shows that these channels were swept by bidirectional tidal currents and were 

typically mutually evasive (the dominant westerly currents were fluvial/ebb-tide oriented and the 

subordinate easterly currents were flood oriented). 

Larger scale, stratigraphic relationships show that the lower Dir Abu Lifa Member comprises 

three stacked, progradational parasequence sets bounded by carbonate-cemented transgressive 

lags (FA7), which are overlain by regionally extensive ravinement surfaces. Significant 

along-strike variability defines three distinctive facies belts (SW, Central and NE). The SW and 

NE facies belts are fine grained, mud-rich and dominated by non-channelised tidal bars (FA1-2), 

smaller channelised bodies (FA5) and mud-filled channels (FA6). The central belt is dominated by 

large, multilateral and multi-storey channel sandstones with widespread IHS and occasional SHS 

(FA3-4) within both PSS1 and PSS2 and is interpreted as a major tidal-distributary channel belt. 

These areas preserve tidal bars and intercalated tidal distributary channels deposited in a delta 

front to inter-tidal to supra-tidal lower delta plain setting. 

A tide-dominated delta model is favoured, based on: (1) the gross stratigraphy (Late 

Eocene to Oligocene) forms part of a large-scale regressive succession, which passes from 

offshore shallow marine sandstones, through inshore/tidal sandstones and mudstones (including 

the Dir Abu Lifa Member), and into fluvial deposits; (2) the parasequences and parasequence set 

stacking patterns are characterised by overall progradational patterns; (3) there is an absence of 

both depositional transgressive successions and tidal ravinement surfaces; and (4) architectural 

relationships demonstrate contemporaneous tidal distributary channel infill and tidal bar accretion 

at the delta front. 

The data-driven interpretation of an exclusively tide-dominated delta significantly expands 

the range of facies and sequence stratigraphic models available for the analysis of ancient tidal 

successions, which are currently biased towards transgressive, valley-confined estuaries. 

77


Generalised facies model of the Dir Abu Lifa Member 

78


RHYTHMITES PRESERVATION IN MACROTIDAL ESTUARINE ENVIRONMENTS: 

FROM UPSTREAM TO DOWNSTREAM ESTUARY 

Maxence LEMOINE*, Julien DELOFFRE*, Robert LAFITE*, Sandric LESOURD**, Patrick 

LESUEUR***, Antoine CUVILLIEZ****, Nicolas FRITIER*, Nicolas MASSEI* 

*UMR CNRS 6143 M2C, UNIVERSITE DE ROUEN , Place Emile Blondel, 76821, Mont Saint Aignan, 

France, maxence.lemoine@univ-rouen.fr 

**UMR 8187 LOG, 28 Avenue Foch, bp 80, 62930, Wimereux, France 

***UMR CNRS 6143 M2C, UNIVERSITE DE CAEN, 24 rue des Tilleuls, 14000, Caen, France 

****UMR 6294 CNRS LOMC, 53, rue Prony, bp 540, 76058, Le Havre, France 

Estuaries are interface environments between continental and marine domains. The 

estuarine system classifications allow estuarine zonation based on the longitudinal distribution of 

hydrodynamic forcing relative energies (flow, tide and swell) which contribute to the 

hydrodynamics and sediment dynamics. The respective influence of hydrodynamic processes 

was represented by Dalrymple et al., 1992 (Fig. 1). The resulting hydrodynamics is highly variable 

and nonlinear in space but also in time: from seconds (swell) to multi-year (interannual variability 

of hydrological flows). 

The Seine estuary is a macrotidal estuary (tidal range of 8m at the mouth) developed over 

160km up the upstream limit of tidal wave penetration at the Poses dam. With an average river 

flow of 450m3.s-1 (ranges between 200 and 2200), the Suspended Particles Matter (SPM) annual 

flux is about 700,000tons, with 80% of solid discharge during the flood period (Avoine, 1986). In 

the downstream part, the Seine estuary Turbidity Maximum (TM) is the second SPM stock with a 

tonnage rangin from 300,000 to 500,000tons (Avoine et al., 1981). During their transfer to the 

English Channel, the fine particles can be trapped in (i) the intertidal mudflats, preferential areas 

characterized by low hydrodynamics and generally sheltered of the flow, the main tidal current the 

Seine river and (ii) the TM. The Seine estuary is a strongly man-altered estuary with numerous 

facilities in order to secure navigation. One consequence of these developments is the tidal bore 

disappearance. 

In the upstream part, sedimentation occurs during the flood (flow > 800m3.s-1) with a 

higher mean water level causing permanent dewatering of the mudflats and the SPM settling. The 

sedimentation episode intensity depends on the flood intensity (pluri-centimetric during strong 

floods carrying larger quantities of SPM) (Guézennec et al., 1999). The gradual release of 

particles filed during the flood is mainly provided by tidal cycles during low flow periods (Deloffre 

et al., 2005). Finally, at the annual scale, the intertidal mudflats of this area seem close to 

balance. The rhythmites are not or poorly preserved on the lateral areas of the upper estuary, 

except in connected basins with the river Seine (i.e. docks), and developed sheltered area from 

the currents, where sedimentation and recording are almost continuously for several decades. 

Close to the mouth, the tidal influence in the deposit rhythms increases with abrupt 

periods of TM particles settling (centimeter to pluricentimeters per tide) preferentially during low 

water (TM not expelled by the Seine river) and during the largest spring tides (Lesourd et al., 

2003 ; Deloffre et al., 2006). The particles settled come from the TM. During the rest of the year, a 

tendency to erosion is recorded (in winter and in flood) following (i) tidal cycles (progressive 

erosion) and (ii) storm surges (erosion-time) (Le Hir et al., 2001). Just as in the upper estuary, the 

sedimentary evolution of the stock shows some stability indicating a lack of preservation of 

rhythmites on an annual basis (Deloffre et al., 2006). 

The Seine estuary middle part is not an intermediate between the upstream and the 

downstream behaviors. This area is strongly influenced by the flow and the inter-annual climatic 

cyclicity (6-7 years) (Massei et al., 2009). Plurimetric sedimentation occurs during low floods. The 

mudflat nourishment lasts during one to two years before reaching its size equilibrium, which 

allows the rhythmites preservation. Erosion is sudden and intense and it occurs during strong 

floods, removing the sedimentary stock and therefore not allowing conservation "long term" of 

these rhythmites. 

Although macrotidal estuarine environments are potentially suitable for sedimentary 

records of tidal cycles, their preservation is the Seine estuary is strongly limited by strong 

hydrodynamic variability and paroxysmal events. This strong variability is expressed at different 

time scales: (i) event (swell), (ii) daily / monthly (tidal cycles) or (iii) annual / pluri-annual 

79


(hydrologic variability). Anthropism (dikes, filling) promotes the increase in hydrodynamic, with a 

channel current velocities increase. These changes are responsible for a shift of the TM 

downstream and the muddy intertidal muddy surface reduction (Cuvilliez et al., 2009). It appears 

that sedimentation occurs during exceptionnal condition periods (flood, spring tides…) and in the 

actual hydrological conditions, erosion seems to be the normal behavior. Finally, in this macrotidal 

estuary, although sedimentation events are consistent (pluricentimetric) over short periods, the 

preservation rate of rhythmites is relatively low. Only a few areas in connection with the Seine 

river (docks) are likely to present a continuous sedimentation record in macrotidal estuary. 

energy distribution in a tide-dominated estuary (Dalrymple et al., 1992) and studied sites location 

Avoine, J., 1986. Evaluation des apports fluviatiles dans l’estuaire de la Seine. In Ifremer, editor, La baie de 

Seine (GRECO Manche) : Caen, Ifremer, 117-124. 

Avoine, J., Allen, G.P., Nichols, M., Salomon, J.C., Larsonneur, C., 1981. Suspended sediment transport in 

the Seine estuary, France: effect of man-made modifications on estuary-shelf. Sedimentology. Marine 

Geology, 40, 119–137. 

Cuvilliez, A., Deloffre, J., Lafite, R., Bessineton, C., 2009. Morphological responses of an estuarine mudflat 

to constructions since 1978 to 2005 : The Seine estuary (France). Geomorphology, 104, (3-4), 165-174. 

Dalrymple, R.W., Zaitlin, B.A., Boyd, R., 1992. Estuarine facies models: conceptual and stratigraphic 

implications BASIS. Journal of Sedimentary Petrology, 62, (6), 1130-1146. 

Deloffre, J., Lafite, R., Lesueur, P., Lesourd, S., Verney, R., Guézennec, L., 2005. Sedimentary processes 

on an intertidal mudflat in the upper macrotidal Seine estuary, France. Estuarine, Coastal and Shelf 

Science, 64, (4), 710-720. 

Deloffre, J., Lafite, R., Lesueur, P., Verney, R., Lesourd, S., Cuvilliez, A., Taylor, J., 2006. Controlling 

factors of rhythmic sedimentation processes on an intertidal estuarine mudflat – Role of the turbidity 

maximum in the macrotidal Seine estuary, France. Marine Geology, 235, (1-4), 151-164. 

Guézennec, L., Lafite, R., Dupont, J.P., Meyer, R., Boust, D., 1999. Hydrodynamics of suspended 

particulate matter in the freshwater zone of a macrotidal estuary (the Seine estuary, france). Estuaries, 22, 

(3A), 717-727. 

Le Hir, P., Ficht, A., Jacinto, R., Lesueur, P., Dupont, J.P., Lafite, R., Brenon, I., Thouvenin, B., Cugier, P., 

2001. Fine sediment transport and accumulations at the mouth of the seine estuary (France). Estuaries and 

Coasts, 24, (6), 950-963. 

Lesourd, S., Lesueur, P., Brun-Cottan, J.C., Garnaud, S., Poupinet, N., 2003. Seasonal variations in the 

characteristics of superficial sediments in a macrotidal estuary (the Seine inlet, France). Estuarine, Coastal 

and Shelf Science, 58, (1), 3-16. 

Massei, N., Laignel, B., Deloffre, J., Mesquita, J., Motelay-Massei, A., Lafite, R., Durand, A., 2009. 

Long-term hydrological changes of the Seine River flow (France) And their relation to North Atlantic 

Oscillation over the period 1950-2008. International Journal of Climatology, 30, (14), 2146-2154. 

Verney, R., Deloffre, J., Brun-Cottan, J.C., Lafite, R., 2007. The effect of wave-induced turbulence on 

intertidal mudflats : Impact of boat traffic and wind. Continental Shelf Research, 27, (5), 594-612. 

80


SEDIMENT TRANSPORT PATTERNS AND SOURCES IN A RIVER DELTA-TIDAL 

FLAT COMPLEX IN TAIWAN 

James T. LIU, Wayne, C. CHEN 

INSTITUTE OF MARINE GEOLOGY AND CHEMISTRY, NATIONAL SUN YAT-SEN UNIVERSITY, 70 

Lien-Hai rd., 80424, Kaohsiung, Taiwan, roc, james@mail.nsysu.edu.tw, e1002399@gmail.com 

Zhoushuei River has the largest sediment discharge (50-60 Mt) on the west coast in 

Taiwan. Its mouth is located on a mesotidal (tidal range between 2 and 4 m) coast. Because of 

the strong tidal currents and seasonal monsoon waves in the Taiwan Strait, the sediment 

exported by the river formed a small fan-shaped tidal delta and a large tidal depositional system 

located immediately north of the river mouth. This tidal system contains tidal ridges separated by 

large tidal channels. Swathbars separated by cross-bar channels are large secondary 

depositional features more or less perpendicular to the main tidal channel. Geomorphologically, 

the delta at the river mouth and the tidal flat seem to be one complex system. 

It is hypothesized that this system is the immediate/temporary sink of sediment exported by 

the river though plume-tide interaction. The sediment might be transported out of the tidal system 

during ebbing tide into the littoral drift and further dispersed by alongshore currents and 

tidal/coastal current systems. 

To test the hypothesis surfacial sediment samples from the river delta and the tidal flat 

complex were taken in May (the end of dry season) and September (end of the flood season) 

2010. The samples were analyzed for the grain-size composition of the original (Liu et al., 2002), 

the lithogenic and non-lithogenic fractions of the samples (Liu et al., 2009). Six grain-sizes 

classes were used in the analysis, including clay, silt, very fine sand, fine sand, medium sand, 

and coarse sand. The samples were also analyzed for their organic (TOC, TN) content and C/N 

ratio. Statistics-based trend analysis techniques (McLaren Model and Transport Vector) and the 

multi-vairate EOF analysis technique combined with ‘digital filters’ were used to decipher the 

information contained in the spatial grain-size distribution patterns (Liu et al, 2000, 2002). 

According to the McLaren Model, sediment transport directions in the study area are shown 

in Figure 1a for the dry season data set and Figure 1b for the wet season data set. Common 

themes in these two scenarios are the bi-directional transport along the surf zone on the outer 

edge of the complex, which is due to the tidal currents and seasonal littoral drift. In the dry 

season, the influence of the river is weak, and on the side-lobes of the delta the sediment 

transport patterns are bi-directional (landward and seaward) due the influence of the river effluent 

and tide (Fig. 1a). The sediment mainly moves from the river delta to the tidal flat (Fig. 1a). 

In the more energetic wet season where the water level is higher over the complex, 

bi-directional transport exists along the main tidal channel and along the upper tidal flat, the net 

sediment movement is still from the river into the tidal flat (Fig. 1b). Over the delta, due the 

increased river influence, the sediment transport patters are seaward except on the south side of 

the delta where secondary flood transport exists (Fig. 1b). 

Results from filtering and EOF technique show among the possible forcings of river 

discharge, tidal transport, wave sorting, and littoral drift, none of them is the dominant 

factor/forcing that influenced the spatial grain-size patterns observed in the dry season. In the wet 

season, the northbound littoral drift appears to be the dominant factor/forcing. This is because 

the incident monsoon waves are from the SW in the summer. Other forcings are of secondary 

importance. Despite of the large sediment load in the summer, most sediment discharged by the 

river bypasses the delta-tidal flat complex and is transported further away from the study area. 

However, the river is the primary source for organic material in the complex. Through grain-size 

affinity, sediment that is organic-rich and has stronger terrestrial signals (high C/N) is associated 

mostly with the distribution of clay in the upper tidal flat and river delta in both seasons. 

81


Sediment trend analysis results according to the McLaren Model for (a) the dry season and (b) wet season. 

The lengths and widths of the arrows have no magnitude implication. They merely indicate statistically 

valid transport directions. The black stars indicate the sampling locations. 

Liu, J.T., Huang, J.-S., and Chyan, J.-M., 2000. The coastal depositional system of a small mountainous 

river: a perspective from grain-size distributions. Marine Geology, 165 (1-4), 63-86. 

Liu, J.T., Liu, K.-j., and Huang, J.-S., 2002. The influence of a submarine canyon on river sediment 

dispersal and inner shelf sediment movements: a perspective from grain-size distributions. Marine 

Geology, 181 (4), 357-386. 

Liu, J.T., Hung, J.-J., and Huang, Y.-W., 2009. Partition of suspended and riverbed sediments related to 

the salt-wedge in the lower reaches of a small mountainous river. Marine Geology, 264, 152-164. 

82


TIDAL FACIES IN SILICICLASTIC, CARBONATE AND MIXED MICROTIDAL 

ANCIENT SYSTEMS OF SOUTHERN ITALY 

Sergio LONGHITANO*, Domenico CHIARELLA**, Luigi SPALLUTO*** 

*UNIVERSITY OF BASILICATA, DEPARTMENT OF GEOLOGICAL SCIENCES, Via Dell'Ateneo Lucano, 

10, 85100, Potenza, Italy, sergio.longhitano@unibas.it 

**WEATHERFORD PETROLEUM CONSULTANTS AS, Folke Bernardottevei, 5007, Bergen, Norway 

***UNIVERSITY OF BARI DIPARTIMENTO DI SCIENZE DELLA TERRA E GEOAMBIENTALI, Via 

Orabona, 4, 70100, Bari, Italy 

Tidalites are usually associated to meso-, macro- or mega-tidal oceanographic settings, 

where the tidal excursions are the main hydrodynamics in sediment distribution and organization 

along coastal environments (Longhitano et al., 2012a). However, also in microtidal settings (i.e., 

the Italian coastlines) tides may have influence on to the sediments, when: (i) tidally-driven 

currents are amplified throughout marine straits, as today along the Messina Strait; (ii) when 

other, usually dominant, hydrodynamic forces (i.e., waves or currents) are mitigated in their 

strength by coastal embayments, as in the Lagoon of Venice, or (iii) along barred coasts, where 

tidal waves enter bays isolated from the open sea by discontinuous sandy bars, as in the 

present-day Lagoon of Lesina. Tidal influence/dominance along microtidal coasts occurred also 

during the Mesozoic and the Cenozoic in a variety of ancient environments, presently cropping 

out in south Italy. 

Examples of ancient tidally-dominated/-influenced facies developed under microtidal 

conditions are widely detectable across southern Italy (Longhitano et al., 2012b). Tidalites were 

documented in: (i) terrigenous, siliciclastic-rich sandstones, (ii) carbonate, platform-like limestones 

and (iii) mixed, silici-/bioclastic sandstones. Each of these deposits recorded depositional systems 

that include different facies assemblages with highly varying properties, although the basic 

process was roughly the same. 

Three main field examples are proposed from the lower Pleistocene Catanzaro palaeo-strait 

(Calabria, Fig. 1A) (Longhitano et al., 2012b), the upper Cretaceous Apulian platform (Apulia, Fig. 

1B) (Spalluto, 2008), and the middle-upper Pliocene Acerenza palaeo-bay (Basilicata, Fig. 1C) 

(Chiarella et al., 2012). 

These case studies summarize the main facies differences and the petrophysical features 

of tidalite-bearing deposits accumulated in very different microtidal scenarios, having a 

fundamental role in reservoir characterisation and fluid migration models. 

83


Example of tidalites exposed in southern Italy. (A) Lowere Pleistocene dune-bedded siliciclastic sandstones 

from the Catanzaro Palaeostrait. (B) Upper Cretaceous stromatolitic limestones from the Apulia Platform. 

(C) Middle-upper Pliocene mixed, bioclastic/siliciclastic cross-bedded sandstones from the Acerenza 

Palaeobay. 

Chiarella D., Longhitano S.G., Sabato L., Tropeano M. (2012). Sedimentology and hydrodynamics of mixed 

(siliciclastic-bioclastic) shallow-marine deposits of Acerenza (Pliocene, Southern Apennines, Italy). Ital. J. 

Geosci., 131, 136-151. 

Longhitano S.G. , Mellere D., Steel R.J., Ainsworth B. (2012a). Tidal Depositional systems in the Rock 

Record: a Review and New Insights. In: Longhitano S.G., Mellere D., Ainsworth B. (Eds.) Modern and 

ancient depositional systems: perspectives, models and signatures, Sed. Geol. Special Issue, in press. 

Longhitano S.G. , Chiarella D., Di Stefano A., Messina C., Sabato L., Tropeano M. (2012b). Tidal 

signatures in Neogene to Quaternary mixed deposits of southern Italy straits and bays. In: Longhitano S.G., 

Mellere D., Ainsworth B. (Eds.) Modern and ancient depositional systems: perspectives, models and 

signatures, Sed. Geol. Special Issue, in press. 

Spalluto L. (2008). Sedimentology and high-resolution sequence stratigraphy of a lower Cretaceous 

shallow-water carbonate succession from the Western Gargano Promontory (Apulia, Southern Italy). 

GeoActa Spec. Publ. 1, 173-192. 

84


BENTHIC HABITAT DIVERSITY IN COARSE SEDIMENT UNDER HIGH MACROTIDAL 

ENVIRONMENT 

Sophie LOZACH*, Romain ABRAHAM**, Alexandrine BAFFREAU*, Jean-Claude DAUVIN*, Deny 

MALENGROS***, Emmanuel POIZOT****, Alain TRENTESAUX** 


sophie.lozach@unicaen.fr 

**UMR CNRS 8217 GEOSYSTEMES, Université Lille1 U.f.r. des Sciences de la Terre, Bâtiment sn5, 

59655, Villeneuve D'Ascq, France 

***UMR CNRS 8217 GEOSYSTEMES, Université Lille1 U.f.r. des Sciences de la Terre, Bâtiment sn5, 

59655, Villeneuve D’ascq, France 

****GEOCEANO, Cnam/intechmer bp 324, 50110, Tourlaville, France 

EUNIS (European Nature Information System) is the habitat typology of reference in Europe 

but it must be implemented by new observations, particularly for the more detailed levels of the 

classification in coarse sediments which were historically less explored because of sampling 

difficulties. 

Two surveys in 2010 and 2011 permitted to sample twelve rectangular areas in the mid part 

of the Channel dominated by coarse sediment habitats in a high hydrodynamic environment 

strongly influenced by tidal currents (see Trentesaux et al., this conference for the map). During 

the survey, four longitudinal side-scan sonar (SSS) profiles were realised (~10 nm length) in each 

area allowing a real time selection of sampling areas. A minimum of four 0.25 m² Hamon grab 

sampling stations for quantitative macrofaunal and sediment analysis and two video footages 

(ROV Seabotix LBV200) were selected in each area (see figure). The main objectives of this 

study were to re-assess the EUNIS typology along an east-west gradient in the English Channel, 

and to find a way to integrate acoustic information in the description and mapping of the habitats 

which is not yet taken into account. 

The sampling protocol provided five descriptors of the benthic environment that had 

different levels of benthic habitat structure: (i) small scale infauna distribution (grabs), (ii) small 

scale epifauna distribution (grabs), (iii) sediment grain size and pictures of collected sediments 

(grab), (iv) seabed morphology (SSS) and (v) macrofauna and megafauna seascape (ROV). All 

this information will be integrated in the EUNIS habitat typology taking into account mainly the 

type sedimentary and benthic macrofauna. This poster presents an approach that follows different 

steps: 

- First of all, a coding for side-scan sonar images was developed to incorporate seabed 

morphology descriptions. For this, it is distinguished different types of seabed morphology in the 

observed acoustic images that has compared with general seabed features previously described 

in publications (see Ashley, 1990) to get different ‘types’ of sonar signatures. 

- Then, as views of the benthic habitat were obtained at different scales according to the 

gear used (ROV or grab), the biological data is processed with the different available descriptors 

to improve the EUNIS habitats coding. 

- The final step was to cross-check EUNIS interpretation with seabed signatures coding and 

integrated these descriptions into benthic habitat typology. 

85


From the left to the right: the side-scan sonar, the Hamon grab and the ROV Seabotix LBV200L. Pictures 

below show examples of raw observation obtain during the survey by these equipments. 

86


EFFECT OF THE 2011 GIANT TSUNAMI ON A SANDY BEACH AT OARAI, EASTERN 

JAPAN 

Yasuhiko MAKINO*, Shota ARAI**, Takashi ITO**, Futoshi NANAYAMA*** 

*IBARAKI UNIV., Bunkyou 2-1-1, 310-8512, Mito, Japan, makinoy@mx.ibaraki.ac.jp 

**IBARAKI UNIV.,, Bunkyou 2-1-1, 310-8512, Mito, Japan 

***GSJ/AIST, Higashi, 305-8567, Tsukuba, Japan 

Introduction 

The 2011 Tohoku earthquake (Mw 9.0) occurred in the Japan Trench on March 11 and 

caused a giant tsunami, which struck the coasts of countries bordering the Pacific Ocean. About 

twenty thousand people in eastern Japan were dead or missing as a result of the earthquake and 

tsunami. The Oarai Sun Beach on the Pacific coast of eastern Japan near Ibaraki University was 

struck by three tsunami waves, the third of which was the highest, at 4.0 m. 

We investigated inundation of the sandy beach by the tsunami, the redistribution of sandy 

sediments, and the current system of the 2011 giant tsunami by examination of changes to the 

topography of the beach, sedimentary structures developed there, and damage to man-made 

structures on and near the sandy beach. 

Results 

1. Remote imagery 

We searched the Internet for information about the Oarai area after the tsunami. Satellite 

images and aerial photographs provided information on the area and depth of inundation and on 

changes to the beach topography. After the tsunami, new channels had been formed in the wide 

backshore area of the beach. Before the tsunami, the backshore area was flat and grass covered. 

The configuration of the channels shows that they were formed by return flows. 

2. Field work 

The information we obtained from the Internet was confirmed during our field work. We 

conducted field investigations of the depth of inundation and the thickness of sand deposits along 

two transect lines (Fig. 1). Line IH was 700 m long and line ON was 1200 m long. Sand deposits 

along both lines were in the form of a thin veneer, less than 6 cm thick. 

The tsunami current system on Oarai Sun Beach consisted of run-up flows travelling from 

S to N and return flows travelling NW to SE. 

Discussion 

The run-up flows appear to have been controlled and redirected by the position of a raised 

road between the residential area and the port area, and the thickness of sand it deposited was a 

thin veneer. The current system indicates that run-up flows were destructive over a very short 

time, but the return flows were mainly within newly cut channels, and exerted traction for a longer 

period of time. Evidence of the strength of the run-up surge is seen in the transport of two steel 

bridge girders (10 m long) over a distance of 100 m, fishing boats and many shipping containers 

moved landward from the port area, bending of steel poles, tilting of thick wooden poles, and the 

creation of plunge pools. 

87


Inundation area at Oarai Sun Beach 

88


SEDIMENTATION OF THE 2011 GIANT TSUNAMI ON A SANDY BEACH ON THE 

PACIFIC COAST OF EASTERN JAPAN 

Yasuhiko MAKINO 

IBARAKI UNIV., Bunkyou 2-1-1, 310-8512, Mito, Japan, makinoy@mx.ibaraki.ac.jp 

Introduction 

The Pacific coast of the Japanese Islands has been struck by many giant tsunamis over 

geological time. Giant tsunamis caused by earthquakes in and around the Japan Trench have 

occurred every several hundred to one thousand years. Very few studies have documented the 

changes to sandy beach sediments immediately after such huge tsunamis, given the rarity of 

these events. The 2011 tsunami provided an opportunity to study the effects of a large tsunami on 

a sandy beach. 

The 2011 Tohoku earthquake occurred in the Japan Trench off Sanriku at 14:46 JST on 

March 11. About 30 minutes later, a giant tsunami struck the Pacific coast of eastern Japan, 

including Oarai Sun Beach at Oarai in Ibaraki Prefecture. Oarai Sun Beach, which is about 1000 

m wide and extends 500 m inland, was struck by three tsunami waves. The third run-up flow was 

at 16:52 JST and, at 4 m, was the highest wave. The topography of the sandy beach was 

changed by the tsunami waves, various new sedimentary structures were formed, and man-made 

structures were damaged. These changes on the beach provide information about the current 

systems of the tsunami. 

Current system 

Evidence of the direction of flow of the tsunami on the beach was examined during field 

surveys and from aerial photographs. The first tsunami wave struck Oarai at 15:20 JST, and the 

third wave, at 16:52 JST, was the biggest, with a height of 4.0 m at Oarai port. Run-up flows were 

from S to N, and return flows were from NW to SE. 

Evidence of the tsunami on the beach 

Run-up flows 

Directional features and other evidence of the passage of the run-up flows indicate a 

surge of great strength. 

1. Two very heavy steel bridge girders (10 m long) were carried about 100 m inland. 

2. Several wooden poles supporting nets on beach volleyball courts were bent landward or 

broken. 

3. Depressions (plunge pools) were formed in the pavement of a parking area on the 

landward side of low steel fences within the parking area. The pools were elliptical with their long 

axes in the N–S direction. 

4. Some steel poles (1 m height) of a soft net fence were bent inland. 

5. Fishing boats were carried landward by up to several hundred meters. 

Return flows 

1. Erosional channels formed by return flows widened seaward. 

2. Many tiles (30 × 30 cm, 10 cm thick) from a 300-m-long tiled sidewalk aligned 

perpendicular to the beach were torn up by the run-up flow and deposited on the N side of the 

sidewalk. These were rearranged in imbricate structures by the return flow. 

3. Wooden poles supporting nets in some beach volleyball courts were bent seaward. 

Discussion 

Run-up flow 

The run-up flows formed a strong surge, probably of 4 m height on the beach front, which 

flowed over the backshore and damaged and distorted man-made structures there over a 

relatively brief time period. The total amount of sand eroded by the run-up flows may have been 

less than that of the return flows, because sporadic areas of grass on the wide backshore were 

exposed after the tsunami. Further inland, sand eroded by run-up flows was mainly deposited 

under hedges. 

Return flow 

Return flows had more time to exert their effects than run-up flows, and they eroded large 

volumes of backshore sand, creating four or five seaward-widening erosional channels on the 

previously flat backshore (Fig. 1). 

89


Current system of the 2011 giant tsunami at Oarai Sun Beach 

90


FRENCH FLANDERS FIELDS: DECIPHERING THE HOLOCENE SEDIMENTARY 

HISTORY OF THE COASTAL PLAIN OF NORTHERN FRANCE 

José MARGOTTA, Alain TRENTESAUX, Nicolas TRIBOVILLARD, Romain ABRAHAM 

UMR 8217 GEOSYSTEMES, Bâtiment sn5 Cité Scientifique, 59655, Villeneuve D'Ascq, France, 

ja.margotta-coronado@etudiant.univ-lille1.fr, Alain.Trentesaux@univ-lille1.fr, 

Nicolas.Tribovillard@univ-lille1.fr, romain.abraham@univ-lille1.fr 

The French Flanders Fields represent the southern end of the North Sea large coastal plain 

that continues northward to the Danish coast. In this area, the Holocene infillings and their 

sedimentary processes have been studied for decades, to decipher the stratigraphic succession 

and paleoclimatic changes that occurred during this period. However, in spite of several 

stratigraphic analyzes that have been carried out in the area, it has not been possible yet to 

establish a robust stratigraphic frame for the evolution of the Holocene. 

In this sense, new integrative methodologies implemented in coastal areas, such as very 

high-resolution seismic surveys, have allowed to reveal significant new information in contrast to 

the studies based on isolated outcrops and boreholes. Integrating all these data in one dataset 

provides the opportunity to develop a model to better describe the architecture of the subsurface. 

In this view, a very high-resolution seismic survey was performed along the French Flemish 

waterways open to navigation. The data consist in a series of seismic profiles that illustrate the 

first 30 meters of the subsoil and show distinctive features of the Holocene infillings. 

Two stratigraphic units have been defined from the seismic profiles; they are separated by 

an unconformity surface with an unresolved chronostratigraphic position. Available boreholes and 

outcrops display the internal characteristics of these stratigraphic units and give an insight into the 

composition of the substrate and the constant tidal influence. The integration of all the data 

provides some clues to understand the overall sedimentary processes at the origin of the deposits 

and the evolution of these lowlands. 

91


Location of study zone showing the French Flemish watercourses and indicating the distribution of seismic 

surveys 

92


IMPACTS OF FLOODS AND CYCLONES ON MANGROVE OVER A SECTOR OF THE 

SAVE RIVER DELTA PLAIN, MOZAMBIQUE 

Elidio MASSUANGANHE*, Salomao BANDEIRA**, Lars-Ove WESTERBERG* 

*DEPARTMENT OF PHYSICAL GEOGRAPHY AND QUATERNARY GEOLOGY, STOCKHOLM 

UNIVERSITY, Svante Arrhenius vag 8c, Frescati, SE106 91, Stockholm, Sweden, 

geomuzaza2000@yahoo.com.br, low@natgeo.su.se 

**DEPARTMENT OF BIOLOGICAL SCIENCES, FACULTY OF SCIENCES, EDUARDO MONDLANE 

UNIVERSITY, Av. Julius Nyerere 3453, 257, Maputo, Mozambique, sband@uem.mz 

Located in Southern Mozambique, the Save River delta plain is an example of estuarine 

deltas with extensive mangrove forests that face threats of climate-related events. During the last 

decade Save River delta plain has been severely affected by recurring high-magnitude weather 

events (e.g. the 1999-2000 floods and cyclone, and the cyclones Japhet (2003) and Favio (2007)) 

that prompted destruction in vegetation, notably on mangroves. However, the impact pattern of 

the mangrove degradation is unclear, given the multiple ways that the floods and cyclones act on 

the study area. This study aims to assess the recent impacts of recurrent floods and cyclones in 

the landscape over a sector of the Save River delta plain, with emphasis on mangrove and 

geomorphology. Aerial photographs and Google Earth images of Save River delta were 

interpreted to find the geomorphological units. Additional field studies were undertaken to 

complement the interpretation and to evaluate the impacts of extreme weather events. The 

geomorphological map produced shows that the study area is composed mainly of beach sand 

and embryonic coastal dunes, beach ridges, marsh, alluvial plain and eluvial depressions (Fig. 1). 

The beach ridges are located in the northern part of the study area reflecting a prograding 

shoreline. Today, embryonic coastal dunes and sand beaches border the delta plain to the open 

sea, acting as a barrier for offshore winds and waves. Mangrove is distributed throughout the 

study area, but it is more luxuriant in the marshland and channel fill where a thick layer of muddy 

sediments is available, and brackish water exchange is frequent. Mangrove dieback is evident in 

different areas, but most accentuated in the mouths of tidal outlet channels exposed to the open 

sea. At such locations (e.g. Waypoint 22 and 23, Fig. 1), extensive areas of the mangrove are 

physically impacted by winds and waves (Fig. 1 B1) during the cyclone landfall. At this site, 

mangroves are also negatively affected by a chenier of beach sand deposited during cyclone 

Eline (2000). In some sectors of the inland side of the barrier formed by beach sand and 

embryonic coastal dunes, the marshland was recently covered by a flush of sediments that 

overtopped the barrier dune during extreme weather event (Fig. 1 B2). This has affected the 

mangrove development negatively. On the other hand, other areas located on the sheltered side 

of the spit (e.g. waypoint 115) show flourishing mangrove and a new mangrove nursery is 

developing in a northerly direction as the spit grows and siltation takes place in the bay (Fig. 1 

B3). During floods the banks of the tidal channels experience accelerated erosion resulting in 

both destruction of the terrestrial and mangrove vegetation on one side and sediment accretion 

on the other side. At the accreted areas mangrove flourishes. Vertical fine sand accretion in the 

waypoint 107 was attributed to recent sediment reworking from the channel and it is affecting the 

mangrove development negatively. 

This work has shown the need to understand the geomorphological process dynamics in 

order to accurately assess the net effects on mangroves of low-magnitude versus high-magnitude 

weather events. The geomorphology controls the evolution pattern of mangrove forest as part of 

the normal landscape dynamic, but it also plays an important role controlling high magnitude 

weather related events. 

93


A1- Map showing the main geomorphological unities of the study area; B1 – mangrove impacted directly by 

cyclone at the Waypoint 23; B2 – Marshland covered by dune sand from the barrier overtopping (Waypoint 

103) and B3 – Very recent sheltered bay (at the right side of the photo) where new mangrove nursery 

develops. 

94


TRANSGRESSIVE, HEADLAND-ATTACHED TIDAL SAND RIDGES IN THE RODA 

FORMATION, NORTHERN SPAIN 

Kain MICHAUD*, Robert W. DALRYMPLE** 

*PETREL ROBERTSON CONSULTING LTD., Suite 500, 736 8th Ave. sw, T2P 1H4, Calgary, Alberta, 

Canada, kain_michaud@hotmail.com 

**DEPT. GEOL. SCI. & GEOL. ENG., Queen'S University, K7L 3N6, Kingston, Ontario, Canada, 

dalrymple@geol.queensu.ca 

In modern shallow-marine settings, tidal currents are often an effective agent of 

transgressive sea-floor reworking. Where sand is present in sufficient quantity and tidal currents 

are fast enough, tidally moved sediment can accumulate to form transgressive sand ridges. Such 

ridges are often composed of well-sorted sand and can be overlain by shelf mudstone, making 

them a clear target for oil and gas exploration. While transgressive tidal ridges are abundant in 

the modern, uncontested ancient counterparts are comparably few, largely because detailed 

studies of their internal facies are rare. This presentation outlines the facies, internal architecture, 

and stratigraphic framework of 6 transgressive tidal ridges. The quality of outcrop exposure is 

excellent, and allows collection of detailed information about the facies, paleocurrent patterns, 

internal architecture and stratigraphic positioning within regressive-transgressive cycles for all 6 

ridges. 

The presence of tidal cross bedding in the Roda Member is well known (Nio 1976; 

Lopez-Blanco et al., 2003; Tinterri et al., 2007) and has been interpreted as being due to 

reworking of contemporaneous delta-front sands by tidal currents. New work, including 

comprehensive logging of the entire Roda Formation (including the overlying Esdolomada 

Member), indicates that tidal sands accumulated at the distal end of 6 of the 18 progradational 

tongues. Detailed outcrop mapping and tracing of the tidal sand bodies shows that they do not 

interfinger with progradational delta lobes, but instead overlie and/or lie immediately seaward of 

the tip of the tongue, indicating they were deposited after deltaic progradation had ended, during 

the ensuing transgression. 

The tidal sands are reconstructed as headland-attached sand ridges that are present only 

on those tongues that prograde more than 2 kilometers basinward: only these tongues protrude 

far enough out into the basin to constrict the shore-parallel tidal currents sufficiently to cause tidal 

reworking of the delta lobe. Each ridge is situated immediately to the west of a deltaic headland, 

further implying local dominance of a westerly flowing ebb tide within the basin. As evidenced by 

paleocurrent analysis for each of the ridges, the southwestern (offshore) side of each ridge was 

dominated by the westerly flowly ebb current whereas the sheltered landward side of the ridge 

was typically dominated by the easterly flowing flood tide. Accretion occurred on both sides of the 

ridges, but with seaward accretion predominating. Facies are quite variable, ranging from a 

high-energy end member dominated by large-scale trough cross bedding to a low-energy end 

member dominated by ripple cross-laminated sand. 

Rates of subsidence, distance from the depocentre, current speed, sedimentation rate and 

water depth are directly linked to facies variability and their stacking pattern within the ridges. 

• Where subsidence rates were high (Esdolomada Member), sediment was effectively 

trapped in up-system estuaries during transgressions, allowing for carbonate drapes to form caps 

on the ridges. Well-developed carbonate caps did not form during the Roda Member because 

subsidence rates were lower, allowing for more rapid progradation of the delta, limiting carbonate 

accumulation on the ridges. 

• In general, current speeds are highest at the ridge crest, such that the internal facies 

change from cross-bedded sandstone at the crest to rippled sandstone and eventually 

interlaminated sands and muds/silts at the toe of the ridge flanks. 

• If the ridge grows high enough, strong tidal currents produce cross-ridge incision, forming 

swatchways. 

• Sandy ridges with cross beds (high sedimentation rate) are less bioturbated than finer 

grained ridges composed of ripple cross lamination (coincident with a lower average 

sedimentation rate). 

• Neap-spring cyclicity visibly affects the preserved bioturbation intensity and diversity within 

bed-sets. The thin tidal bundles deposited during neap-tide periods are significantly more 

bioturbated than the thicker bundles formed during spring tides. 

Changes in environmental conditions that accompanied the transgression are sometimes, 

but not always, recorded within the ridges. Some ridges were drowned (relative sea-level rise 

95


outpaced ridge growth) and are mantled by lower-energy sandy facies deposited as the ridge 

became moribund. More rapidly growing ridges, by contrast, retain a core of lower energy 

deposits draped by shallower-water deposits. 

Simplified proximal-distal cross section of the Roda Formation, showing the stratigraphic and geographic 

location of the headland-attached transgressive sand ridges (yellow). 

LOPEZ-BLANCO, M., MARZO, M., and MUNOZ, J.A., 2003, Low-amplitude, synsedimentary folding of a 

deltaic complex: Roda Sandstone (lower Eocene), South-Pyrenean Foreland Basin: Basin Research, v. 15, 

p. 73-95. 

NIO, S.D., 1976, Marine transgressions as a factor in the formation of sandwave complexes: Geologie En 

Mijnbouw, v. 55, p. 18-40. 

TINTERRI, R., 2007, The lower Eocene Roda Sandstone (south-central Pyrenees): An example of a 

flood-dominated river-delta system in a tectonically controlled basin: Rivista Italiana di Paleontologia e 

Stratigrapfia, v. 113, no. 2, p. 223-255. 

96


LATE QUATERNARY STRATIGRAPHY AND MORPHODYNAMICS OF MACROTIDAL 

SAND BODIES IN THE WESTERN COAST OF KOREA 

Soo Chul PARK 

DEPARTMENT OF OCEANOGRAPHY, CHUNGNAM NATIONAL UNIVERSITY, Gung-Dong 220, 

Yuseong-Ku, 305-350, Daejeon, Korea, scpark@cnu.ac.kr 

The west coast of Korea (eastern Yellow Sea) is a well-known macrotidal environment with 

tidal ranges of up to 9 m. Sand bodies are prominent sedimentary features in this area and most 

of them occur either as a series of linear or individual sand bodies. The shelf sand bodies are 

present in water depths of 50–90 m and show large, elongate shapes with a length up to 200 km. 

In contrast, the nearshore sand bodies are much smaller in size (up to 34 km length) and occur in 

water depths shallower than about 30 m. In this study, we analyze a number of sediment cores, 

high-resolution seismic (sparker) profiles and side-scan sonar images to understand the 

stratigraphy and morphodynamics of these sand bodies, using radiocarbon datings to constrain 

the ages of the ridges. 

The coastal sand bodies above the acoustic basement can be divided into three 

stratigraphic units (N1, N2, and N3 in a descending order) based on the mid-reflecors and 

acoustic characters. The upper unit (N1) is the main body of the ridges with a thickness of 5-25 

m, which formed during the recent highstand of sea-level (


Seismic profiles of the nearshore (top) and shelf (bottom) sand bodies 

98


RHYTHMIC CLIMBING RIPPLES LAMINATION FROM MODERN (BAY OF THE 

MONT-SAINT-MICHEL, FRANCE) AND ANCIENT (DUR AT TALAH, PALEOGENE, 

LIBYA) TIDAL DEPOSITIONAL ENVIRONMENTS: DESCRIPTION, GENESIS, 

SIGNIFICANCE AND NEW CRITERION FOR TIDAL EVIDENCE 

Jonathan PELLETIER*, Ashour ABOUESSA*, Philippe DURINGER*, Mathieu SCHUSTER*, 

Jean-François GHIENNE*, Jean-Loup RUBINO** 

*INSTITUT DE PHYSIQUE DU GLOBE DE STRASBOURG (IPGS)-UMR 7516; UNIVERSITE DE 

STRASBOURG (UDS)/EOST/CNRS, 1 rue Blessig, 67084, Strasbourg, France, 

jonathan.pelletier@aliceadsl.fr 

**TOTAL, CENTRE SCIENTIFIQUE ET TECHNIQUE JEAN FEGER, Avenue Larribau, 64000, Pau, France 

The New Idam Unit of the Dur At Talah Formation is known to have been deposited in a 

tidal environment (Abouessa et al., 2012; Pelletier et al., 2012a this congress). Some of the 

associated deposits display typical Rhythmic Climbing Ripple (RCR; Choi, 2010) sequences. 

From a distance, RCR laminations look like classical climbing ripples laminations, but a 

closer observation reveals alternations of sand and mud laminations which suggest that they form 

step by step (i.e. rythmically) rather than continuously. RCR have been described from modern 

environments (Lanier and Tessier, 1998; Choi, 2010) and rarely reported from the geological 

record (Lanier and Tessier, 1998; Chanda and Bhattacharyya, 1974). This work displays 

Rhythmic Climbing Ripple structures from both modern (MSM) and ancient (DAT) tidal systems 

and reveals RCR as being a key feature to identify tide-driven depositional process. 

For both cases, RCR sequences are characterized by rhythmic gradual thinning and 

thickening of cross-laminae expressed by neap-spring tidal cycles, indicating a strong control by 

tidal dynamic. A fine observation of modern Mont-Saint-Michel Bay RCR shows that they are, 

most of the time, generated in upper intertidal domain in inclined heterolithic stratification (IHS) of 

tidal channels. Indeed, RCR record flood and ebb markers; the morphologic dissymmetry is due 

to the asymmetric energy between dominant and subordinate currents. Mud couplets, 

corresponding to the slack water phases of flood and ebb tides, should give evidence of 

subaquatic genesis but it seems that the mud drape corresponding to the ebb slack water is an 

intermediate settling of mud occurring during the ebb tide way down. These structures are formed 

in a narrow interval in tidal channel IHS indicative of a precise elevation. Moreover, new 

diagnostic criteria of morphology have been observed to define these ripples. For example, a new 

recognition criterion for tidal dynamic was deducted and observed in these structures; in most of 

cases, the RCR lee sides seem notably eroded, contrary to conventional climbing ripples. 

This study is principally focused on the centimetric to decimetric-scaled description of these 

sedimentary structures as well as the comparison with ancient series. These are also indicative of 

paleogeography. This work tries to demonstrate and suggests first, indirectly, that macro to 

mesotidal regime of the Tethian Sea prevailed on the Sirtic paleocoast, that these structures were 

formed in intertidal and/to subtidal domain respectively in MSM Bay and in Libyan deposits, and 

finally, that the tidal regime of the Tethian Sea in the Sirt embayment was certainly semi-diurnal. 

This comparison between modern MSM Bay facies and ancient DAT facies seems to be a 

good tool to restrict environment and dynamic conditions and reveals RCR are a robust criterion 

to identify tidal dynamic. 

99


Comparison between modern RCR from the Mont-Saint-Michel Bay (MSM) and ancient RCR from the Dur 

At Talah (DAT): (A) Rhythmic climbing ripple (RCR) sequence showing a neap-spring cyclicity (N-S), note 

the slight lee-side erosion (black arrows) and the ripple cap (c) generated by a subordinate current; (B) 

Modern RCR sequence showing exactly same characteristics than A; (C) Close-view of ripple laminations 

underlined by double mud drapes (yellow and red lines) generated by slack water periods (of ebb and 

flood); (D) Close-view of modern RCR exposing well-preserved double mud drapes, note the slight lee-side 

erosion. 

100


THE GEOLOGICAL RECORD OF TIDAL DYNAMIC: DIVERSITY OF ASSOCIATED 

DEPOSITS AND MULTI-SCALE CYCLES FROM THE DUR AT TALAH FORMATION 

(UPPER EOCENE, SIRT BASIN, LIBYA) 

Jonathan PELLETIER*, Ashour ABOUESSA*, Philippe DURINGER*, Mathieu SCHUSTER*, 

Jean-Loup RUBINO** 

*INSTITUT DE PHYSIQUE DU GLOBE DE STRASBOURG (IPGS)-UMR 7516; UNIVERSITE DE 

STRASBOURG (UDS)/EOST/CNRS, 1 rue Blessig, 67084, Strasbourg, France, 

jonathan.pelletier@aliceadsl.fr 


Dur At Talah sequence is outcropping in the Abu Tumayam Trough, in the southern part of 

the Sirt Basin (Libya). This formation consists of tidal marine deposits at the base (New Idam 

Unit) and fluvial deposits at the top (Sarir Unit). This stratigraphic succession highlights a 

regressive trend attributed to the upper Eocene (Abouessa et al., 2012). 

Sedimentological investigations based on lithofacies and ichnofacies suggest that the 

depositional environments were mainly dominated by a tidal dynamic. Characterization of this 

tidal dynamic is focused on diagnostic sedimentary structures and their associated sequences. 

Several paleoenvironments have been defined for the New Idam Unit: the basal part of this unit is 

built up of an intertidal to supratidal flat system associated with oyster patches. The medium part 

is characterized by an estuarine channels belt. The upper part of the New Idam Unit exposes 

typical facies of tidal flats and prograding bar system (mouth bars?). The extremely good quality 

of preservation of sedimentary structures and sequences allows to investigate the recording of 

tidal cycles at various scales of time, from the elementary tidal cycle to the solsticial cycles. A 

comparison between modern Mont-Saint-Michel Bay facies and ancient Dur At Talah facies was 

proposed to calibrate facies and paleoenvironments. 

These tidal cyclicities are recorded through several sedimentary structures and lamination 

morphologies. Tidal overprint can be expressed inside horizontal laminations, ripples (flaser, wavy 

or lenticular) as well as megaripples. And this spectrum of morphologies is preserved into 

sedimentary bodies such as inclined heterolithic stratifications (IHS) of tidal channels. 

The elementary recording is made of mud-sand couplet corresponding to one tide event 

(slack and flood/ebb). The next scale recording corresponds to the neap-spring cycle and it is 

characterized by a contraction-dilation of ripple bundles. Finally, a higher wavelength cycle is 

recognizable, likely corresponding to a solsticial cyclicity. All these cycles have been identified for 

large-scale sedimentary bodies attributed to tidal channels and are best expressed within IHS. 

These cycles can be used as a chronometer for the timing of tidal channel migration and channel 

infilling. From a basic calculation based on the tidal cycle counting, a hypothetic migration rate 

was deduced. 

Calculation of tidal cycles recorded inside IHS gives a lateral migration rate between 0,4 to 

2 m/month and a channel infilling average between 15-20 years. This postulate is valid for Dur At 

Talah tidal channels and probably for equivalent in size and hydrodynamic parameters (e.g. tidal 

range) modern tidal channels. Finally, modern analogue such as Mont-Saint-Michel Bay facies is 

a good tool to compare tidal cyclicities and tidal structures and were useful for 

paleoenvironmental reconstruction. 

101


(A) Inclined heterolithic Stratifications (IHS) of tidal Channel; (B) Tidalite pin-stripe facies in vertical 

accretion; (C) Neap (n)/spring (s) cyclicity recorded in tidal channel facies; (D) Flaser bedding showing the 

bidirectionality of elementary ebb and flood curents (black arrows). 

102


TIDE-INFLUENCED FLUVIAL-DELTAIC SEDIMENTS VERSUS CONTINENTAL 

SANDY-MUDDY FLAT DEPOSITS: EVIDENCE FROM THE HUERTELES FM (EARLY 

CRETACEOUS, N SPAIN) 

I. Emma QUIJADA, Pablo SUAREZ-GONZALEZ, M. Isabel BENITO, Ramón MAS 

STRATIGRAPHY DPT.-COMPLUTENSE UNIV. OF MADRID-IGEO (CSIC-UCM), José Antonio Novais 2, 

28040, Madrid, Spain, equijada@geo.ucm.es 

Recognizing and interpreting features attributable to tidal influence in the sedimentary 

record may be difficult in certain tidal settings, such as fluvial-tidal transition estuaries, fluvial-tidal 

deltas and protected inland tidal embayments (e.g. Kvale & Archer, 1990; Gingras, 2002; 

Hovikoski, 2005, Rebata et al., 2006). In these settings, clear evidence of tidal influence, such as 

tidal bundles, herringbone structures or biological features, may be absent. Mixed 

siliciclastic-carbonate Huérteles Fm, from the Cameros Basin (Early Cretaceous, N Spain), poses 

a challenging sedimentological problem as it displays several features suggesting tidal influence 

but some other evidences, such as marine biota, are lacking. 

The Huérteles Fm was deposited during the Berriasian in the Cameros Basin, a Tithonian to 

Albian rift basin situated in northern Spain. This basin comprises more than 9000m of 

stratigraphic record, including essentially alluvial, fluvial and lacustrine deposits (Mas et al., 

2002). This record has been subdivided in 8 depositional sequences limited by unconformities 

(Mas et al., 2002): the Huérteles Fm is part of the third one. 

The Huérteles Fm consists of siliciclastic deposits in the central area of the basin and 

changes to coeval carbonate-evaporitic deposits to the eastern area. The siliciclastic deposits, 

made up of channelled sandstones, laminated mudstones and fine-grained sandstones, have 

been interpreted as deposited in continental sandy-muddy flats and meandering fluvial systems 

(Gómez-Fernández & Meléndez, 1994). Several sedimentary features, such as sandstone 

channelled beds and mudcracked laminated lutites, the lack of marine fossil remains and the 

presence of reptile fossil remains and footprints (Fig. 1) led to interpret these siliciclastic deposits 

as formed in a continental setting. In addition, carbonates and evaporites, laterally related and 

interbedded with the siliciclastics, do not contain marine fossils and do not display sedimentary 

features clearly indicating a marine depositional setting. They are made up of laminated 

carbonates and evaporites (Fig. 2-3) and massive carbonates with large pseudomorphs after 

gypsum. Their fossil content is limited to stromatolites, ostracods and occasional charophytes. 

Nevertheless, several sedimentary structures of the siliciclastic deposits lead us to a 

different interpretation. The presence of inclined heterolithic stratification (IHS) within channelled 

beds (Fig. 4), abundant flaser, wavy and lenticular stratification (frequently within the IHS) (Fig. 

5-6), rhythmic alternations of sandstones and lutites (Fig. 5) and occasional bi-polar current 

indicators suggest that these siliciclastic deposits were formed in tidally-influenced fluvial-deltaic 

environments. In such context, the carbonate and evaporite deposits would have been formed in 

a coastal environment. Marine influence in these carbonate-evaporitic areas is consistent with the 

large input of sulphate ions into these settings and with ostracod assemblages indicating mixed 

fresh and brackish water environments (Schudack & Schudack, 2009). 

The absence of marine fossils in the Huérteles Fm needs not be explained by a continental 

setting. Instead, a fresh to brackish tidal environment, such as the Upper San Francisco 

Estuary/Sacramento Delta (California) during the late Holocene (Wells & Goman, 1995), could 

explain this lack of marine organisms. Some other reasons for the scarcity of biota in the 

proposed sedimentary environments may be high sedimentation rates, rapid salinity fluctuations 

and acidic ground or surface waters (Kvale & Archer, 1990). 

The Colorado River Delta and the Tigris-Euphrates Delta could represent two present-day 

analogues for siliciclastic tidal environments laterally related to evaporitic depositional settings 

similar to the proposed for the Huérteles Fm. However, in both modern analogues, the evaporites 

are interbedded with siliciclastics, while in the studied unit, they are interbedded with carbonates. 

Probably a wide and restricted area where siliciclastic discharges were scarce developed in the 

eastern Cameros Basin, allowing particularly deposition of carbonate and evaporite in this more 

distal zone. 

103


Gingras, M.K., Räsänen, M. & Ranzi, A., 2002. Palaios 17, 591-601. 

Gómez-Fernández, J.C. & Meléndez, N., 1994. Journal of Paleolimnology 11, 91-107. 

Hovikoski, J., 2005. Geology 33, 177-180. 

Kvale, E.P. & Archer, A.W.,1990. Journal of Sedimentary Petrology 60, 563-574. 

Mas, R., Benito, M.I., Arribas, J., Serrano, A., Guimerà, J., Alonso, A. & Alonso-Azcárate, J., 2002. Zubía 

14, 9-64. 

Rebata-H., L.A., Gingras, M.K., Räsänen & M.E. Barbieri, M., 2006. Sedimentology 53, 971-1013. 

Schudack, S. & Schudack, M., 2009. Journal of Iberian Geology 35, 141-168. 

Wells, L.E. & Goman, M., 1995. In: Isaacs & Tharp (eds.), Proceedings of the 11th Annual Pacific Climate 

(PACLIM) Workshop, 185-198. 

104


UNDERSTANDING THE DEPOSITION OF TIDALLY DEPOSITED MUDSTONES: AN 

EXAMPLE FROM THE TILJE FORMATION (JURASSIC), OFFSHORE NORWAY 

Geoff REITH*, Robert W. DALRYMPLE*, Duncan MACKAY**, Aitor ICHASO*** 


reith.geoff@gmail.com, dalrymple@geol.queensu.ca 

**P1 ENERGY, Suite 700, 440 - 2nd ave sw, T2P 5E9, Calgary, Alberta, Canada, 

duncanamackay@yahoo.com 

***SHELL CANADA LTD., 400 - 4th ave sw, T2P 2H5, Calgary, Alberta, Canada, aitorichaso@hotmail.com 

Our understanding of tidally transported and deposited mud has been reshaped over the 

last two decades. It is now recognized that not all mud deposition is by passive settling; indeed, 

mud can accumulate under dynamic conditions where current velocities are above the threshold 

of mud erosion, provided there are high-density (i.e., > 1 g/L) near-bed mud suspensions (Baas et 

al., 2009, 2011; Schieber and Southard, 2009). Such high-density suspensions, and especially 

fluid mud (> 10 g/L), are now known to occur in many different tidal environments, and may even 

be an indicator of significant tidal action. Ichaso and Dalrymple (2009) have provided general 

criteria for identifying fluid-mud deposits in the rock record. Using core from the Tilje Formation, 

an Early Jurassic, mixed-energy (tide- and river-influenced) deltaic succession, thick (up to 15 

cm), slack-water mud layers at the base of tidal-fluvial channels and in mouth-bar deposits have 

been interpreted as the product of fluid muds deposited during tidal slack-water periods. It was 

assumed that they accumulated by passive settling, but is now known that generally similar, thick 

mudstone layers can accumulate dynamically (Mackay and Dalrymple, 2011). Therefore, we 

have undertaken a more detailed investigation of the Tilje fluid-mud layers using thin sections, to 

determine whether they too were deposited by dynamic processes. This study reveals the 

presence of three main mudstone “facies” within the fluid-mud layers. 

UNSTRATIFIED MUDSTONE (UM) 

This facies consists of thick claystone and siltstone laminae (5-10 mm thick) and beds (> 

10mm thick) that do not contain any internal laminations. They are interpreted to have formed 

during periods of moderate (1-10 g/L) to high (>10 g/L) SSC levels where near-bed turbulence is 

completely suppressed by a “plug” (a strong cohesive network of clay floccules) (Mackay and 

Dalrymple, 2011). The lack of internal lamination is accounted for by the lack of turbulence, 

which is required as a sorting mechanism. This facies was classified as a fluid mud by Ichaso 

and Dalrymple (2009). Two sub-facies are recognized. 

1) Without floating sand grains 

2) With floating sand grains 

The presence or absence of floating sand grains in a plug depends on the cohesive 

strength of the suspension. Baas et al. (2011) noted that the critical value occurred at SSC levels 

from ~315 g/L to 430 g/L: at values below this, the sand grains sink to the bottom, whereas, from 

these values and above, the sand grains cannot sink. In some cases the dispersed sand grains 

may appear to be graded; however, this is due to differential ability to sink through the suspension 

and is not due to turbulent sorting. 

CROSS-LAMINATED MUDSTONE (CLM) 

These mudstone layers contain small-scale cross lamination as a result of bedload 

transport of material. Moderate (1-10 g/L) SSC levels were shown to deposit mud dynamically in 

flume studies by Schieber and Southard (2009), where mud flocs can be transported in bedload 

and deposited as floccule ripples. Two varieties exist. 

1) Mud Ripple Laminations: This cross laminations consists solely of fine to very fine silt 

and clay, and occurs in small low-angle sets (3-5 mm thick). They are thought to be formed by 

floccule ripples and have been flattened due to the high degree of compaction. 

2) Mixed Grain-size Ripple Laminations: In systems where silt and fine sand are able to be 

transported in bedload together with flocculated mud, mixed grain-size laminations may form. 

Typically these sets are thicker and are more easily recognizable in thin-section than floccule 

ripples. 

PLANAR-LAMINATED MUDSTONE (PLM) 

Planar-laminated mudstones are common in the Tilje Formation, and many intervals 

interpreted by Ichaso and Dalrymple (2009) as unstratified are indeed laminated when observed 

in thin section. Many physical mechanisms have been proposed for the formation of these 

complex laminations. Two sub-facies have been created. 

105


1) Continuous Lamination: Non-bioturbated alternating laminae of clay and silt were 

interpreted by Mackay and Dalrymple (2011) to have formed underneath a plug in a flow with high 

SSC levels and mixed turbulent and laminar forces. Many of their examples underlay unstratified 

mudstone (UM); however, the Tilje Formation does not always display this pattern. Therefore, if 

continuous laminations occur below an UM, they likely formed at high SSC levels, but if there is 

no overlying UM, it is possible that the continuous laminations formed in a flow with lower SSC 

levels. 

2) Non-continuous Lamination (Grain Clusters): Non-continuous laminations occur as 

several millimeters-long sand/silt clusters that are capped with clay. Many of these clusters 

appear to have accumulated in a similar manner to pebble clusters in gravel rivers. This indicates 

that turbulence must have been present at the bed and they, thus, are likely to have accumulated 

at lower SSC levels. Some examples of this feature appear to indicate current direction because 

of grain imbrication. 

Cyclic variations in flow strength and SSC levels are recorded within some mudstone layers 

by vertical changes in the facies. Figure 1, a sample deposited in a tidal channel in the Tilje Fm., 

has been interpreted to contain a complete tidal cycle. 

Baas, J.H., Best, J.L., Peakall, J., and Wang, M., 2009, A phase diagram for turbulent, transitional, and 

laminar clay suspension flows: Journal of Sedimentary Research, v. 79, p. 162–183. 

Baas, J.H., Best, J.L., and Peakall, J., 2011, Depositional processes, bedform development and hybrid bed 

formation in rapidly decelerated cohesive (mud–sand) sediment flows: Sedimentology. doi: 

10.1111/j.1365-3091.2011.01247.x. 

Ichaso, A.A., and Dalrymple, R.W., 2009, Tide- and wave-generated fluid mud deposits in the Tilje 

Formation (Jurassic), offshore Norway: Geology, v. 37, p. 539–542. 

Mackay, D.A., and Dalrymple, R.W., 2011, Dynamic mud deposition in a tidal environment: the record of 

fluid-mud deposition in the Cretaceous Bluesky Formation, Alberta, Canada: Jour. Sed. Res., v. 81, p. 

901-920. 

Schieber, J., and Southard, J.B., 2009, Bedload transport of mud by floccule ripples-direct observation of 

ripple migration processes and their implications: Geology, v. 37, p. 483–486. 

106


OFFSHORE TIDAL BIOCLASTIC BODIES IN EPEIRIC SEAS: MIOCENE EXAMPLES 

FROM SE FRANCE AND CORSICA 

Jean-Yves REYNAUD*, Jean-Loup RUBINO**, Olivier PARIZE***, Robert W. DALRYMPLE****, 

Emmanuelle VENNIN*****, Michelle FERRANDINI******, Jean FERRANDINI******, Jean-Pierre 

ANDRE*******, Bernadette TESSIER********, Noel JAMES**** 

*MUSEUM NATIONAL D'HISTOIRE NATURELLE, Dht-43 rue Buffon, 75005, Paris, France, jyr@mnhn.fr 


***AREVA NC, 1 Place Jean Millier, 92084, Paris la Défense, France 

****QUEEN'S UNIVERSITY, Dept Geological Sciences, ONK7L3N6, Kingston Otario, Canada 

*****UNIVERSITE DE DIJON, 6 Boulevard Gabriel, 21000, Dijon, France 

******UNIVERSITE DE CORSE, Bp52, 20250, Santa-Lucia-Di-mercurio, France 

*******UNIVERSITE D'ANGERS, 2 bd Lavoisier, 49000, Angers, France 

********UMR CNRS 6143 M2C, UNIVERSITE DE CAEN, 24 Rue des Tilleuls, 14000, Caen, France 

In the Lower and Middle Miocene, the northern part of the Western Mediterranean and most 

of the western perialpine foreland basins experienced strong tides, which were locally enhanced 

where the tidal flows were entrenched in narrow seaways or straits. The resulting deposits are 

mixed siliciclastic to dominantly bioclastic crossbedded successions, several tens of meters thick 

and about several kilometers in extent which where formed by the stacking of subtidal dunes. In 

France these rocks are famous since the Romans used them to build the roman bridge over the 

Gard River (photo). Although most of the bioclastic grains in each unit were derived from the 

same heterozoan carbonate factory (dominated by bryozoans to coralline algae), they were 

sorted by tidal currents and residual faunal assemblages depict vertical and lateral trends that can 

be interpreted in terms of current strength, proximal-distal relationships and high-frequency 

sea-level changes. 

These tidal deposits are mostly comprised within TSTs but also locally in FRSTs. The 

historical stratotype of the Burdigalian in the foreland basin of SE France is an overall 

transgressive stack of high frequency sequences of crossbedded calcarenites, which have been 

interpreted as tidal bars and channel-fills (Lesueur et al., 1990). In the Vénasque valley, the tidal 

deposits are confined within the walls of the valley, and topped by storm-influenced marls that 

overlap the valley interfluves (Besson et al., 2005). This points to the dominant control of tidal flow 

constriction on the localization of the tidal deposits. Similarly, tidal deposits are emplaced as a 

flood-tidal delta at the outlet of the Uzès-Castillon valley into Uzès Basin (Reynaud et al., 2006). 

This is explained as the consequence of tidal flow expansion into the basin. The tidal inlet is 

plugged by very large tidal dunes. 

In the Sommières Basin, which had the same paleogeography as Uzès Basin, storm 

influenced deposits are found at the base of the TST below the tidal dunes. This shows, in 

addition to the dominant role of constriction or expansion of tidal flows, a local control by relative 

sea-level. The tidal climax was, in that case, the time of maximum tidal prism in the course of 

sea-level rise. At larger scales, tectonics also controlled the non-tidal to tidal switch of offshore 

dynamics in those basins. In the Bonifacio Basin (André et al., 2011; Reynaud et al., 2012), an 

agradational tide-dominated sand sheet composed of dunes replaced a wave-dominated ramp 

after the strait separating Corsica and Sardinia abruptly deepened, at the end of the opening of 

the Western Mediterranean. 

107


The roman bridge over the Gard River is made up of Miocene tidal calcarenites, extracted from a 

paleovalley incised in the Lower Cretaceous platform carbonates (which form the bedrock outcropping on 

this picture). 

André J.-P., Barthet Y., Ferrandini M., Ferrandini J., Reynaud J.-Y. & Tessier B. (2011) The Bonifacio 

Formation (Miocene of Corsica): Transition from a wave- to tide-dominated coastal system in mixed 

carbonate-siliciclastic sediments. Bull. Soc. Geol. Fr., 182, 225-234 

Besson D., Parize O., Rubino J.-L., Aguilar J.-P., Aubry M.-P., Beaudoin B., Berggren W.A., Clauzon G., 

Crumeyrolle P., Dexcoté Y., Fiet N., Iaccarino S., Jimenez-Moreno G., Laporte-Galaa C., Michaux J., von 

Salis K., Suc J.-P., Reynaud J.-Y. & Wernli R. (2005) Un réseau fluviatile d’âge Burdigalien terminal dans le 

Sud-Est de la France : remplissage, extension, âge, implications.- C.R. Géoscience, 337, 1045-1054. 

Lesueur J.-L., Rubino J.-L. & Giraudmaillet M. (1990) Organisation et structures internes des dépots tidaux 

du Miocène rhodanien. Bull. Soc. Geol. Fr., 6, 49-65. 

Reynaud J.-Y., Dalrymple R.W, Vennin E., Parize O., Besson D. & Rubino J.-L. (2006) Topographic 

controls on producing and depositing tidal cool-water carbonates, Uzès basin, SE France. J. Sed. Res., 76, 

117-130. 

Reynaud J.-Y., Ferrandini M., Ferrandini J., Santiago M., Thinon I., André J.-P., Barthet Y., Guennoc P. & 

Tessier B. (2012) From non-tidal shelf to tide-dominated seaway: the Miocene Bonifacio Basin, southern 

Corsica. Sedimentology, in press. 

108


COMPOUND TIDAL DUNES IN THE NEUQUEN JURASSIC RIFT BASIN 

Valentina ROSSI, Ronald STEEL, Cornel OLARIU, Julio LEVA LOPEZ 

JACKSON SCHOOL OF GEOSCIENCE, UNIVERSITY OF TEXAS AT AUSTIN, 1 University Station 

C9000, 78712, Austin, Usa, valentina.marzia.rossi@utexas.edu, RSteel@jsg.utexas.edu, 

cornelo@jsg.utexas.edu, julioleva@utexas.edu 

As part of a larger collaborative project revisiting the origin of the 500 m-thick, Bajocian 

Lajas Formation in the Neuquén Basin of Argentina, the present work reports on the distal delta 

front to shelf portion of the lower Lajas Formation, exposed in a 6 Km long outcrop belt at Lohan 

Mahuida. 

The studied unit is characterized by stacked, cross-stratified sandbodies and is sand-rich 

with relatively thin intervening mudstones. 

Detailed stratigraphic sections, linked to high resolution photo-mosaics, provide correlation 

and definition of the architecture of the sedimentary bodies. Three sandstone bodies (Fig. 1) 

have been selected for detailed study and 3D photos and LIDAR data have been acquired. These 

cross-stratified bodies have average thickness of 3, 5.5 and 15 m respectively; they are generally 

capped by heterolithic, thinly laminated facies , which can pass upwards to storm-wave 

generated sandstones or fine-grained sediments. 

Hundreds of paleocurrent indicators have been collected to determine the accretion style of 

these bodies (forward versus lateral accretion) in order to discriminate between compound tidal 

dunes and tidal sand ridges. To accomplish this, a hierarchy of inclined surfaces have been 

discriminated within the sandbodies (Fig. 2a and 2b): first order master surfaces or downlap 

surfaces, second order foreset surfaces of large dunes and third order foresets of small dunes 

within the larger ones. If the growth style of the sandbody is lateral accretion, the angle between 

master surfaces and second/third order surfaces would be significant, and usually greater than 

60°. In the selected sandbodies there was little deviation between the dip azimuth of the master 

surfaces and the two sets of dunes, indicating that the sandbodies are compound dunes (Fig. 3). 

The bodies are therefore likely to be elongate perpendicular to the main tidal current direction 

rather than parallel to it. 

The analyzed succession is mainly unidirectional, with very few indicators of bidirectionality. 

This characteristic can possibly be explained in a shelfal environment, where the tidal currents 

are mainly rotary. An alternative explanation is that flood tidal currents, just seaward of the deltas, 

dominated. 

109


110


MONSOON-CONTROLLED DELTAIC SEDIMENTATION IN A TIDE-DOMINATED 

SETTING: EXAMPLES FROM MEGA-DELTAS IN ASIA 

Yoshiki SAITO 

GSJ/AIST, Higashi, 305-8567, Tsukuba, Japan, yoshiki.saito@aist.go.jp 

Sediment discharge from rivers to the ocean and sediment dispersal in coastal zones in 

Asia are mainly controlled by the monsoon. The monsoon climate is characterized by a rainy 

summer with prevailing south winds and a dry winter with strong north winds in Asia. More than 

70–80% of annual sediment discharge occurs in summer, and re-suspension of sediment in the 

coastal zone by waves is dominant in winter. These characters are well recognized in the Yellow 

River Delta, Yangtze River Delta and Mekong River Delta. Here I review recent studies on these 

deltas and show an example of seasonal changes of sediment delivery and dispersal in a 

tide-dominated setting from the Mekong River Delta in Vietnam. 

The Mekong River Delta in Vietnam and Cambodia is one of largest deltas in the world with 

a delta plain that is about 300 km wide plain in a wave-tide dominated setting (mesotidal). 

Repeated surveys between November 2005 and March 2012 along shore-normal beach transects 

have shown that muddy sediment delivery occurs in summer, resulting in thick mud distribution on 

upper parts of the delta-front platform at the river mouth and a slightly muddier beach. During 

summer, the wave direction is relatively weak southwesterly. However, mud and very fine sand in 

the surface sediments tend to be removed during winter, suggesting that the sediment supplied 

from the river during summer is temporarily deposited near the river mouth and later transported 

southwestward during the winter monsoon. This feature coincides with the long-term sediment 

distribution and strata formation of the Mekong River Delta. 

111


Location and geomorphology of the Mekong River Delta with Optically stimulated luminescence (OSL) and 

radiocarbon ages (After Tamura et al., 2012) 

A: Location of Mekong River delta. Locations of sediment drill cores reported by previous studies are 

shown. B: Geomorphology of Mekong River delta (simplified from Nguyen et al., 2000; Tamura et al., 2010) 

and bathymetry of coastal sea relative to mean sea level (Ta et al., 2005). Beach ridges were redefined 

using Landsat image taken in 1989. Delta-front platform extends from shoreline to 4-m-deep isobath, 

offshore of which is delta-front slope. Delta-front slope grades offshore into prodelta and shelf at water 

depth of 18–20 m. Optically stimulated luminescence (OSL) and radiocarbon ages are expressed relative to 

A.D. 2010. 

Nguyen, V.L., Ta, T.K.O., and Tateishi, M., 2000. Late Holocene depositional environments and coastal 

evolution of the Mekong River Delta, southern Vietnam. Journal of Asian Earth Sciences, vol. 18, pp. 

427–439, doi:10.1016/S1367-9120(99)00076-0. 

Ta, T.K.O., Nguyen, V.L., Tateishi, M., Kobayashi, I., and Saito, Y., 2005. Holocene delta evolution and 

depositional models of the Mekong River delta, southern Vietnam, in Giosan, L., and Bhattacharya, J.P., 

eds., River deltas—Concepts, models, and examples: Society for Sedimentary Geology Special Publication 

83, pp. 453–466. 

Tamura, T., Horaguchi, K., Saito, Y., Nguyen, V.L., Tateishi, M., Ta, T.K.O., Nanayama, F., and Watanabe, 

K., 2010. Monsoon-influenced variations in morphology and sediment of a mesotidal beach on the Mekong 

River delta coast: Geomorphology, vol. 116, pp. 11–23, doi:10.1016/j.geomorph.2009.10.003. 

Tamura, T., Saito, Y., Nguyen, V.L., Ta, T.K.O., Bateman, M.D., Matsumoto, D., Yamashita, S., 2012. 

Origin and evolution of inter-distributary delta plains, insights from Mekong River delta. Geology, vol. 40, 

no. 4, pp. 303–306, doi:10.1130/G32717.1 

112


MEANDERING TIDAL CHANNEL DEPOSITS IN THE FLUVIAL-TIDAL TRANSITION 

OF A MIOCENE ESTUARY IN PATAGONIA 

Roberto SCASSO*, José Ignacio CUITIÑO*, Teresa DOZO**, Pablo BOUZA** 

*DEPARTMENT OF GEOLOGICAL SCIENCES, Intendente Guiraldes 2160, Ciudad Universitaria,, 

C1428EHA, Pabelón ii, Argentina, rscasso@gl.fcen.uba.ar, joseignacio@gl.fcen.uba.ar 

**CENPAT, CONICET, Boulevard Brown 2915, U9120ACD, Puerto Madryn, Argentina, 

dozo@cenpat.edu.ar, bouza@cenpat.edu.ar 

La Pastosa beds constitute a nice example of sediments deposited in the highly 

meandering reach of the of fluvial-tidal transition (Dalrymple and Choi, 2007; van den Berg et al., 

2007) within an estuary developed at the top of the “Rionegrense”, a marine-estuarine sequence 

of Late Miocene age in northeast Patagonia (Scasso and del Río, 1987; Scasso et al., 2001; 

Dozo et al., 2010). Sedimentary facies like channel lags rich in rip-up boulders and mud 

intraclasts, cross-bedded sands with mud drapes and “set-climber” ripples, inclined (HIS)and 

horizontal heterolithic stratification, herringbone bedding and tidal rhythmites, together with 

paucity of bioturbation and marine fossils, indicate that sedimentation took place in tidal channels 

subjected to strong tidal influence bounded by deposits formed in transgressive conditions at the 

base and at the top of the succession (Figure 1). 

Channel lag intraformational conglomerates are product of collapse of the cutbank due to 

erosion in the active margin of meandering channels. Cross-bedded sands accumulate in deeper 

parts of the channel and IHS formed in point bars. Discontinuities at the base of the channels and 

at the base of large IHS sets are the result of the migration of the whole channel-system and 

seasonally increased run-off and widening of the channel, respectively. Thick mud drapes and 

mud pebbles point to high suspended-sediment concentration and subsequent erosion by peak 

currents. Mud pebbles and blocks were also formed by lateral migration of the channels that 

eroded adjacent muddy tidal flats and salt marshes. 

Alternation of sand-rich and muddy IHS suggests periodical changes in the position of the 

turbidity maximum due to seasonal variation of fluvial discharge, in good agreement with the 

seasonal climate in Patagonia during the Late Miocene. Heterolithic bedding preserves 

neap-spring tidal cycles interrupted by periods of erosion occurred during spring tides or 

increases in the fluvial discharge, and no sand deposition occurred during neap tides. IHS sets 

dipping in N-S opposite directions indicate recurrent migration of high sinuosity channels in the 

tightly meandering reach. 

Grain size analyses of successive sand-mud layers in heterolithic bedding allow distinction 

of a part of a tidal cycle. Layers of current-ripple laminated sands with bipolar palaeocurrents 

directions show a consistent asymmetry in mean grain size, with coarser grained west (flood) 

oriented layers and finer grained east (ebb) oriented ones. The east oriented layers tend to 

disappear during neap tides. 

Repeated lateral migration of meandering channels caused erosion of the adjacent 

freshwater, low-energy restricted environments, including a well preserved vertebrate fauna 

concentrated in channel lags after short transport. 

Dalrymple, R.W., Choi, K., 2007. Morphologic and facies trends through the fluvial–marine transition in 

tide-dominated depositional systems: A schematic framework for environmental and sequence-stratigraphic 

interpretation. Earth-Science Reviews 81, 135–174. 

Dozo, M.T., Bouza, P., Monti, A., Palazzesi, L., Barreda, V., Massaferro, G., Scasso, R.A, Tambussi, C., 

2010. Late Miocene continental biota in Northeastern Patagonia (Península Valdés, Chubut, Argentina). 

Palaeogeography, Palaeoclimatology, Palaeoecology, 297: 100-106. 

Scasso, R., del Río, C.J., 1987. Ambientes de sedimentación y proveniencia de la secuencia marina del 

Terciario Superior de la región de Península Valdés. Revista de la Asociación Geológica Argentina 42 

(3/4), 291–321. 

Scasso, R., McArthur, J.M., del Río, C., Martínez, S., Thirlwall, M.F., 2001. 87Sr/86Sr Late Miocene age of 

fossil molluscs in the “Entrerriense” of the Valdés Peninsula (Chubut, Argentina). Journal of South 

American Earth Sciences 14, 319–329. 

van den Berg, J.H., Boersma, J.R., van Gelder, A., 2007. Diagnostic sedimentary structures of the 

fluvial-tidal transition zone – Evidence from deposits of the Rhine and Meuse. Netherlands Journal of 

Geosciences — Geologie en Mijnbouw, 86: 287 – 306. 

113


114


THE VARIATION OF THE SEDIMENTARY FACIES ON JADEBUSEN TIDAL BASIN IN 

GERMANY: SURFACE SEDIMENTS AND SEDIMENTARY STRUCTURES 

Chang Soo SON*, Alexander BARTHOLOMAE**, Burghard W. FLEMMING**, Seong Soo 

CHUN*, In Tae LEE*** 

*CHONNAM NATIONAL UNIVERSITY, 77 Yongbong-Ro, Buk-Gu, 500-757, Gwangju, Korea, 

senlab@hanmail.net 

**SENCKENBERG, Suedstrand 40, 26382, Wilhelmshaven, Germany 

***RESEARCH INSTITUTE FOR COASTAL ENVIRONMENT AND FISHERY-POLICY, 77 Yongbong-Ro, 

Buk-Gu, 500-757, Gwangju, Korea, itlee63@hanmail.net 

The study area is located at northwestern Germany. It is a broad inlet of the North Sea that 

covers an area of 190 km2. This area is characterized by semi-diurnal tides and the mean tidal 

range is around 3.8 m. The prevailing wind direction is from west-southwest. The discharge of the 

River can be negligible due to the small amount of water. 

For this study, 80 samples of surface sediments and 38 box- and pipe-cores were collected 

along four transects (Fig. 1). 

In general, the distribution pattern of surface sediments in this area is shown in Fig. 1. First 

of all, sand facies are predominant in the eastern area (transect 1) except for the nearby 

shoreline, whereas sand contents tend to decrease dramatically from the vicinity of the main 

channel to the landward direction in the southern and southwestern areas (transect 2 and 3). In 

the western area, on the other hand, the mud contents are high on average regardless of 

sampling positions (transect 4). 

In the case of sedimentary structures, cross-laminated sand, bioturbated sand and 

alternated sand/mud beds are prominent in the sand dominant areas, whereas homogeneous 

mud and bioturbated mud are predominant in the muddy area. In addition, the southwestern and 

western areas (transect 3 and 4) are characterized by the presence of coarse sand to gravel bed 

and shell bed except for the close to the shoreline. 

115


The distribution pattern of surface sediments on Jadebusen tidal basin. 

116


DO STROMATOLITES NEED TIDES TO TRAP OOIDS? INSIGHTS FROM THE 

COASTAL-LAKE CARBONATES OF THE LEZA FM (EARLY CRETACEOUS, N 

SPAIN) 

Pablo SUAREZ-GONZALEZ, I. Emma QUIJADA, M. Isabel BENITO, Ramón MAS 

DPTO. ESTRATIGRAFIA, FACULTAD DE CIENCIAS GEOLOGICAS, UNIVERSIDAD COMPLUTENSE 

DE MADRID - IGEO (CSIC-UCM), José Antonio Nováis 12., 28040, Madrid, Spain, 

pablosuarez@geo.ucm.es 

Stromatolites associated with ooid grainstones are often described in the literature, both in 

marine and fresh-water environments. However, lateral relationship between them does not 

necessary entail that ooids are trapped within the stromatolites. Interestingly, stromatolites that 

trap ooids are quite rare. The Cretaceous Leza Fm (Barremian-Aptian in age, Cameros Basin, N. 

Spain) offers an exceptional opportunity to elucidate the factors controlling grain trapping. The 

Leza Fm carbonates were deposited in coastal-lakes with several interrelated sedimentary 

environments, including fresh-water facies and facies with clear marine influence, and it contains 

two stromatolite types associated with ooids: one type traps grains (agglutinated oolitic 

stromatolites) and the other (skeletal stromatolites) does not. 

Agglutinated oolitic stromatolites of the Leza Fm (Fig. 1A) occur at the top of rippled ooid 

grainstone deposits, up to 1 m thick. Ooid grainstones are composed of ooids, peloids, intraclasts 

and bioclasts (ostracodes and foraminifera) and they show cm-scale lenticular, wavy and flaser 

bedding (Fig. 1C-D), which resemble some of the typical structures of peritidal carbonates. The 

agglutinated oolitic stromatolites are composed of alternating oolitic layers (formed by trapping of 

ooids by microbial mats) and clotted-peloidal micritic layers (formed by microbially-induced 

carbonate precipitation) (Fig. 1B). Small calcified filaments, relicts of mat microbes, are very rare. 

These stromatolites are one of the oldest examples of agglutinated carbonate stromatolites and 

their oolitic layers are similar to those of present-day popular examples of Bahamas and Shark 

Bay (Australia) (Reid et al., 1995). Nevertheless, the present-day agglutinated oolitic stromatolites 

are formed mainly by one accretion mechanism (trapping of ooids) with hiatuses marked by thin 

micritic crusts, but they do not significantly accrete by precipitating microbially-induced 

clotted-peloidal or filamentous carbonate. The conditions for effectively trapping ooids in these 

recent examples are soft and partially uncalcified surface mats, explained by the low carbonate 

saturation state of the waters (Riding, 2011), and grains supply, explained by the movement of 

ooids over the stromatolites due to tidal currents (Dill et al., 1986). Shallow marine settings, 

generally showing tidal influence, have been proposed for the rare ancient examples of these 

stromatolites (Riding et al., 1991; Matyskiewicz et al., 2006; Arenas & Pomar, 2010). 

Skeletal stromatolites of the Leza Fm (Fig. 1E) occur in fresh-water lacustrine facies, where 

they are laterally related with sandstones and grainstones of intraclasts, oncoids, ooids and 

bioclasts (ostracodes and charophytes). The dominant microfabric of these examples is long and 

strongly calcified microbial filaments with no trapped grains (Fig. 1F), thus their main accretion 

mechanism is active microbial mat calcification. Several examples of skeletal stromatolites and 

other stromatolite types are associated with ooid grainstones in ancient lacustrine sequences 

(e.g. Cole & Picard, 1978; Paul & Peryt, 2000), but, to our knowledge, none of them have trapped 

ooids in their microfabrics. 

The textural differences between the Leza Fm tidal-influenced agglutinated oolitic 

stromatolites (with soft and poorly calcified mats that trapped grains, Figs. 1A-B) and fresh-water 

skeletal stromatolites (with hard and strongly calcified mats that did not trap grains, Figs. 1E-F), 

suggests that water chemistry and hydrodynamics during their formation were different. 

Carbonate saturation state of marine water might have been low enough to prevent intense 

microbial calcification in the tidal-influenced coastal-lakes, producing soft mats that trapped 

grains. In addition, the cyclic hydrodynamic changes produced by tides allowed periodic supply of 

grains to be trapped by the soft mats, producing agglutinated ooid stromatolites. In contrast, the 

higher carbonate saturation of meteoric waters, which came from the Jurassic carbonate 

substrate of the Cameros Basin, as well as the lower hydrodynamic changes of lacustrine 

environments, probably lead to the stronger mat calcification of skeletal stromatolites of the Leza 

Fm and the absence of trapped grains. 

Furthermore, input of meteoric water in the tidal-influenced coastal-lakes of the Leza Fm 

would explain the differences between the present-day agglutinated oolitic stromatolites (formed 

mainly by trapping), and the Leza agglutinated examples (formed by alternation of trapping and 

mat calcification). 

To conclude, we propose that water chemistry and hydrodynamics of tidal-influenced 

environments are very suitable for the development of agglutinated carbonate stromatolites, 

117


explaining why these stromatolites are almost restricted to tidal environments at the present-day 

and in the geological record. 

Field (A, C, D, E) and microscope (B, F) images of the Leza Fm stromatolites and associated facies. See 

text for descriptions. 

Arenas, C. & Pomar, L. (2010) Palaeog., Palaeocl., Palaeoec., 297, 465-485. 

Cole, R. & Picard, M. (1978) Geological Society of America Bulletin, 89, 1441-1454. 

Dill, R.F.; Shinn, E.A.; Jones, A.T.; Kelly, K. & Steinen, R.P. (1986) Nature, 324, 55-58. 

Matyszkiewicz, J.; Krajewski, M. and Kedzierski, J. (2006) Facies, 52, 249-263. 

Paul, J. & Peryt, T.M. (2000) Palaeog., Palaeocl., Palaeoec., 161, 435-458. 

Reid, P.; Macintyre, I.; Browne, K.; Steneck, R. & Miller, T. (1995) Facies, 33, 1-18. 

Riding, R. (2011) In: Reitner & Thiel (eds.), Encyclopedia of Geobiology, 635-654. 

Riding, R.; Braga, J.C. & Martín, J.M. (1991) Sedimentary Geology, 71, 121-127. 

118


COASTAL MONITORING USING L-BAND SYNTHETIC APERTURE RADAR (SAR) 

IMAGE DATA IN THE MEKONG AND HUANGHE (YELLOW RIVER) DELTA AREAS 

Akiko TANAKA 

GSJ/AIST, Higashi, 305-8567, Tsukuba, Japan, akiko-tanaka@aist.go.jp 

Coastal geomorphology is highly variable as it is affected by sea-level changes and other 

naturally- and human-induced fluctuations. To effectively assess and monitor geomorphological 

changes in various time scales is thus critical for coastal management. Asian mega deltas are 

vulnerable to a sea-level rise due to its low-lying delta plain, and are dynamic region given a large 

amount of sediment supply. However, limited data availability and accessibility in the deltas have 

prevented establishment of systematic coastal monitoring. A variety of remote sensing systems 

can be used to monitor geomorphological changes in coastal areas as it has wide spatial 

coverage and high temporal repeatability. Especially, analysis using SAR (Synthetic Aperture 

Radar) data not affected by the cloud conditions offer potential for monitoring in the monsoon 

Asia region. In this paper, I present that L-band SAR data are useful for monitoring coastal areas 

on a regional scale. I present two examples: ALOS (Advanced Land Observing Satellite) PALSAR 

(Phased Array type L-band SAR) data for the Mekong Delta area, and JERS-1 (Japanese Earth 

Resource Satellite-1) SAR data for the Huanghe (Yellow River) Delta Areas. 

ALOS/PALSAR data acquired over a period from December 2006 to January 2011 are 

analyzed to investigate the relation between the sea level and the shape of mouthbars in the 

Mekong River (Figure 1 (b)). River mouthbars with strong backscatter, which is surrounded by the 

water with weak backscatter, are successfully extracted using a histogram thresholding algorithm. 

Estimated areas of river mouthbars, which are located openly faced to the South China Sea, 

gradually increase on an annual time scale (Figure 2). Besides this overall increasing trend, 

seasonal variations of areas are observed. 

A series of binary image of JERS-1 data demonstrates the ability to monitor tidal flat in the 

he Huanghe (Yellow River) Delta area quantitatively. Tidal flat area increased until 1995, and then 

eroded between 1995 and 1997. In May 1996, a new channel was cut near the tip of the delta, 

with the result that tidal flat area again increased. This area change is well correlated with annual 

water and sediment discharge at the Lijin Station, which is located about 100 km upstream from 

the entrance of the mouth channel and the lowest hydrological station on the river. A series of 

binary data also captures the seasonal changes in tidal flat area. 

To monitor the area changes over longer time intervals, further investigation combing data 

from another SAR and optical sensors is required. It will also be useful to apply to other regions to 

reach more comprehensive and comparable analysis. 

Acknowledgement: Ministry of Economy, Trade and Industry (METI) and Japan Aerospace 

eXploration Agency (JAXA) retains the ownership of the original JERS-1/SAR and 

ALOS/PALSAR data. This work is done in collaboration with Dr. Yoshiki Saito, Dr. Toru Tamura, 

Dr. Katsuto Uehara, Dr. Zuosheng Yang, Dr. Houjie Wang, Dr. Nguyen Van Lap, and Dr. Ta Thi 

Kim Oanho. 

119


(a) Location map of the study area, (b) the Mekong River Delta in Vietnam, and (c) the Huanghe (Yellow 

River) River Delta, in China. (b) Study area in the Mekong River Delta. Dashed boxes denote the 

approximate area coverage of the acquired ALOS/PALSAR images with path-frame numbers. White line 

boxes represent the target river mouthbars (RMs) used for area changes, superimposed on SAR intensity 

image. (c) Study area in the Huanghe (Yellow River) River Delta, facing the Bohai Sea. Gray represents 

land areas using SRTM 90 m digital elevation model data (Jarvis et al, 2008). Bold dashed and solid lines 

show coastline and river from GSHHS, which is a high-resolution shoreline data set amalgamated from two 

databases in the public domain (Wessel and Smith, 1996). Rectangle indicates the target area. The target 

area is located between the coastline and the low tide line. Figure 2 Temporal area changes in RM1 

(black), RM2 (blue), and RM3 (red) at the Mekong River Delta, with the linear least-square fit (dashed-line). 

Circles, squares, crosses, and triangles show data from ascending tracks, Path-Frame 4770-0190 and 

4770-0180, and descending tracks, Path-Frame, 110-3420 and 110-3430, respectively. Symbols with gray 

fill represent the area data without hourly tidal height data. 

120


SEDIMENTARY RECORDS OF CLIMATE CHANGES IN MACROTIDAL 

TIDE-DOMINATED ESTUARIES 

Bernadette TESSIER*, Isabelle BILLEAUD**, Philippe SORREL*** 


bernadette.tessier@unicaen.fr 

**TOTAL EXPLORATION & PRODUCTION, CSTJF, Avenue Larribau, 64018, Pau, France, 

isabelle.billeaud@total.com 

***UMR CNRS 5125 PEPS, UNIVERSITE CLAUDE BERNARD–LYON 1, 27-43 bd du 11 Novembre, 

69622, Other, France, philippe.sorrel@univ-lyon1.fr 

During the last few years, many studies dealing with the Holocene evolution of 

tide-dominated estuaries and embayments, pointed out the major role of rapid climate changes 

on the morphodynamics behaviour of such coastal systems (Chaumillon et al., 2010). Examples 

include the Holocene sedimentary infill of incised valleys along the Atlantic and English Channel 

coasts of France (Billeaud et al., 2009; Sorrel et al., 2009, Sorrel et al., 2010; Tessier et al., 

2011). 

The aim here is to propose a synthesis of the different features that can be ascribed to 

climate changes during the sedimentary infill of macrotidal tide-dominated estuaries and 

embayments (Figure). This synthesis is based mainly on the data collected in the 

Mont-Saint-Michel Bay (MSMB) and Seine estuary (SE) (NW France). The general context is that 

of the mid- to late Holocene (since 7000 y. BP) and associated slow sea-level rise (1-2 mm/y), 

and that of the ~1500 year-periodicity rapid climate changes of the North Atlantic domain (RCC, 

Mayewski et al., 2004; or Bond’s cold events, Bond et al., 1997) characterized by enhanced storm 

periods of a few hundred years. Available radiocarbon dating clearly demonstrates that the 

following features described are contemporaneous of these periods (Billeaud et al., 2009; Sorrel 

et al., 2009). 

Various depositional environments such as tidal flats and salt marshes, estuarine channels 

and bars characterize tide-dominated systems. In some areas, upper tidal flats and salt marshes 

develop in tidal “lagoons” sheltered behind wave-dominated coastal barriers that construct along 

the edges of the tide-dominated domain. 

Cores collected in the sandflats (MSMB), subtidal bottomsets of the estuarine bars (SE) and 

marginal tidal channel area (SE), display typical tide-dominated facies successions, including 

badly sorted muddy sands and well-preserved mud-drapes (tidal beddings). Coarse-grained 

shelly layers, decimetric in thickness, and with an erosive base, are regularly intercalated within 

these 5-6 m long successions. These layers that can be correlated at the scale of the whole 

studied system (a few km) are interpreted as the result of storm-induced processes, and 

associated with the periods of enhanced storminess. Tide-dominated successions that compose 

the infill of back-barrier tidal depressions (MSMB) display regular variations in grain-sizes; muddy 

and peaty facies are associated with a well-stabilized barrier, whereas, coarser sandy facies are 

related to a destabilized (or at least partly destroyed) barrier. In embayment (MSMB), when 

barriers are destroyed during the enhanced storm periods, the tidal prism suddenly increases due 

to the inundation of the salt marsh areas located behind the barriers. This phenomenon of 

enhanced tidal currents, due to enhanced storm activity, induces the formation of tidal creeks that 

incise deeply mud flat successions. In the offshore approaches of these tide-dominated 

environments (MSMB), subtidal sandbanks are composed of stacked tidal bodies, separated from 

each other by flat surfaces interpreted as the result of high energy erosional processes during the 

enhanced storm periods. 

The preservation of these different signatures demonstrates that climate changes should be 

considered as major factors of morphodynamic behaviour and long-term evolution of macrotidal 

tide-dominated coastal environments. However, no signature related to climate change has been 

found into the successions that characterize the main axis of the estuaries, where intense 

reworking constantly occurs under the action of powerful tidal currents. The cut-and-fill facies 

preserved at the base of the successions are probably good candidate that remains to explore for 

deciphering climate change impacts into these environments. More surely, since annual cycles 

are commonly preserved on the upper part of these successions (Tessier, 1998), impacts of very 

high frequency climate changes on macrotidal tide-dominated estuaries can be potentially 

studied. 

121


Schematic representation of the sedimentary features preserved in Holocene incised-valley infills recording 

the impacts of enhanced storminess periods (~1500 year-periodicity Rapid Climate Change – RCC) on 

macrotidal tide-dominated environments. Such features are preserved almost everywhere, except in the 

active estuary, where however very high frequency (VHF) climate variability can potentially be deciphered 

(black scale bar indicative: 1 m) 

BILLEAUD I., TESSIER B, LESUEUR. P (2009). – Impacts of Late Holocene rapid climate changes as 

recorded in a macrotidal coastal setting (Mont-Saint-Michel Bay, France). Geology, 37, 1031-1034. 

BOND G., SHOWERS W., CHESEBY M., LOTTI R., ALMASI P., DE MONECAL P., PRIORE P., CULLEN 

H., HAJDAS I., BONANI G. (1997). A pervasive millennial-scale cycle in north Atlantic Holocene and glacial 

climates, Science, vol. 278, pp. 1257-1266. 

CHAUMILLON E., TESSIER B. & REYNAUD J.-Y. (2010). Stratigraphic records and variability of incised 

valleys and estuaries along French coasts. Bull. Soc. géol. France, 181, 2, 75-86. 

MAYEWSK P.A., ROHLING E.E., STAGER J.C., KARLÈN W., MAASCH K.A., MEEKER L.D., MEYERSON 

E.A., GASSE F., VAN KREVELD S., HOLMGREN K., LEE-THORP J., ROSQVIST G., RACK F., 

STAUBWASSER M., SCHNEIDER R.R., STEIG E.J. (2004). Holocene climate variability, Quaternary 

Research, vol. 62, pp. 243-255. 

SORREL P., TESSIER B., DEMORY F., DELSINNE N., MOUAZÉ D. (2009). Evidence for millennial-scale 

climatic events in the sedimentary infilling of a macrotidal estuarine system, the Seine Estuary (NW 

France). Quaternary Science Reviews, 28, 499-516. 

SORREL P., TESSIER B., DEMORY F., BALTZER A., BOUAOUINA F., PROUST J.N., MENIER D., 

TRAINI C. (2010) Sedimentary archives of the French Atlantic coast (inner Bay of Vilaine, south Brittany): 

depositional history and late Holocene climatic signals. Continental Shelf Research 30, 1250-1266. 

TESSIER B., 1998. Tidal cycles: annual versus semi-lunar records. In: Tidalites: Processes and Products. 

Eds.: Alexander, C., Davis Jr., R.A. & Henry, V.J. SEPM Special Publication n°61, 69-74 

TESSIER B., BILLEAUD I., SORREL P., DELSINNE N. & LESUEUR P. (2011) Infilling stratigraphy of 

macrotidal tide-dominated estuaries. Sedimentary Geology. doi:10.1016/j.sedgeo.2011.02.003 

122


MARINE HABITAT CLASSIFICATION: A PLURIDISCIPLINARY APPROACH IN A 

HIGH MACROTIDAL ENVIRONMENT. THE CASE OF THE ENGLISH MEDIAN 

CHANNEL 

Alain TRENTESAUX*, Romain ABRAHAM*, Alexandrine BAFFREAU**, Jean-Claude DAUVIN**, 

Sophie LOZACH**, Deny MALENGROS*, Emmanuel POIZOT*** 

*UMR CNRS 8217 GEOSYSTEMES, University Lille 1, 59655, Villeneuve D'Ascq, France, 

alain.trentesaux@univ-lille1.fr, romain.abraham@univ-lille1.fr 

**UMR CNRS 6143 M2C, UNIVERSITE DE CAEN, 24 rue des Tilleuls, 14000, Caen, France, 

jean-claude.dauvin@unicaen.fr, sophie.lozach@unicaen.fr 

***GEOCEANO, Cnam/intechmer bp 324, 50110, Tourlaville, France, emmanuel.poizot@cnam.fr 

In megatidal sea, benthic marine communities are strongly dependent on the substrate, 

which is fashioned by hydrodynamism. This interdependence between substrate and benthic 

communities has enabled the establishment of marine benthic habitats classifications. Such 

classification allows depicting at the same time the general habitats diversity at the scale of a 

given shelf, and the local variations at the scale of a smaller area. Indeed, it meets diverse needs 

for ecological description of the marine environment such as general habitat knowledge or 

environmental impact assessment. The EUNIS classification is available to describe the main 

habitats of the European marine seabeds (Davies et al., 2004). Based on available data at the 

time of its delivery, it is well adapted to describe shallow bays and estuarine environments, mostly 

characterised by mobile muddy fine sediments. On the contrary it fails in describing correctly 

clean coarser sediments habitats in more deep areas such as those found in the central part of 

English Channel (La Manche) (Connor, 2005; James et al., 2007). This continental shelf sea 

connects with the Atlantic Ocean in its western part and to the Southern North Sea in its eastern 

part. It is characterised by a series of strong offshore-inshore and capes/bays gradients 

characterised by progressive changes in temperature, bathymetry, shear stress that are 

registered in the sediment, but also in the benthic communities. 

In the framework of the European INTERREG IVa CHARM III project, supplementary data 

were needed to increase knowledge in sublittoral coarse sediment habitats. To fulfil this objective 

and to re-assess EUNIS habitats types, the deepest (mid) part of the Western English Channel 

was prospected. Our study is a snapshot of the habitats diversity thanks to two VideoCHARM 

surveys in June 2010 and June 2011. We focussed on a longitudinal profile, from the western 

approach to the Greenwich meridian to stay in the deepest part of the English Channel (Figure 1). 

Nevertheless, no sediment was taken in the Hurd Deep, elongated depression in the median 

Channel. Conversely, near coastal deep zone was sampled along the Brittany coast to investigate 

an inshore/offshore gradient (Figure 1). This approach could be compared to that of Cabioch et 

al. (1977). One big difference is that, despite the high quality of their study, it was a combination 

of several surveys that were run during more than ten years in the 1960’ to the 1970’. 

VideoCHARM study is a synoptic work as sampling has been realised within two year and at the 

same season. A multidisciplinary approach was used to better precise the different habitats. Both 

indirect (Side scan sonar, ROV) and direct (Grab sampling with benthos determination, and 

grain-size analyses) approaches were used and combined. 

Different types of benthic habitats are defined. We observe a progressive change in the 

residual tidal current speed and a progressive change in the habitat structure from the Western 

Approaches to the East. The diversity is changing at the scale of a local study depending on the 

sediment type and the presence of pebbles or hard substrates, but also over the entire English 

Channel. The substrates and sediment characteristics vary a lot, also at diverse scales (Figure 2). 

These changes will be discussed and compared with physical data such as shear stress or 

seawater temperatures. 

123


Comparison of different visual description of the sediment, by grab sampling or by video. Grab samples 

show the variability is sediment type in a small area on the sea bed (each picture is from a different 

sampling site) and ROV images show heterogeneity of sedimentary profiles at the scale of one sampling 

station (all images are from the same video). The top frame and the bottom frame show observations within 

a same area, indicated on the map. 

Cabioch, L., Gentil, F., Glaçon, R., et Retière, C., 1977. Le macrobenthos des fonds meubles de la 

Manche: distribution générale et écologie. In : Biology of benthic organisms : 11th European symposium on 

marine biology, Galway, Ireland, 115-128. 

Connor, D.W., 2005. EUNIS marine habitat classification: application, testing and improvement. MESH, pp. 

16 

Davies C. E., Moss, D., et Hill, M.O., 2004. EUNIS habitat classification revised 2004. 307 pp 

James, J.W.C., Coggan, R.A., Blyth-Skyrme, V.J., Morando, A., Birchenough, S.N.R., Bee, E., Limpenny, 

D.S., Verling, E., Vanstaen, K., Pearce, B., Johnston, C.M., Rocks, K.F., Philpott, S. et Rees, H.L., 2007. 

The eastern English Channel map. Science Series Technical Report n°139, CEFAS, lowestoft, 191 pp. 

124


DEVELOPMENT OF A SEABED MODEL FOR ANALYZING SEDIMENT AND 

MORPHODYNAMIC PROCESSES IN THE GERMAN BIGHT (NORTH SEA) 

Jennifer VALERIUS*, Peter MILBRADT**, Michael VAN ZOEST**, Manfred ZEILER* 

*FEDERAL MARITIME AND HYDROGRAPHIC AGENCY, Bernhard-Nocht-str. 78, 20359, Hamburg, 

Germany, jennifer.valerius@bsh.de, manfred.zeiler@bsh.de 

**SMILE CONSULT GMBH, Vahrenwalder Straße 4, 30165, Hanover, Germany, milbradt@smileconsult.de, 

vanzoest@smileconsult.de 

Motivation 

An increase in human activities in shelf and coastal waters as well as rising sea level due to 

climate change reveals the need for better understanding nature and variability of the seabed. 

Especially the combination of marine geological field work and numeric modelling helps to 

improve our knowledge and prediction capabilities with respect to sediment and morphodynamic 

processes. 

The AufMod project funded by the Federal Ministry of Research and Education (BMBF) is 

focussing on this interdisciplinary approach to develop tools and models for analyzing the 

long-term morphodynamics in the German Bight (North Sea). 

One objective is to build up a Seabed Model based on bathymetric and sedimentologic 

datasets in space and time. The Seabed Model consists of a quasi-consistent and plausible 

geodatabase for bathymetric data and sedimentological parameters like grain size distributions, 

porosity, thickness of the mobile sediment (sand) layer and bedforms. 

This geodatabase may be used as (1) a source of input data for numeric modelling and (2) 

for data-based analyses of morphological changes and sedimentological variations. 

Methodology 

In the first stage of the project, point datasets available for the different parameters were 

collected and stored in a database system called Functional Seabed Model, which includes 

sophisticated interpolation and approximation methods for data-based modelling in time and 

space. In the second stage of the project data-based modelling was applied to regular or irregular 

grids in variable spatial resolution; confidence layers will be provided for each product. 

Results and Products 

The amount of data differs strongly among the parameters stored in the Functional Seabed 

Model. Nearshore bathymetric data are available in an acceptable to relatively high spatial 

resolution from 1948 until today. Beyond a water depth of 15 m, bathymetric data in time are 

scarce as well as sedimentological parameters. 

Based on these consistent bathymetric time series, morphological parameters like changes 

in depth (dz/dt) or „morphological space“ (zmax – zmin) can be derived or volumetric calculations 

can be performed. Figure 1 illustrates the morphological space for the coastal and nearshore 

waters of the German Bight. 

Statistical parameters were calculated for the German Bight based on consistent 

sedimentological datasets. Figure 2 shows the distribution of the median (D50) in the German 

Bight depicting areas of reworked (coarse) sediment (red colours) and areas of grain size 

fractionation (green colours). 

125


Fig. 1: Morphological Space (zmax - zmin) in the German Bight from the coastline to the 20m-isobath for a 

period of 15 years (1996 to 2011) on a 50m-raster. Fig. 2: Interpolated d50-value in the German Bight in 

half Phi intervals on an irregular grid. 

126


TIDAL ASYMMETRY: THE USE OF ARTIFICIAL RADIONUCLIDES IN SEDIMENTS 

(THE SEINE ESTUARY, FRANCE) 

Anne VREL*, Dominique BOUST**, Patrick LESUEUR*, Catherine COSSONNET***, Julien 

DELOFFRE****, Carole DUBRULLE-BRUNAUD*, Nicolas MASSEI****, Marianne ROZET**, Luc 

SOLIER**, Sandrine THOMAS*** 


anne.vrel@unicaen.fr, patrick.lesueur@unicaen.fr 

**IRSN - LABORATOIRE DE RADIOECOLOGIE DE CHERBOURG-OCTEVILLE, Rue max pol Fouchet, 

50130, Cherbourg, France 

***IRSN - LABORATOIRE DE MESURE DE LA RADIOACTIVITE DANS L’ENVIRONNEMENT, Bois des 

Rames, 91400, Orsay, France 

****UMR CNRS 6143 M2C, UNIVERSITE DE ROUEN , Place Emile Blondel, 76821, Mont Saint Aignan, 

France 

The Seine estuary is the outlet of the catchment area of the Paris Basin, where fine 

sediments and a number of anthropogenic elements and substances end in. Among them, 

artificial radionuclides can be used as tracers of sediment sources and mixing processes. They 

may originate from upstream (atmospheric fallout from Chernobyl accident in 1986 and from 

nuclear weapons testing in the 1960s, licensed discharges from nuclear facilities...) or from 

downstream (La Hague reprocessing plant –Central Channel). 

In this macrotidal estuary, trapping and upstream migration of sediment is in process, due to 

the tide asymmetry; it is named “tidal pumping”. It has been previously documented using 60Co, a 

short-lived radionuclide, originating from the La Hague reprocessing plant (north of Cotentin 

peninsula). The average upstream velocity of 60Co-labelled sediment particles has been 

estimated to be in the order of 10 km per year. The plutonium 239, 240 and the americium 241 

have much longer decay period and could, therefore, give the opportunity to better understand 

the dynamics of the “tidal pumping” on a longer term. 

Plutonium and americium profiles have been obtained in three sediment cores collected in 

various settings along the lower Seine: (1) a proximal fluvial floodplain upstream from the estuary 

(i.e. without any tidal influence); (2) an old sheltered dock in the upper estuary (under moderate 

tidal influence); (3) a mudflat at the mouth (under strong tide and wave forcings). The sediments 

cored were analysed and dated using historical data (bathymetric maps, flood time-series...), 

analysis of cesium 137, and signal processing techniques. 

The inputs of Pu- and Am-bearing particles are characterized by contrasting ratios (239, 

240Pu/241Am). At the most upstream (fluvial) cored site, the sediments are marked by the global 

fallout with a ratio about 2.5. In the upper estuary, a combined influence of upstream solid 

discharges with sediment particles coming from downstream (since 1975) is observed. The 

sediment pool coming from downstream, marked by discharges from La Hague reprocessing 

plant, is characterized by a much lower ratio about 1.0. The input signal of marine Pu- and 

Am-bearing particles is constrained by the Pu and Am data obtained in the sediments cored at 

the mouth of the estuary (Figure 1). 

Thanks to a simple mixing model, it is possible to quantify the percentage of radionuclides 

from upstream for each year and to obtain a time-series of the percentage of radionuclides in the 

upper estuary due to “tidal pumping”. The radionuclides downstream contribution in the upper 

estuary is low or nonexistent depending on the year (0 to 4%). The “tidal pumping” is dependent 

on a lot of parameters during several consecutive years: hydrological parameters and tidal 

parameters. Overall, “tidal pumping” is amplified when the flow is low and the tide energy is high 

during the 10 previous years. 

Artificial radionuclides are likely to be powerful tracers for the understanding of fine-grained 

sediment dynamics in macrotidal estuaries. Moreover, they lead to unique and valuable 

information on the dynamics of the “tidal pumping” over the last 20 years. 

127


Upstream and downstream inputs of artificial radionuclides in the Seine estuary 

Boust, D., Lesueur, P., Rozet, M., Solier, L., Ficht, A., 2002. The dynamics of Co- labelled sédiment 

particles in the Seine estuary. Radioprotection 37, 749-754. 

128


HYDROLOGIC CHARACTERISTICS OF THE YELLOW RIVER MOUTH, CHINA 

Dong WANG*, Shengli SONG*, Hao DING*, Jichun WU*, Qingping ZHU**, Ling WANG*** 

*SCHOOL OF EARTH SCIENCES AND ENGINEERING, Nanjing University, 210093, Nanjing, China, 

wangdong@nju.edu.cn 

**CHINA WATER INTERNATIONAL ENGINEERING CONSULTING CO, LTD., China Water International 

Engineering Consulting co, Ltd., 100010, Beijing, China 

***HYDROLOGY BUREAU , the Yellow River Conservancy Committee, 450000, Zhengzhou, China 

In recent years, the impact of climate change and human activities on the World‘s Large 

Rivers’ runoff is great, especially on that of the Yellow River. Using 1950-2003 runoff series from 

Lijin hydrologic station of the Yellow River Mouth as the case, the eigenvalues (maximum value, 

minimum value, mean value, skewness coefficient Cv ,Variation coefficient Cs , etc.) are 

calculated. And the main periods characteristics of monthly runoff series are ascertained by using 

WA (Wavelet Analysis) method. Then taking these eigenvalues and the main period’s 

characteristics of monthly runoff series as the input vector of the SOM (Self-Organizing Maps) 

method, a WA-SOM coupling model is established in this study. Thus the characteristics of 

monthly and annual runoff series of 2 spans (1950-1969 and 1970-2003 respectively) of the 

Yellow River Mouth are compared. Results show that: (1) After 1970s, the monthly and annual 

runoff series decreased significantly in the lower Yellow River. (2) The main periods 

characteristics of monthly runoff after 1970s became more complex than before 1970s. (3) After 

1970s, the change of runoff series in January and February is not obvious, but the changes of 

runoff series in the other months are significant. 

129


The continuous wavelet transform result of observed annual runoff series in Lijing station of the Yellow 

River (1-30a) 

130


SEDIMENT RESUSPENSION, FLOCCULATION AND SETTLING IN A MACROTIDAL 

ESTUARINE ENVIRONMENT 

Ya Ping WANG 

SCHOOL OF GEOGRAPHIC AND OCEANOGRAPHIC SCIENCES, 22 Hankou Road, 210093, Nanjing, 

China, ypwang@nju.edu.cn 

Flocculation, settling and resuspension play important roles on the cohesive sediment 

transport and biogeochemical processes in the estuarine environment. Results from in-situ 

measurements of hydrodynamics, sediment resuspension and sediment particle size distribution 

from both the bentic boundary layer and the whole water column are used to examine the 

sediment resuspension and sediment aggregation process in the Jiulong River estuary (China). 

Time-series from two experimental periods were phased averaged into typical neap and spring 

tidal cycles and the tidal variability of the processes is discussed. 

Near bed flow data were used to provide accurate estimates of bottom shear velocities and 

associated turbulence parameters. The law of the wall, Reynolds stress and the inertial 

dissipation methods were utilized. The latter two methods were found to be more reliable in this 

environment while the law of the wall failed to provide reliable estimates during slack water 

conditions. On the basis of these results a drag coefficient of approximately 4.2x10-3 was 

estimated to be valid in this area without a significant difference between ebb and flood stages. 

Sediment resuspension is higher during spring tides in response to higher velocities. During 

resuspension, flocullation processes were revealed. The primary particles identified through the 

analysis of dispersed sediment from water samples had a mean size of just under 10microns. 

Bottom sediments were found to be either unimodal with a mean size of approximately 200 

microns or bimodal with peaks corresponding to 200microns and to the mean size obtained from 

the water samples. In situ size distributions obtained using the LISST show a variable sediment 

size concentration in the water column that is influenced by flocculation processes. 

The size of the flocullates seems to be controlled by turbulence more than any other 

parameter, 

The flocculation exists widely during tidal cycles in the estuary, with in-situ mean size 

significantly coarser one order more than the primary size of sampling particles. In addition, the 

turbulence dissipation is found to be negative related to the floc size and positive related to the 

settling velocity, which controls the aggregation and deflocculation processes. The 95-percentile 

floc size, which was close to the maximum floc size, had a significant linear relationship with 

Kolmogorov microscale, while the former was 0.3-0.5 size of the later. It indicated that floc size 

variations are limited by the turbulent eddy evolution during a tidal cycle. Further, the high 

turbulence dissipation parameter, corresponding to high bottom shear velocities, is attributed to 

the entrainment and resuspension of bottom sediment with high densities into the water column 

and results in high effective density of SPM and high settling velocity. In addition, the high 

turbulence dissipation parameter is associated with small eddies and could destroy the macrofloc. 

Such a condition is present at the middle flood/ebb, especially during the spring stage. On the 

contrary, the sea water becomes strong stratification at low water level when the river discharge 

enhances and the low salinity or salt wedge dominated, and then the turbulence was suppressed 

with low dissipation. This induces large Kolmogorov microscale (or big eddy) and thus is 

advantage of macrofloc formation. 

131


Study area showing the tripod station 

132

EFFECTS OF GRAIN-SIZE SORTING ON THE SCALE-DEPENDENCES OF 

EQUILIBRIUM MORPHOLOGY OF BACKBARRIER TIDAL BASINS 

Yunwei WANG, Qian YU, Shu GAO 

MOE KEY LABORATORY OF COAST AND ISLAND DEVELOPMENT, 22 Hankou Road, Nanjing 

University, 210093, Nanjing, China, ms.ywwang@gmail.com 

Coastal tidal basins consist of two major morphological units: tidal channels and tidal flats. 

Based on field observations of the backbarrier tidal basins along the Dutch-German North Sea 

coast, some empirical relations were found between the morphological parameters and the basin 

scale: the dimensional parameters of channel area (Ac) and volume (Vc) are proportional to the 

1.5 power of the basin area (Ab) and tidal prism (P), respectively; and the dimensionless 

parameters of relative channel area (Ac/Ab) and the ratio of channel volume to tidal prism (Vc/P) 

are both proportional to the square root of basin area (Ab1/2). The coefficients in the power-law 

expressions are all in the order of 10-5. Furthermore, previous observations also indicated that, at 

equilibrium states, both volume and area hypsometries of back-barrier tidal flats are dependent 

on the basin scale. Large basins favour pronounced concave hypsometries, while small basins 

favour subdued concave ones. In this study, the scale-dependences of equilibrium morphology of 

the Dutch-German tidal basins are investigated by process-based modeling approaches on the 

basis of the Delft3D system with single and multi-grain-size fractions of sediments, so as to 

provide physical explanations for the scaling relations. The effects of grain-size sorting on the 

scale-dependences of equilibrium morphology are therefore emphasized through comparisons of 

the results from the single fraction modeling, multi-fraction modeling and observations. 

The model results suggest that both the single and multi-fraction modeling series show the 

same types of the power-law scaling relations as the empirical expressions derived from 

observations, and the values of the coefficients in the equations are also close. However, the 

differences of the flat hypsometries in the single and multi-fraction modeling series are 

pronounced, and for the equilibrium flat hypsometries, the multi-fraction modeling has a better 

performance than the single-fraction cases, since the coefficients in the scaling relations are 

closer to those derived from the observed data. 

The local balance processes in channels is proposed as interpretations. Due to limited 

remote sediment supply, the channel-flat morphology is generated from the redistribution of the 

local sediments in the basins. When multi-grain-size fractions are employed, the channel tends to 

be sculptured by the scouring of the fine grains. The fine sediments, on one hand, are more easily 

eroded, leading to more occurrences of the shallow channels. On the other hand, the lagged 

coarse sediments may prevent erosions, the deep channels thus become shallower. Therefore, 

the deeper shallow channels and the shallower deep channels result in limited changes of the 

morphological parameters about channels. However, the grain-size sorting effects on the tidal 

flats are more pronounced due to the lack of these balance processes. The pronounced 

differences in the flat hypsometry suggest the importance of grain-size sorting on the flat 

morphology. Through this effect, fine sediments deposit on the high flat, and coarse sediments 

accumulate on the low flat, resulting in the significant modifications to the flat morphology. 

133

a: initial bathymetry and grid of the reference case; b and c: bathymetry of the reference case after a 

60-year simulation period from the single and multi- fraction modeling, respectively (The color bar denotes 

the bed elevation relative to mean sea level (m)) 

134


INTERNAL ARCHITECTURE AND EVOLUTION OF BIOCLASTIC BEACH RIDGES IN 

A MEGATIDAL CHENIER PLAIN: WAVE FLUME EXPERIMENTS AND FIELD DATA 

Pierre WEILL*, Dominique MOUAZE**, Bernadette TESSIER** 

*MINES PARISTECH, CENTRE DE GEOSCIENCES, 35 rue Saint-Honoré, 77300, Fontainebleau, France, 

pierre.weill@mines-paristech.fr 

**UMR CNRS 6143 M2C, UNIVERSITE DE CAEN, 24 rue des Tilleuls, 14000, Caen, France, 

dominique.mouaze@unicaen.fr, bernadette.tessier@unicaen.fr 

Forcing parameters of chenier ridges formation and internal structure are investigated using 

field data and wave flume experiments. This work focuses on modern, coarse bioclastic beach 

ridges such as those located on the uppermost part of the tidal flat in Mt. St. Michel Bay (NW 

France), in the context of a prograding megatidal chenier plain. These ridges migrate landward 

over the upper tidal flat and salt marshes by washover processes during coincidence of high 

spring tide and enhanced wave activity, until they are stabilized and integrated in the chenier 

plain. 

The internal architecture of these ridges has been investigated on the field using 

high-frequency ground-penetrating radar (GPR). Three types of ridges were identified, that 

represent a continuum of evolution between active transgressive, mature transgressive (Fig. 1), 

and mature progradational ridges (Fig. 2). Each type reflects major differences in external 

morphology and internal structure. The altitude of the banks regarding to the level of tidal 

flooding, as well as local sediment supply, are assumed to be important forcing parameters in 

chenier development and evolution. 

In order to investigate the role of low frequency fluctuations of the level of tidal flooding, 

wave flume experiments were carried out with natural sediment sampled on the field. Despite 

differences of spatial and time scales, the experimental models compare very well with the 

morphologies and internal structures observed on the field (Fig. 1 and 2). The three stages 

identified on GPR profiles have been successfully modelled. Flume experiments confirmed that 

the flat shape of bioclastic particles plays an essential role in sediment sorting in the wave 

breaking zone, and bedding deposition on the beachface or in washover fans. On longer time 

scales, the water level appears to be the key parameter controlling the patterns of washover 

geometries. Moreover, low water levels allow sediment to accumulate off the chenier. During 

subsequent water level rise, this sediment is available for the deposition of a new washover unit, 

or for a new stage of chenier progradation, depending on the altitude of the ridge. This result 

highlights the role of multi-annual to multi-decennial tidal cycles in chenier construction. 

Both field work and flume experiment results ties up with the conclusion that low frequency 

mean water level fluctuations control the dynamics and the evolution of chenier ridges, and 

consequently their internal architecture. On the field, low frequency mean water level fluctuations 

are related to the 4 and 18 years tidal cycles, which should thus be regarded as the main factor of 

chenier coast evolution at this time scale in such macrotidal environments. 

135


Comparison between flume experiment results (A) and GPR profile (B) and interpretation (C). The different 

colours emphasize the similarities between the different morpho-sedimentary units. HSTL = High Spring 

Tidal Level. 

136


THE LATE PLEISTOCENE–HOLOCENE STRATIGRAPHY AND SEDIMENTARY 

ENVIRONMENT OF THE TIDAL RADIAL SAND RIDGE SYSTEM, JIANGSU 

OFFSHORE, SOUTH YELLOW SEA 

Yong YIN 

THE KEY LABORATORY OF COAST AND ISLAND DEVELOPMENT, Hankou rd. 22, 210093, Nanjing, 

China, yinyong@nju.edu.cn 

The South Yellow Sea is a shallow and semi-closed, epicontinetal sea between the Korean 

peninsula and China, with average water depth of 46m. The western coast of South Yellow Sea 

within Jiangsu province has a length of 888.9 km and mostly dominated by tidal flat. On the 

average, it has a slope less than 1/1000 and a width between 4 and 5 km. But the widest tidal flat 

can reach to 14 km. On offshore area, a characteristic tidal radial sand ridge system (TRSRS), 

radiating perpendicularly or at a high angle to the coastline, has developed under a complex tidal 

current field along the west coast of South Yellow Sea between the Yangtze River delta to the 

south and the abandoned Yellow River delta to the north. This ridge system has a length of 

199.6km in latitude and 140 km in longitude, which covers an area of 22470km2. It contains more 

than 70 ridges and tidal channels between them. The ridge system which overlies the late 

Pleistocene terrestrial and marine deposits has formed during Holocene period. The late 

Pleistocene terrestrial deposits are mostly contributed by the Yangtze and Yellow River (the two 

biggest rivers in China) when they flowed into the sea in the study area. There remains lot of 

uncertainties about the evolution of sedimentary environments and the source materials whether 

they are derived from Yangtze or Yellow River. This paper is based on 12 cores and some 

chronological control obtained in 2007 and 2011. We try to set up the stratigraphic framework and 

sedimentary sequence based on sedimentary facies and core correlation between. We also try to 

distinguish the source of deposits from clay mineral ratio from cores. 

12 cores, some from sandy ridges and some from tidal channels have been drilled to reveal 

the late Pleistocene–Holocene sedimentary environment of the system. Seven facies have been 

distinguished (fig.1): (1) Fluvial. This facies usually appears on the core bottom. It consists of 

fining-upward successions of poorly sorted fine to medium sands, with fine pebbles. Ripple cross 

and horizontal-beddings are common. No foraminifera, but fresh water snails are present. 

Calcareous concretion probably containing ferric oxide can be found in the facies. These deposits 

are probably from the point bar. In core 07SR11, the overbank deposits have been found 

superimposed on the point bar, which are composed of olive grey to greyish brown silty clay to 

clay, with lenticular beddings and horizontal laminas. Climbing-ripple laminations are common in 

the facies. (2) Tidal flat. This facies appears immediately beneath and above the so called stiff 

clay. It consists of light olive grey silt, interlayered with dark yellowish brown silty clay. Flaser, 

wavy and lenticular beddings, with bidirectional laminations are common. Foraminifera species 

are mostly benthic communities, indicating littoral to neritic environment. (3) Estuary to Neritic. 

This facies consists of olive black clay with silty layers, interlayered with poorly sorted light olive 

grey silt, with lenticular and wavy beddings and few bioturbation. Foraminifera species are similar 

to tidal flat. (4) tidal-controlled coast to inner shelf. This environment includes sandy ridge and 

associated tidal channels. The tidal ridge is characterized by massive sand and sand-dominated 

couplets such as flaser beddings. The muddy pebbles are common in this facies. Tidal channel 

consists of light olive grey silt and muddy silt, with wavy beddings. Bidirectional cross beddings 

and contorted beddings are common. (5)Stiff mud (paleosol). This facies is composed of yellow 

brown clay and silty clay. The stiff mud contains abundant pedogenesis features, such as 

argillans, ferric mottles, concretions and plant roots, but lacks marine microfossils. The stiff mud 

was produced in a complex terrestrial environment from fluvial overbank to swampy and 

lacustrine plain. It is distinct from overlying strata in lithological characteristics and microfossil 

assemblages with sharp contact. 14C dating indicated that stiff mud was formed during 15-25 ka 

B.P. (Li et al., 2001). 

The scenario shows that during the MIS 4, the cut down of incised valley took place in study 

area due to the sea level decline. With the sea level rise during the MIS 3, the incised valley has 

been filled with fluvial and tidal flat deposits successively. It experienced extensive exposure 

during the LGM and produced the symbolized stiff mud (paleosol). The study area was drowned 

during the Holocene transgression and received tidal flat deposits at the first period of sea level 

rise and then estuary to neritic deposits during Mid-Holocene. In late Holocene, the study area 

changed to a tidal-controlled coast to inner shelf. The sediments have been reworked by strong 

tides to build up sandy ridges and channels between them. 

137


The stratigraphic correlation between cores in study area 

Li, C.X, Zhang, J. Q.,Fan D. D. et. al.,2001. Holocene regression and the tidal radial sand ridge system 

formation in the Jiangsu coastal zone, east China. Marine Geology, 173:97-120 

138


MODELING THE FORMATION OF A SAND BAR WITHIN A LARGE 

FUNNEL-SHAPED, TIDE-DOMINATED ESTUARY: QIANTANGJIANG ESTUARY, 

CHINA 

Qian YU 

MOE KEY LABORATORY OF COAST AND ISLAND DEVELOPMENT, 22 Hankou Road, Nanjing 

University, 210093, Nanjing, China, qianyu.nju@gmail.com 

The Qiangtangjiang Estuary (the outer part being known as Hangzhou Bay) located on the 

east coast of China is a large funnel-shaped, tide-dominated and well-mixed estuary. The 

equilibrium estuarine morphology has been attained and characterized by a large sand bar having 

a total length of 125 km and an elevation of 10 m above the average adjacent seabed. In order to 

investigate the physical processes governing the formation of this morphological feature, 

two-dimensional depth-averaged process-based morphodynamic modeling (Delft3D) was carried 

out on a schematized funnel-shaped domain with exponentially decreasing widths based on the 

dimensions of the Qiangtangjiang Estuary. The model simulated a 6,000-year period, the output 

showing the development of a sand bar that reached equilibrium within about 3,000 years. The 

general shape, size and position of the modeled sand bar are consistent with the observations. 

Short-term simulations of hydrodynamic and sediment transport processes at the initial stage 

indicate that, in response to the interactions between river discharge and tidal currents, which are 

strongly influenced by the funnel-shape, the sand bar developed in the transition zone between 

the river-dominated upper estuary and the flood-dominated lower estuary where sediment 

transport pathways converge. A series of sensitivity analyses suggest that the estuarine 

convergence rate, sediment grain size, and river discharge are the main controlling factors of 

sand bar formation. Similar to other large funnel-shaped, tide-dominated estuaries of the world, a 

sufficient supply of fine cohesionless sediment (derived from the adjacent Changjiang Estuary), a 

large river discharge, and a strong shoreline convergence rate have shaped the large sand bar in 

the Qiangtangjiang Estuary. 

139


Modelled long-term evolution of the longitudinal bed morphology of Qiangtangjiang estuary, and the 

modelled final (6000 yr) equilibrium lateral averaged bed and the large sand bar. 

140


THE VARIATIONS OF SALINITY AND STRATIFICATION FOR MICRO-TIDAL AND 

MANGROVE-COVERED FROG CREEK SYSTEMS, FLORIDA 

Jicai ZHANG*, Joseph HUGHES**, Ping WANG***, Mark HORWITZ*** 

*MOE KEY LABORATORY OF COAST AND ISLAND DEVELOPMENT, 22 Hankou Road, Nanjing 

University, 210093, Nanjing, China, jczhang2008@yahoo.cn 

**U.S. GEOLOGICAL SURVEY, Florida Water Science Center, 33612, Tampa, United states, 

jdhughes@usgs.gov 

***COASTAL RESEARCH LABORATORY, DEPARTMENT OF GEOLOGY, Department of Geology, 

University of South Florida, 33620, Tampa, United states, pwang@usf.edu, mhorwitz@mail.usf.edu 

The variations of salinity and stratification for Terra Ceia River and Frog Creek (Frog Creek 

systems), Florida, which were mangrove covered, micro-tidal, partially mixed and shallow 

estuaries, were discussed based on one-year observations. Temperature, salinity and tidal 

fluctuation were all important physical factors that influence the size and extent of mangrove 

swamps. The level of stratification in the water column was crucial in controlling the intensity of 

vertical mixing and hence, the vertical flux of water properties. The circulation of Frog Creek 

systems was driven by weak tidal dynamics and small river discharge, which can be a 

supplement to the studies of estuarine hydrodynamics. Salinity observations indicated that the 

saline water can persistently affect upstream areas of Frog Creek systems and the reason was 

attributed to the bathymetry of river channel. The results of spectral analysis also proved that the 

bathemetry can significantly influence the temporal structure of salinity. The effects of periodical 

tidal shears and river freshwater discharge on the stratification were investigated. Well mixed 

conditions were observed during flood tide and stratified conditions during ebb tide. Besides, we 

found that the stratification can be enhanced by higher river discharge, while the stratification 

would be destroyed above a threshold river discharge. The threshold river discharge value was 

described qualitatively by: (1) processing the salinity time series with a low pass filter to eliminate 

the diurnal, semidiural and other high-frequency tidal signals; (2) calculating the filtered (i.e., 

subtidal) stratification as the difference between the bottom and the surface subtidal salinities; (3) 

rearranging the filtered stratification data according to the time of corresponding river discharge. 

Example from Frog Creek Systems, Florida. The 100 pairs of average stratification versus 

exceedence probability (p) at four stations are shown in Fig. 1. The clearest relation of 

stratification and p is observed at TF3 as shown in Fig. 1a. When the exceedence probability is 

less than 10%, the stratification is 1 or less. When p exceeds 10%, the stratification increases to 

values as high as 12. When p is approximately 20%, the stratification is sharply reduced to about 

6. Above a p of 20%, the stratification shows an approximately linear decrease from 6 to 2 with 

increasing p. A similar response is also observed at TF2 as shown in Fig. 1b. However, the trends 

are not very clear at TF1 or Manatee River where stratification would also be influenced by 

periodical tidal variations (Figs. 1c and 1d). 

141


Stratification versus the exceedence probability at TF3 (a), TF2 (b), TF1(c) and Manatee River (d). Red 

dotted lines indicate the trend of variations. 

142


143


LIST OF AUTHORS 

144


A 

ABOUESSA Ashour: p. 99, 101 

ABRAHAM Romain: p. 85, 91, 123 

ALVAREZ Luis G.: p. 1 

ANDERSEN Thorbjørn Joest: p. 47, 69 

ANDRE Jean-Pierre: p. 107 

ARAI Shota: p. 87 

ARCHER Allen: p. 3 

B 

BAFFREAU Alexandrine: p. 85, 123 

BANDEIRA Salomao: p. 93 

BARRIOS Edixon Jose: p. 5 

BARTHOLDY Jesper: p. 7 

BARTHOLOMAE Alexander: p. 9, 115 

BAUCON Andrea: p. 11, 13 

BENITO M. Isabel: p. 35, 103, 117 

BERTEL F: p. 75 

BERYOUNI Khadija: p. 31 

BESSON David: p. 29 

BILLEAUD Isabelle: p. 121 

BILLY Julie: p. 21 

BLANPAIN Olivier: p. 41 

BOUST Dominique: p. 127 

BOUZA Pablo: p. 113 

BREILH Jean-François: p. 21 

BURCHARD Hans: p. 45 

C 

CAI Guofu: p. 39 

CHAMIZO BORREGUERO M.: p. 15 

CHANG Taesoo: p. 17, 19 

CHAUMILLON Eric: p. 21 

CHEN Wayne, C.: p. 81 

CHIARELLA Domenico: p. 83 

CHOI Kyungsik: p. 23, 25, 27 

CHUN Seong Soo: p. 115 

CLIQUET Dominique: p. 67 

COSSONNET Catherine: p. 127 

CUITIÑO José Ignacio: p. 113 

CUVILLIEZ Antoine: p. 79 

D 

DALRYMPLE Robert W.: p. 29, 65, 73, 95, 

105, 107 

DAUVIN Jean-Claude: p. 31, 85, 123 

DE BOER Poppe: p. 15, 33 

DELCAILLAU Bernard: p. 67 

DELOFFRE Julien: p. 79, 127 

DIAZ-MOLINA Margarita: p. 35 

DIEZ-CANSECO Davinia: p. 35 

DING Hao: p. 129 

DOZO Teresa: p. 113 

DUBRULLE-BRUNAUD Carole: p. 127 

DUGUE Olivier: p. 67 

DURINGER Philippe: p. 99, 101 

E 

EKWENYE Ogechi: p. 37 

EL-BARKOOKY Ahmed: p. 77 

ERNSTSEN Verner B.: p. 7 

ESIRTGEN Tolga: p. 63 

F 

FAN Daidu: p. 39 

FELLETTI Fabrizio: p. 11, 13 

FENIES Hugues: p. 21 

FERRANDINI Jean: p. 107 

FERRANDINI Michelle: p. 107 

FERRET Yann: p. 41 

FLEMMING Burghard W.: p. 43, 115 

FLINT Stephen: p. 55 

FLOESER Goetz: p. 45 

FOREY Estelle: p. 75 

FRITIER Nicolas: p. 79 

FRUERGAARD Mikkel: p. 47 

FURGEROT Lucille: p. 49 

G 

GAO Shu: p. 133 

GARLAN Thierry: p. 41 

GHIENNE Jean-François: p. 99 

GLUARD Lucile: p. 51 

GONG Wenping: p. 53 

GUGLIOTTA Marcello: p. 55 

H 

HAMPSON Gary: p. 77 

HAQUIN Sylvain: p. 49 

HERRLING Gerald: p. 57 

HODGSON David: p. 55 

HOLLER Peter: p. 9 

HONG Chang Min: p. 27 

HORWITZ Mark: p. 141 

HUGHES Joseph: p. 141 

HUSTELI Berit: p. 59 

I 

ICHASO Aitor: p. 73, 105 

ILGAR Ayhan: p. 61, 63 

ITO Takashi: p. 87 

J 

JABLONSKI Bryce: p. 65 

JACKSON Christopher: p. 77 

JACKSON Matthew: p. 77 

JAMES Noel: p. 29, 107 

JAMET Guillaume: p. 67 

JENSEN Maria: p. 59 

JO Joo Hee: p. 25 

JOHANNESSEN Peter N.: p. 47, 69 

JOHNSON Howard: p. 77 

JUNG Jae Hoon: p. 25, 27 

K 

KALIN Otto: p. 35 

KARAKUS Erhan: p. 61, 63 

KAYA Serap: p. 61 

KIM Jincheol: p. 17 

KITAZAWA Toshiyuki: p. 71 

KURCINKA Colleen: p. 73 

L 

LAFITE Robert: p. 41, 75, 79 

LANGLOIS Estelle: p. 75 

LE BOT Sophie: p. 41, 75


LEE In Tae: p. 115 

LEGLER Berit: p. 77 

LEMOINE Maxence: p. 79 

LESOURD Sandric: p. 79 

LESUEUR Patrick: p. 79, 127 

LEVA LOPEZ Julio: p. 109 

LEVOY Franck: p. 51 

LIU James T.: p. 81 

LONGHITANO Sergio: p. 83 

LOZACH Sophie: p. 31, 85, 123 

M 

MACKAY Duncan: p. 105 

MAKINO Yasuhiko: p. 87, 89 

MALENGROS Deny: p. 85, 123 

MARGOTTA José: p. 91 

MAS Ramón: p. 103, 117 

MASSART Benoit: p. 77 

MASSEI Nicolas: p. 79, 127 

MASSUANGANHE Elidio: p. 93 

MEAR Yann: p. 31 

MEIRLAND Antoine: p. 75 

MELENDEZ N.: p. 15 

MICHAUD Kain: p. 95 

MILBRADT Peter: p. 125 

MOUAZE Dominique: p. 49, 135 

MURAT Anne: p. 31 

MØLLER Ingelise: p. 69 

N 

NANAYAMA Futoshi: p. 87 

NICHOLS Gary: p. 37 

NIELSEN Lars Henrik: p. 47, 69, 69 

NWAJIDE Sunny: p. 37 

O 

OBI Gordian: p. 37 

OH Chung Rok: p. 27 

OLARIU Cornel: p. 23, 109 

OLAUSSEN Snorre: p. 59 

P 

PARIZE Olivier: p. 29, 107 

PARK Soo Chul: p. 97 

PEJRUP Morten: p. 47, 69 

PELLETIER Jonathan: p. 99, 101 

PEREZ Laurent: p. 49 

POIZOT Emmanuel: p. 31, 85, 123 

Q 

QUIJADA I. Emma: p. 103, 117 

R 

RAMIREZ Rafael: p. 1 

RAVNAS Rodmar: p. 77 

REITH Geoff: p. 105 

REYNAUD Jean-Yves: p. 107 

RIETHMUELLER Rolf: p. 45 

ROSSI Valentina: p. 109 

ROZET Marianne: p. 127 

RUBINO Jean-Loup: p. 99, 101, 107 

S 

SAITO Yoshiki: p. 111 

SCASSO Roberto: p. 113 

SCHUSTER Mathieu: p. 99, 101 

SEIBEL Meg: p. 29 

SHANG Shuai: p. 39 

SOLIER Luc: p. 127 

SON Chang Soo: p. 115 

SONG Shengli: p. 129 

SORREL Philippe: p. 121 

SPALLUTO Luigi: p. 83 

STEEL Ronald: p. 23, 109 

SUAREZ-GONZALEZ Pablo: p. 103, 117 

T 

TANAKA Akiko: p. 119 

TESSIER Bernadette: p. 49, 107, 121, 135 

THOMAS Sandrine: p. 127 

TIMUR Erol: p. 61 

TRENTESAUX Alain: p. 85, 91, 123 

TRIBOVILLARD Nicolas: p. 91 

TU Jinbiao: p. 39 

TURKMEN Banu: p. 61 

V 

VALERIUS Jennifer: p. 125 

VAN ZOEST Michael: p. 125 

VEIGA Gonzalo: p. 55 

VENNIN Emmanuelle: p. 107 

VIEL Félix: p. 49 

VREL Anne: p. 127 

W 

WANG Dong: p. 129 

WANG Ling: p. 129 

WANG Ping: p. 141 

WANG Ya Ping: p. 131 

WANG Yunwei: p. 133 

WEILL Pierre: p. 135 

WESTERBERG Lars-Ove: p. 93 

WINTER Christian: p. 57 

WU Jichun: p. 129 

WU Yijing: p. 39 

Y 

YIN Yong: p. 137 

YOO Dong-Geun: p. 17 

YU Qian: p. 133, 139 

Z 

ZEILER Manfred: p. 125 

ZHANG Jicai: p. 141 

ZHU Qingping: p. 129

programme tuesday, july, 31 - UniversitÃ© de Caen Basse Normandie

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