Rome et Éphèse sont deux villes portuaires emblématiques de la Méditerranée antique ; la première fut le centre de l’Empire romain et la seconde devint la capitale romaine d’Asie mineure à la fin du 1er s. av. J.-C. Leur rayonnement économique et commercial en Méditerranée reposa notamment sur leur système portuaire. Cette étude a pour vocation de retranscrire le développement économique de ces deux cités par le signal des paléo-pollutions. Pour mener à bien ces travaux, nous avons prélevé des carottes dans les archives sédimentaires des bassins portuaires sur lesquels les isotopes du plomb ont été mesurés. La reconstitution des paléo-environnements par la géochimie élémentaire a été un préalable indispensable. Sur le temps long, la dynamique des masses d’eau portuaires fut visiblement soumise à la progradation des systèmes deltaïques, ainsi qu’aux interventions humaines qui modifièrent les environnements aquatiques initialement ouverts et bien oxygénés au profit de milieux fermés en déficit de dioxygène. Ce confinement des bassins portuaires franchit un seuil irréversible pour la navigation dès lors qu’un régime épilimnique se mit en place en raison d’une trop faible profondeur de la colonne d’eau. Les niveaux de contamination au plomb ont relativement bien enregistré l’état de santé économique de Rome et d’Éphèse qui évolua notamment au gré des périodes de prospérité et de troubles. Cependant, l’évolution des conditions environnementales et les multiples dragages semblent avoir altéré une partie de ces enregistrements. Les données isotopiques du plomb, converties en paramètres géologiques (Tmod, μ et к), nous ont également permis d’émettre des hypothèses sur les sources d’approvisionnement en minerais de plomb à l’origine de ces pollutions. On peut en retenir que les stratégies d’alimentation en plomb à l’époque romaine furent locales. En effet, il semble assez logique que ces deux cités aient dominé les espaces économiques environnants avec lesquelles elles étaient en contact. En revanche, alors que l’entrée dans le Moyen Âge s’accompagne du déclin de Rome, Éphèse retrouve sa prospérité passée avec l’importation de plomb hercynien d’Europe de l’Ouest produit massivement à la suite de la révolution économique médiévale. / Rome and Ephesus are two iconic harbor cities of the ancient Mediterranean; the first was the center of the Roman Empire and the second became the Roman capital of Asia Minor at the end of the 1st c. BC. The economic and commercial influence of these two ports in the Mediterranean depended heavily on their harbor systems. The aim of this study is to discern the economic development of Rome and Ephesus from the geochemical signals of the pollution they were exposed to. To this end, we drilled cores through the sedimentary archives of the two ancient harbors and measured major and trace element concentrations and Pb isotope compositions. Both harbors were subject to delta progradation, Rome by the Tiber and Ephesus by the Caÿster, which changed the aquatic environments from being initially open and well oxygenated to becoming closed and anoxic. The harbor basins finally shut down for shipping when an epilimnic system came into place due to too shallow a depth of the water column. Although changing environmental conditions and multiple dredgings appear to have altered some parts of the geochemical record, the pollution levels of lead quite accurately reflect the state of the economic health of Rome and Ephesus, which evolved the most during periods of prosperity and disorder. Pb isotope data, converted into geological parameters (Tmod, μ and к), further allowed deducing the provenance of the geological sources of lead ores at the origin of the pollution. Based on these results, it appears that lead ore supplies during the Roman period were of local origins, reflecting how Rome and Ephesus dominated the surrounding economic areas with which they were in contact. However, while the beginning of the Middle Ages is accompanied by a decline of Rome, Ephesus regains its past prosperity with the importation of Hercynian lead from western Europe. It was produced massively as a result of the medieval economic revolution that Europe experienced from the 10th century onward.

Estuarine circulation and its associated transport processes drive the environmental integrity of many near-shore habitats (the coastal ocean, rivers, estuaries and emergent wetlands). A thorough understanding and consideration of this circulation is, therefore, vital in the proper management of these habitats. The aim of this study is to bring together theory and new satellite observations in the Columbia River Estuary to increase our understanding of estuarine circulation and transport. Surface reflectance measurements gathered by the Moderate Imaging Spectroradiometer (MODIS) are first compared to in situ observations to develop an empirical model for remotely derived surface turbidity. Results indicate that MODIS data significantly correlate with in situ measurements of turbidity throughout the CRE (R2 = 0.96). Remote estimates of turbidity are then used to explore the physical processes that drive their spatial distribution. Although the response to different hydrodynamic conditions varies throughout the system, global levels of turbidity are most sensitive to fluvial and tidal inputs and increase during spring tides and high river flow. As a result, the turbidity field has temporal cycles that are consistent with the frequency of these processes. The location of the estuarine turbidity maximum (ETM) is highly dynamic and typically migrates downstream as the tidal velocity or river flow increases. The ETM becomes trapped near the Megler Bridge (river kilometer 20), however, and the presence of strong topography in this region suggests there exists an interaction between bottom topography and sediment transport. A 2-D semi-analytical model, developed herein from the simplified Navier-Stokes equations, confirms that topographic features exhibit substantial influence on longitudinal turbidity distributions. The model considers the coupled, tidally-averaged velocity (composed of gravitational circulation, internal tidal asymmetry, and river flow) and salinity fields and assumes a condition of morphodynamic equilibrium to estimate the distribution of sediment for arbitrary channel configurations. Model simulations demonstrate that topographic highs tend to increase local seaward sediment fluxes, and that topographic lows increase local landward sediment fluxes. Sediment flux convergence near topographic highs compresses the local turbidity distribution, whereas flux divergence near topographic lows dilates the distribution and, under appropriate conditions, produces multiple ETMs. In summary a combination of the model and satellite data has given valuable new insights into the sediment dynamics of estuarine environments; in particular, both show that turbidity distribution and ETM location vary considerably with tidal and river flow conditions, fluctuating on a variety of timescales, and are heavily influenced by bottom topography.

Une grande partie de la période Néoprotérozoïque Ediacarienne, depuis la fin de la glaciation Marinoan (c. 635 Ma) jusqu'à la limite Précambrienne-Cambrienne (c. 542 Ma), est caractérisée par d'amples excursions négatives de la courbe isotopique du carbone dans l'enregistrement CArbonaté. Ces excursions sont observables dans la 'cap séquence' Marinoan, la Shuram-Wonoka et la limite Précambrienne-Cambrienne (Fig. 0.1).<br> La succession Néoprotérozoïque d'Oman, quasiment complète, repose sur un socle daté à 822-825 Ma. Le SuperGroup de Huqf affleure largement au nord de l'Oman, dans le coeur de l'anticlinal du Jabal Akhdar. Il est constitué des sédiments glaciogéniques du group de Abu Mahara (723+16/-10 Ma). L'événement glaciaire se termine avec la 'cap carbonate formation de Hadash d'âge supposé Marinoan (c. 635 Ma). Le groupe de Abu Mahara contiens aussi les volcaniclastiques du Membre de Saqlah caractérisant un épisode d'extension crustal.<br> Le Groupe de Nafun, situé au-dessus de la Marinoan cap carbonate (Formation de Hadash), représente deux 'grands cycles' siliciclastiques à carbonatés, tous deux initiés par de grandes transgressions. Ces cycles comprennent les formations de Masirah Bay/Khufai et les formations de Shuram/Buah. La Formation de Khufai est organisée selon un profil de rampe carbonatée et représente des cycles carbonatés en «shallowing-upward» (HST), allant de facies de rampe externe à des facies à grainstones cross-stratifiés et des dépôts de back-shoal de milieu de rampe, à des cycles «shallowing upward» de rampe interne. En domaine distal, la fin du Khufai highstand est marquée par des petits chenaux incisifs, suivi d'un système transgressif dominé par des argiles monotones, déposées sous la limite d'action des vagues de tempête. Dans le Huqf (domaine proximal du bassin), la Formation de Shuram enregistre une diminution progressive de la tranche d'eau qui se traduit par une série de parasequences «shallowing upward» constituées de dépôts de tempête. Les dépôts siliciclastiques de Shuram passent progressivement aux environnements en rampe carbonatée progradante de Buah. L'excursion de Shuram (Group de Nafun, Supergroup de Huqf) d'Oman est caractérisée par une amplitude exceptionnelle (+5‰ to -12‰ d13C; Fig. 0.1) et un long enregistrement stratigraphique (~800 m). Cette tendance est observée à travers tout l'Oman, de l'affleurement à la sub-surface, et ce indépendamment des faciès sédimentaires. L'excursion est globalement en phase avec les changements relatifs du niveau marin, le paroxysme du d13C étant atteint dans la partie inferieure de Shuram, au niveau de la zone d'inondation maximum, alors que le retour aux valeurs positives apparaît avec le prisme de haut niveau de Buah. La Formation de Shuram affleure parfaitement sur les 40 km d'escarpement N-S du nord de la région du Huqf. Elle montre un empilement de parasequences «shallowing upward» dominées par des dépôts de tempête. À l'échelle de la parasequence, les valeurs isotopiques du carbone reflètent la position stratigraphique dans la pile de parasequences, et chaque parasequence montre une variation des valeurs du d13C avec la direction de progradation. Ces informations stratigraphiques et isotopiques ainsi que la reproductibilité du signal isotopique à travers l'Oman suggèrent une origine primaire et océanographique du rapport isotopique du carbone. L'excursion est contrainte par des âges radiométriques combinés à une modélisation de la subsidence thermique du bassin. Son initiation est datée à ~600 Ma, pour une durée d'approximative de 50 Ma. L'excursion, bien documentée en Oman, présente des équivalents probables dans d'autres séries Ediacariennes et pourrait constituer une spécificité de la période Ediacarienne. Cependant, une corrélation globale demeure spéculative en raison d'un enregistrement sédimentaire souvent limité par de nombreuses discordances. En Chine, la Formation de Doushantuo enregistre probablement la fin de l'excursion autour de 551 Ma. La période Ediacarienne est aussi marquée par la glaciation non-global et de courte durée de Gaskiers, autour de 580 Ma, et ces possibles corrélatifs moins bien temporellement contraints. Si la chronologie proposée est correcte, la glaciation de Gaskiers est alors comprise dans une excursion négative de large amplitude et de longue durée du carbone isotopique. La glaciation apparaît aussi sans effet direct sur l'enregistrement isotopique et stratigraphique d'Oman et des autres sections du même âge. Le fait qu'une excursion de l'isotope du carbone de cette amplitude peut être identifiée dans les sédiments Ediacariens de plusieurs continents indique qu'il s'agit d'un phénomène océanographique global, reflétant la composition océanique par laquelle les carbonates sont précipités. Une telle excursion est inhabituelle dans les temps géologiques et son explication représente un vrai défi. Cependant, le cas Shuram démontre que les excursions négatives des isotopes du carbone ne sont par liées aux glaciations per se et que l'enregistrement du carbone isotopique marin ne peut être utilisé comme témoin direct des glaciations Néoprotérozoïques.<br> Toutes tentative d'interprétation de l'excursion de Shuram doit alors inclure un temps de résidence exceptionnellement long en comparaison avec les perturbations du cycle du carbone Phanérozoïques (Fig. 0.1) et doit engager un réservoir de matériel appauvri en 13C suffisamment large (e.g. carbone organique dissous).

Hydrogeologic investigations were conducted on the drainage systems of an area of the Pennyroyal sinkhole plain of south central Kentucky. The degree of karstification of five area streams was studied to develop an understanding of the evolution of drainage as the landscape changes from a sandstone caprock plateau to a limestone sinkhole plain. The Chester Upland, capped by the Big Clifty Sandstone, possesses predominantly surface drainage and the Pennyroyal Plain, formed on Mississippian limestones, possesses considerable subsurface drainage. As the Chester Upland Escarpment retreats and surface streams are onto the limestones, the streams evolve to become subsurface streams. The five streams observed in the study (all flowing on limestones) demonstrated less karst development close to the Chester Escarpment and more karst development with increasing distance from the escarpment. Sediments derived from the escarpment and plateau blanket the stream beds thus perching the streams and preventing chemically aggressive water from forming karst solution features in the limestones. The streams farther away from the escarpment are removed from the sediment source and are therefore able to downcut into the limestone and invade the subsurface to become cave streams. Lithologic investigation of limestones exposed in stream beds revealed that minor resistant units can act to diminish downcutting and maintain short sections of surface flow. The stream investigated was not flowing on a perching layer, but instead was held on the surface by a stratigraphic control (spillover layer) that prevented subterranean stream invasion. Dye traces conducted on groundwater flow in the sinkhole plain revealed that the area drainage pattern is changing as surface streams invade the subsurface and that integration between drainage basins is taking place. Stream piracy and stream diversion are occurring in the subsurface causing alteration of the existing topographic drainage divides that developed before the surface streams invaded the subsurface. A general model is presented which shows the evolution of surface drainage to subsurface drainage, as the Chester Escarpment continues its northwestward retreat.

Η περιοχή μελέτης καλύπτει ένα μέρος των ανθρακικών αποθέσεων της Κεντρικής και Εξωτερικής Ιόνιας ζώνης οι οποίες αποτέθηκαν από το Τριαδικό έως το Ηώκαινο. Γεωγραφικά οριοθετείται, κατά τον άξονα Ανατολή – Δύση, από τον εθνικό δρόμο Άρτας – Ιωαννίνων και το Ιόνιο Πέλαγος, και κατά Βορά – Νότο από νοητούς, παράλληλους προς τον Ισημερινό άξονες που διέρχονται από την Άρτα και την Ηγουμενίτσα. Η περιοχή βρίσκεται ανάμεσα στις συντεταγμένες 20ο 12΄ και 21ο 00΄ Ανατολικά, και 39ο 00΄ με 39ο 30΄ Βόρεια και καλύπτεται από τα ακόλουθα γεωλογικά φύλλα του Ι.Γ.Μ.Ε, κλίμακας 1:50.000: Άρτα, Καναλάκι, Πάργα, Θεσπρωτικό και Παραμυθιά. Από την μικροφασική ανάλυση και την ανάλυση φασικών ζωνών που προηγήθηκε σε συνδυασμό με την βιοχρονολόγηση εξάγεται το συμπέρασμα ότι κατά το Α.Τριαδικό αποτέθηκαν μικριτικοί και κατά θέσεις λιθοκλαστικοί ασβεστόλιθοι σε περιβάλλον υφαλοκρηπίδας περιορισμένης κυκλοφορίας. Από το Α.Τριαδικό και μέχρι το τέλος του Λιασίου αποτίθενται σε όμοιες περιβαλλοντικές συνθήκες grapestones, rudstones, floatstones και grainstones. Από το Λιάσιο και μέχρι το Σαντώνιο αποτίθενται mudstone – wackestone και σπανιότερα packstone σε περιβάλλον πρόσθιας κατωφέρειας έως και υφαλοκρηπίδας ανοιχτής θάλασσας. Από το Καμπάνιο έως το Πριαμπόνιο, όπου τοποθετείται και το τέλος της ανθρακικής ιζηματογένεσης στην Ιόνιο ζώνη, αποτίθενται εναλλαγές από mudstone – wackestone και floatstone – packstone σε περιβάλλον πρόσθιας κατωφέρειας και βαθύτερο όριο υφαλοκρηπίδας. Στρωματογραφικά οι αποθέσεις της περιοχής μελέτης αποτελούνται από τέσσερις συνολικά ακολουθίες 3ης τάξης, δύο χαμηλής στάθμης (LST), μία υψηλής στάθμης (HST) και μια επικλυσιγενής (TST). Ο συνολικός όγκος των μελετηθέντων ιζημάτων ανέρχεται σε 3064,796 χλμ3, καταλαμβάνοντας χρονικό διάστημα από το Ανώτερο Τριαδικό έως το Παλαιογενές, από τα όποια 1398,050 χλμ3 αποτελούνται από τους ασβεστόλιθους του Ιουρασσικού οι οποίοι λόγω της απουσίας το Ammonitico Rosso δεν διαχωρίζονται. Επιπλέον 796,777 χλμ3 αποτελούνται από τους ασβεστόλιθους της Βίγλας οι οποίοι μαζί με τις πελαγικές αποθέσεις του Μέσου – Άνω – Ιουρασσικού απαρτίζουν την πελαγική ακολουθία 2ης τάξης. Τέλος 449,921 χλμ3 και 420,048 χλμ3 ανήκουν στους ασβεστόλιθους το Α.Κρητιδικού και του Παλαιογενούς οι οποίοι απαρτίζουν την δεύτερη ακολουθία 3ης τάξης. Οι αποθέσεις του Τριαδικού λόγω του άγνωστου υποβάθρου τους και τις ευδιάλυτης φύσης τους δεν συμπεριλήφθηκαν στους υπολογισμούς όγκου. Από την μελέτη με ηλεκτρονικό μικροσκόπιο σάρωσης προέκυψε ότι διεργασίες όπως μικριτίωση, ανακρυστάλωση, προσαύξηση και νεομορφισμός του υλικού τσιμεντοποίησης είναι καθολικές για όλα τα δείγματα. Σε κάποια δείγματα παρατηρήθηκαν πυριτικά συσσωματώματα τα οποία συνδέονται με την δράση θειοβακτηριδίων. Επίσης στο σύνολο των δειγμάτων παρατηρήθηκε ασήμαντο από άποψη υδραυλικών χαρακτηριστικών μεσοκρυσταλλικό και μεσοκοκκώδες πορώδες. Το πιο σημαντικό πορώδες παρατηρήθηκε σε δείγματα wackestone του Παλαιογενούς το οποίο συνίσταται από πορώδες διαλυσιγενών καναλιών, βιοδιάτρησης και ενδοκοκκώδες παρουσιάζοντας αυξημένο ενδιαφέρον από άποψη υδροχωριτικότητας και διαπερατότητας. Από την μελέτη των αργιλικών ορυκτών προκύπτει ότι τα ιζήματα το Μέσου Ιουρασσικού βρέθηκαν σε στάδιο Μέσης διαγένεσης και σε θερμοκρασίες που δεν υπερέβησαν τους 100 0C. Τα μεταγενέστερα ιζήματα βρεθήκαν όπως αναμένονταν σε ζώνες ασθενέστερης διαγένεσης με αποκορύφωμα τα ιζήματα του Παλαιογενούς που βρέθηκαν μόνο στο στάδιο της πρώιμης διαγένεσης ή ρηχής ταφής. Οι συνθήκες διαγένεσης κρίνονται ανεπαρκής για την ωρίμανση και γένεση υδρογονανθράκων. Από τη ανάλυση σταθερών ισοτόπων και οργανικού άνθρακα εξάγεται το συμπέρασμα ότι κανένα από τα δείγματα που μελετήθηκαν δεν συνδέεται με κανένα τρόπο με μητρικό πέτρωμα υδρογονανθράκων. Επίσης από ανάλυση μάζας πετρώματος δεν μπορούν να εξαχθούν ασφαλή συμπεράσματα ως προς την θερμοκρασία που επικρατούσε στο περιβάλλον απόθεσης, λόγω των διαγενετικών αλλαγών. Όλα τα δείγματα που εξετάστηκαν έχουν δ τιμές μέσα στο εύρος των κανονικών πελαγικών αποθέσεων. Η υπό αμφισβήτηση παραδοχή ότι από τα παλαιότερα σε νεότερα πετρώματα το περιεχόμενο σταθερών ισοτόπων γίνεται ελαφρύτερο, δεν επιβεβαιώθηκε και επιπρόσθετα από τα αποτελέσματα τεκμηριώνεται η μη ορθότητα της παραδοχής. Το ποσοστό οργανικού άνθρακα καθορίζεται από τις οξειδωτικές ή αναγωγικές συνθήκες που επικρατούσαν και από τη δράση θειοβακτηριδίων και παραμένει εξαιρετικά χαμηλο στο σύνολο των δειγμάτων (<0,05 %). Η Ιόνιος ζώνη αναπτύχθηκε πάνω από ένα παθητικό περιθώριο με υπόβαθρο παλαιοζωικά μεταμορφωμένα πετρώματα τα οποία δεν έχουν επιφανειακές εμφανίσεις. Αρχικά και μετά από ηπειρωτική διάρρηξη αποτέθηκαν εβαποριτικά και ανθρακικά ιζήματα σε περιβάλλον περιορισμένης υφαλοκρηπίδας με εκτεταμένες και διάσπαρτες υπεράλμυρες λίμνες (sabkhas). Μετά από μία σύντομη περίοδο επιφανειακής έκθεσης η στάθμη της θάλασσας αυξήθηκε και αποτέθηκαν κανονικής αλμυρότητας ασβεστόλιθοι υφαλοκρηπίδας σε όλη τη διάρκεια του Λιασίου (Κ.Ιουρασσικό, κυρίως οι λεγόμενοι ασβεστόλιθοι ‘‘Παντοκράτορα’’). Στη συνέχεια και μέχρι το Σαντώνιο (Α.Κρητιδικό) αποτίθενται πελαγικοί ασβεστόλιθοι σε περιβάλλον υφαλοκρηπίδας ανοιχτής κυκλοφορίας με γεωμετρία ράμπας ίσης κλίσης (homoclinal ramp). Το περιβάλλον παραμένει ίδιο, με κάποιες μικρές τροποποιήσεις, όπως μεταβολή της κλίσης σε συνάρτηση με τη απόσταση από την ακτή και μικρή μείωση της στάθμης της θάλασσας, μέχρι το τέλος του Ηωκαίνου (Παλαιογενές) οπότε γίνεται μετάβαση σε κλαστική ιζηματογένεση. Από όλα τα δείγματα που μελετήθηκαν αυτά που δείχνουν να έχουν εκτεθεί σε θερμοκρασίες πάνω από 90-100 0C είναι ηλικίας Ιουρασσικού ή παλαιότερα. Στη περιοχή μελέτης όλα τα δείγματα που μελετήθηκαν έχουν περιεκτικότητα σε οργανικό υλικό μέχρι 0,05 % το οποίο είναι πολύ χαμηλότερο από το ελάχιστο απαιτούμενο 0,7 % για να είναι πιθανή ή γένεση υδρογονανθράκων. Επιπλέον οι τιμές δ του σταθερού ισοτόπου 13C απέχουν πολύ από τις τιμές -18 ‰ έως -27 ‰ οι οποίες χαρακτηρίζουν τα μητρικά πετρώματα υδρογονανθράκων. Για τους παραπάνω λόγους πιθανά μητρικά πετρώματα φαίνεται να είναι οι Τοάρσιας ηλικίας, λεγόμενοι “Κατώτεροι σχιστόλιθοι με Poseidonia”, και οι πλούσιες σε οργανικό υλικό παρενστρώσεις που βρίσκονται μέσα στα Τριαδικής ηλικίας ιζήματα. Σημαντικό είναι ότι καμία από τις παραπάνω αποθέσεις δεν έχουν επιφανειακή εμφάνιση στην περιοχή μελέτης. Ταμιευτήρια πετρώματα μπορεί να είναι είτε οι ημιπελαγικές αποθέσεις του Α.Κρητιδικού και του Παλαιογενούς είτε οι μεταηωκαινικές κλαστικές αποθέσεις. Ολοκληρώνοντας το ρόλο καλυμμάτων μπορούν να παίξουν τόσο οι πελαγικές αποθέσεις από το Μ.Ιουρασσικό έως το Κ.Κρητιδικό όσο και οι μεταηωκαινικές κλαστικές αποθέσεις. / PhD Thesis title is “The sedimentological evolution of the Ionian basin during Triassic to Eocene and the possible existence of hydrocarbon plays in the central part of the basin”. The main target of the study is to reveal, in every detail, the sedimentation pattern during the above mentioned time interval. The study area is located in western Greece (Fig. 1). The sediments of the Ionian basin were studied in fifty outcrops and a number of 300 samples were collected (Fig 2). Thin sections were prepared for all the samples and they were studied under polar microscopy. The samples were classified using Dunham’s (1965) classification chart. Afterwards, SMF and FZ, after Flugel (1972) and Wilson (1975), were determined. In addition, stable isotope analysis; clay mineral analysis, organic carbon analysis and micropaleontological study were contacted. The Triassic rocks crop out sparsely and only in signs due to their stratigraphic position, the oldest rocks, and their soluble nature. The outcrops are consisted of chaotic masses with no preferred orientation and no primary structures, like bedding (Getsos et al., 2004). Often they have suffered extensive dissolution and collapsing giving rise to the formation “Solution Collapse Breccias” (Pomoni-Papaioannou, 1980; Pomoni-Papaioannou, 1985; Karakitsios & Pomoni-Papaioannou 1998). Extensive outcrops characterize lower Jurassic sediments with great thickness, completely absence of bedding or other similar primary structure and abundant fragments and fragmentation effects. Karstification, calichification and pedogenesis are common. The sediments were studied in the following six different outcrops: T45, T5, T6, T30, T33, and T38. Samples were studied under polar microscope and their sedimentological and diagenetical pattern were revealed. The studied Early to Late Cretaceous Vigla’s formation appear as extensive outcrops of thin to medium bedded limestones with an average thickness of 200-400 m. Samples were collected from fifteen outcrops around the study area and they were studied under polar microscope. The results of the sedimentological analysis were further combined with the results of low resolution stable isotope analysis, organic carbon and clay mineral analysis. The Paleogene limestones appear as extensive outcrops consisted of intercalations of thin bedded pelagic limestones and medium to thick bedded coarse bioclastic – lithoclastic limestones. Their thickness varies between 180 and 440 m. Triassic. The studied sediments are contributed to four 3rd order sequences, two low stand systems tracts (LST), one of high stand systems tract (HST) and one transressive systems tract (TST). The total volume of studied sediments amounts in 3000 km3, occupying the Late Triassic – Paleogene time interval. The first LST has a duration of 45 million years and average thickness more than 3000 metres. It is consisted of the Triassic rocks and the Early Jurassic shallow shelf limestones, the so called “Pantokrator Limestones”. The HST is constituted of the Late Jurassic to Late Cretaceous (Santonian) pelagic limestones with an average thickness of 600 metres. The duration of the sequence is almost 80 million years. Between the above mentioned sequences the TST were deposited. The deposition took part during the Middle Jurassic and duration was almost 20 million years with a maximum thickness of no more than 200 metres. Finally the last LST sequence is constituted by the Late Cretaceous (Campanian) to Paleogene (Eocene) limestones with an average thickness of 400 m. and 45 million years duration. The study of samples under SEM has revealed a common diagenetic pattern. It is consisted of early diagenetic micritization and early diagenetic neomorphism and recrystallization. In a small number of samples pyrite was studied. Usually pyrite is the product of sulphate reduction bacteria. The microporosity is mainly intecrystall and it has no importance for reservation and fluid circulation. The most important porosity was observed in samples consisted of wackestones and packstones Paleogene in age and it was consisted of solution channels, borings and intraparticle. Clay mineral analysis have revealed the Middle Jurassic sediments suffered the Middle diagenesis stage and their temperatures did not exceed 100 0C. The newer sediments reached up to the Middle stage as well with only exception the Paleogene sediments which suffered only Early diagenesis or “Shallow burial stage”. The diagenetical conditions are insufficient for the maturation and genesis of hydrocarbons. Oxygen and carbon stable isotopes analysis and organic carbon analysis has revealed that the studied sediments do not constitute oil source rocks or reservoirs. The obtained δ values of the studied sediments are within the -+ 4 ‰ which is the characteristic of the normal pelagic limestones. The organic carbon analysis was contacted with the wet oxidation method. The organic carbon content of the whole sediments is very low and do not exceeds the 0.05% value. The Ionian basin was developed on a Mesozoic passive margin. The basement is studied only in signs in nearby areas (Albania) and it is consisted of metamorphosed Palaeozoic rocks. The first sediments deposited were carbonates and sulfates. The depositional environment was restricted circulation shelf and tidal flats and evaporates on sabkhas – Salinas. During the transgressive phase the environment was deep shelf margin and it was part of a homoclinal ramp system (middle ramp). The homoclinal ramp was covered until the initialization of the deposition of the last LST phase when the environment was transformed into a distally steepened ramp or rimmed shelf. Afterwards the carbonate sedimentation came to an end and the clastic sedimentation was established in a foreland basin. The studied sediments with depositional age after the Middle Jurassic have been exposed in temperature much less than 100 0C and as a consequence they are immature. The older sediments have suffered diagenetical temperature almost 100 0C or more and as consequence they are mature. The organic carbon content, as have already been mentioned, is maximum 0.05 %. This value is much lower than minimum hydrocarbon source rock organic carbon content (0.7%). Furthermore the δ values of the carbon stable isotope are much heavier than the values -18 to -27 ‰ which are the typical values of the source rocks. Taking into account the above facts the possible source rocks of the studied area could be the Toarcian age “Lower Posidonia Shales” and the rich in organic matter clayey intercalation of Triassic age. These possible source rocks do not crop out anywhere in the study are. Potential reservoirs can be the hemipelagic LST sequence of Late Cretaceous – Paleogene age or the clastic post Eocene sediments. Potential seal rocks are the pelagic HST sequence of Middle Jurassic – Late Cretaceous limestone and the fine-grained post Eocene clastic sediments.

Il y a 7000 ans BP, la stabilisation du niveau marin a entraîné la formation de deltas. Ces zones deltaïques abritent des milieux aux degrés de protection différents favorables à une activité maritime. Cependant, ces espaces sont soumis à des contraintes naturelles : à l'échelle de la longue durée, l'alluvionnement des deltas entraîne la mobilité des littoraux et le colmatage des milieux portuaires ; à l'échelle de l'événement, les tempêtes, les tsunamis et la mobilité crustale entraînent la destruction, la submersion ou le soulèvement des zones portuaires. Ce travail porte sur l'étude des contraintes et des potentialités environnementales de cinq ports antiques répartis dans le monde Méditerranéen en marge de deltas. L'objectif est d'estimer le poids de ces contraintes sur les sociétés via une approche statistique. Pour quatre des sites d'études, l'alluvionnement est le forçage majeur. A Kition et Orgame, l'impact de l'alluvionnement est indirect. La fermeture des baies marines par l'édification de cordons littoraux crée des environnements lagunaires propices à l'installation de zones portuaires. En revanche, Fréjus et Ampurias sont soumis à un alluvionnement direct qui a rapidement colmaté les bassins. A partir de l'époque romaine et avec l'invention de la pouzzolane, des zones portuaires sont installées en milieu littoral ouvert, comme à Istanbul. Dans un contexte tectoniquement actif, les tsunamis constituent la contrainte majeure opérant sur le port byzantin de Théodose à Istanbul. Un dépôt grossier et chaotique, contenant du matériel marin et archéologique remanié, compose une partie de la séquence stratigraphique de colmatage du bassin et témoigne de ce forçage. / The stabilization of sea level at 7000 years ago led to the formation of deltaic areas. These areas constituted sheltered environments particularly conducive to maritime activity. However, these areas were also subject to natural constraints for human occupation: at long timescales, high sediment supply to deltaic areas led to significative coastal changes and the infilling of harbour areas; at shorter timescales, high-energy events and crustal mobility led to the destruction, submersion and/or uplift of harbour areas. This work focuses on the study of environmental constraints and potentialities governing five ancient harbours, located on deltaic margins in the Mediterranean. The study aims to semi-qualitatively measure of the weight of these constraints on harbour cities, using statistical approach. High sediment supply is the major natural forcing. At Orgame and Kition, the closure of marine bays by coastal barriers led to the formation of lagoon environments conducive to the installation of harbour areas. Frejus and Ampurias were subject to direct siltation which quickly infilled the harbour basin. The invention of the pozzolan in Roman times means that harbours could be constructed in coastal areas open to the sea and away from river mouths, such as Istanbul harbour. In a tectonically active context, tsunamis are the major constraint acting in the Byzantine harbour of Theodosius in Istanbul. There, the stratigraphic sequence contains a coarse and chaotic deposit composed of reworked marine and archaeological material which demonstrates the societal impacts of such a natural and destructive forcing agent.

Uma série de pesquisas realizadas em depósitos de sistemas fluviais, desenvolvidos anterior e concomitantemente à colonização dos continentes por vegetação, são aqui apresentadas com o intuito de investigar as principais características deposicionais destes sistemas, particularmente suas assembléias de fácies e elementos arquitetônicos preservados. Esta pesquisa busca, desta maneira, propor modelos deposicionais para sucessões fluviais pré-vegetação e contribuir para o avanço do conhecimento sobre as mudanças seculares em padrões de sedimentação, principalmente em relação à evolução dos rios através do tempo geológico. Estudos sedimentológicos foram realizados em depósitos fluviais da Formação Applecross do Grupo Torridon (Toniano, Escócia), Formação Guarda Velha do Grupo Guaritas (Cambriano, Brasil) e no Old Red Sandstone do Midland Valley (Siluriano-Carbonífero, Escócia). Foram empregadas análises de associações de fácies e arquitetura deposicional por meio de estudos de alto detalhe em afloramentos, combinadas a análises de paleocorrentes, de proveniência, e de estruturas de deformação sinsedimentar. Depósitos de canais fluviais meandrantes pré-vegetação com espessos depósitos de planícies de inundação ricos em sedimentos de granulação fina são pela primeira vez descritos em detalhe nos estudos aqui apresentados sobre depósitos da Formação Applecross. Diversas estruturas de deformação sinsedimentar encontradas na unidade acima referida são analisadas, revelando que seus estilos podem ser relacionados a diferentes regiões de uma planície fluvial. Nos depósitos da Formação Guarda Velha, é registrada a inter-relação entre dois sistemas fluviais coevos, cuja arquitetura deposicional contrastante resultou da diferente localização destes sistemas em relação à estrutura da bacia, assim como de diferentes áreas de captação. São relatados os efeitos de distintos controles deposicionais, como ambiente tectônico e regimes hidráulicos, sobre a arquitetura deposicional preservada em sistemas fluviais pré-vegetação. Esses dados demonstram que o estilo entrelaçado-em-lençol, apontado como o estilo pré-vegetação predominante, engloba na verdade uma variedade de diferentes estilos fluviais. Estudos em depósitos do Siluriano ao Carbonífero do Old Red Sandstone revelam o crescente impacto da vegetação sobre depósitos fluviais, particularmente o aumento exponencial de formação de paleosolos, além de mostrar semelhanças entre alguns destes sistemas com os sistemas pré-silurianos. A integração desses estudos revela que sistemas fluviais pré-vegetação são relativamente mais complexos do que previsto pelos modelos atualmente disponíveis. Importantemente, sugere que a escassez de sedimentos de granulção fina, preservados em depósitos fluviais pré-silurianos, está mais relacionada à baixa competência destes sistemas em preservar tais sedimentos do que à sua suposta ausência em ambientes pré-vegetação. Foi também desenvolvida uma metodologia específica para o uso de estruturas de deformação em sedimentos inconsolidados como ferramentas na reconstrução de paleoambientes, através das relações entre diferentes estilos deformacionais e ambientes deposicionais, possibilitando a indicação de regimes hidráulicos em depósitos fluviais e a informação indireta de taxas de atividades tectônicas em bacias. A integração de dados de sedimentologia com estudos específicos de deformação sinsedimentar é uma ferramenta útil na reconstrução paleoambiental de sistemas fluviais. / A series of studies were undertaken on fluvial systems deposits which developed prior to land-plant colonization, in order to investigate the main depositional characteristics of those systems, particularly their main facies assemblages and preserved depositional architecture. Main objectives are the proposal of depositional models for pre-vegetation fluvial systems, and the understanding of main secular changes in sedimentation processes and its influence on the evolution of rivers through geological times. Sedimentologic studies were undertaken in fluvial deposits from the Applecoss Formation of the Torridon Group (Tonian, NW Scotland), the Guarda Velha Formation (Cambrian, southern Brazil), and the Old Red Sandstone in the Midland Valley (Silurian-Carboniferous, NE Scotland). Highly-detailed sedimentary facies and depositional architecture analyses in outcrop scale were integrated with palaeocurrent and provenance studies, and soft-sediment deformation analysis. Pre-vegetation meandering channel deposits with relatively thick, fine-grained floodplain deposits from the Applecross Formation and here described for the first time. Analyses on sinsedimentary deformation structures preserved in the Applecross Formation reveal different styles which can be related to different parts of the fluvial plain. Studies on the Guarda Velha Formation revealed the inter-relationship between two coeval fluvial systems with markedly contrasting preserved depositional architecture, which developed as a result of the different location of the systems in relation to basin structure and different caption areas. The effects of different depositional controls on preserved pre-vegetation fluvial system architecture, such as tectonic environment and hydraulic regime, are recorded and interpreted. The present data demonstrate that the sheet-braided style, which is regarded as the prevailing fluvial style before the Silurian, in fact encompasses a varied number of different pre-vegetation fluvial styles. Studies on the Silurian to Early Carboniferous Old Red Sandstones in the Midland Valley of Scotland reveal the progressive impact of land plants on fluvial sedimentation, particularly the exponential increasing rates of soil production. Integration of the here presented data reveal that pre-vegetation fluvial styles. Studies on the Silurian to Early Carboniferous Old Red Sandstone in the Midland Valley of Scotland reveal the progressive impact of land plants on fluvial sedimentation, particularly the exponential increasing rates of soil production. Integration of the here presented data reveal that pre-vegetation fluvial systems are relatively more complex than previously described in the literature. Importantly, it suggests that the paucity of fine-grained sediments in pre-Silurian fluvial deposits is most likely related to various preservation issues than to the lack of such sediments. A particular methodology for the use of soft-sediment deformation structures as palaeoenvironmental tool was developed, allowing the interpretation of hydraulic regimes in fluvial deposits, indication of the basin\'s tectonic activity, and the relationship between different deformation styles and distinct depositional environments. The combined analyses of soft-sediment deformation structures and sedimentologic data is a powerful tool with which fluvial systems palaeoenvironmental can be reconstructed.

Dans le bassin d’avant-pays sud-pyrénéen, la continuité exceptionnelle des environnements de dépôts du complexe deltaïque éocène moyen du Sobrarbe permet d’observer l’architecture stratigraphique et sédimentaire d’un système fluvio-deltaïque syntectonique à différents échelles. L’objectif principal de cette étude est de déterminer l’origine des facteurs allogéniques et/ou autogéniques contrôlant la géométrie et la répartition des dépôts d’un tel système sédimentaire en contexte compressif, dans le but de pouvoir le comparer à d’autres systèmes deltaïques accumulés dans des contextes géologiques différents. Cette étude est basée sur l’acquisition d’une cartographie géologique détaillée et d’une soixantaine de logs sédimentologiques. La base de données est complétée par une actualisation de données chronostratigraphiques issues de la littérature, l’acquisition de données magnétostratigraphiques. L’analyse sédimentologique et stratigraphique du système sédimentaire aboutit à une description précise des géométries, des faciès et des processus physiques caractérisant les différents environnements de dépôt répartis au sein de deux modèles sédimentaires : un système fluvio-deltaïque de forte énergie développé pendant les phases progradantes, un système mixte gréso-carbonaté de basse énergie caractérisant les phases aggrado-progradantes et transgressives. L’analyse de trois transects de corrélation, d’orientation proximale-distale, a permis la distinction de trois ordres de séquence imbriqués : les séquences de cinquième ordre, les séquences de quatrième ordre et les séquences de troisième ordre. L’organisation complexe des différents cortèges de dépôts des séquences de quatrième et de troisième ordre reflète des variations d’accommodation provoquées principalement par les déformations structurales de différentes longueurs d’onde, secondairement par les variations eustatiques. Une analyse poussée des cortèges de dépôts permet une discussion sur les interrelations entre les trois paramètres majeurs qui contrôlent la dynamique du système sédimentaire dans le temps et dans l’espace: les variations du taux d’accommodation, du flux sédimentaire et l’influence des processus sédimentaires. Ces éléments fournissent des informations semi-quantitatives sur l’accumulation sédimentaire au sein des différents environnements de dépôt (source to sink). La synthèse des résultats aboutit à la reconstruction séquentielle de la paléogéographique du complexe deltaïque du Sobrarbe. Enfin; l’analyse de la subsidence du bassin d’Ainsa a permis de reconstituer l’évolution de la sédimentation et du bassin sédimentaire entre le Lutétien et l’Oligocène. Une étude intégrée affleurement-modélisation sismique synthétique-analogue réel de subsurface fournit une combinaison de données architecturales et dimensionnelles, qui est utilisée pour améliorer les interprétations sismiques des systèmes réservoirs fluvio-deltaïques. De telles études réduisent considérablement les incertitudes associées à la résolution des données de subsurface, ce qui permet une meilleure évaluation économique des réservoirs. / In the South-Pyrenean foreland basin, the exceptional continuity of middle Eocene Sobrarbe deltaic complex deposit environments allows to observe the stratigraphic and sedimentary architecture of a syntectonic river-dominated delta system at different scales. The main objective of this study is to determine the origin of allogenic and/or autogenic factors that control the distribution of deposits of such sedimentary system in a compressive setting, in order to compare it to other deltaic systems that accumulate in different geological contexts. This study is based on the acquisition of detailed geological mapping and about sixty measured sections. The database is complemented by updating chronostratigraphic data from the literature and additional magnetostratigraphic data. Sedimentological and stratigraphic analysis of the sedimentary system leads to an accurate description of geometry, facies and physical processes of different depositional environments distributed along two sedimentary models: a high energy river-delta system developed during progradational phases, a low energy mixed siliciclastic-carbonate system characterizing the aggrado-progradational and transgressive phases. Three dip sections analysis allows the identification of three nested order sequence: fifth-order sequences, fourth-order sequences and third-order sequences. The complex organization of fourth and third-order sequences systems tracts reflects accommodation variations caused mainly by structural deformation at different scales, secondary by eustatic changes. An advanced systems tract analysis leads a discussion of interrelationships between three main parameters that control the dynamics in time and space of sedimentary system: changes in the accommodation rate, sediment input and the influence of sedimentary processes. These elements provide semi-quantitative information regarding to the sediment accumulation within the different depositional environments (source to sink). Summary of results leads to the sequential reconstruction of the Sobrarbe deltaic complex paleogeography. Subsidence analysis of the Ainsa basin permits to reconstruct the sedimentation and sedimentary basin evolution from Lutetian to Oligocene times. An integrated study of outcrop-forward seismic modelling-real seismic analog provides an architectural and dimensional data combination used to improve seismic interpretation of river-deltaic reservoir systems. Such studies greatly reduce the uncertainties associated with the resolution of subsurface data, enabling better economic assessment of reservoirs. / En la cuenca de antepais surpirenaica, la continuidad extraordinaria de los ambientes de deposito del complejo deltaico eoceno medio del Sobrarbe permite la observacion de la arquitectura estratigrafica y sedimentaria de un sistema fluvio-deltaico sintectonico a diferentes escalas. El objetivo principal del estudio presentado es la determinacion del origen de los factores alogenicos y/o autogenicos que controlan la distribucion de los depositos de dicho sistema sedimentario en contexto compresivo, para poder compararlo con otros sistemas deltaicos acumulados en contextos geologicos diferentes. Este estudio se basa en la adquisicion de una cartografia geologica detallada y de una sesentena de columnas sedimentarias. La base de datos se completa mediante la actualizacion de los datos cronoestratigraficos originarios de la literatura y la adquisicion puntual de datos magnetoestratigraficos. El analisis sedimentologico y estratigrafico del sistema sedimentario ha dado lugar a una descripcion exacta de las geometrias, las facies, y de los procesos fisicos que caracterizan los diferentes ambientes de depositos dentro de dos modelos sedimentarios: un sistema fluvio-deltaico de alta energia desarrollado durante fases progradantes, un sistema mixto detritico-carbonatado caracterizando fases agrado-progradantes y transgresivas. El analisis de tres paneles de correlacion, de orientacion proximal-distal, ha permitido la distincion de tres ordenes de secuencialidad: secuencias de quinto orden, de cuarto orden y de tercer orden. La organizacion compleja de diferentes cortejos de deposito de secuencias de cuarto y tercer orden refleja variaciones de acomodacion provocadas principalmente por la deformacion estructural a diferentes escalas y por variaciones eustaticas. Un analisis detallado de los cortejos sedimentarios permite una discusion sobre interrelaciones entre los tres parametros mayores que controlan la dinamica del sistema sedimentario en el espacio y en el tiempo: las variaciones de la tasa de acomodacion, del flujo sedimentario y la influencia de procesos sedimentarios. Dichos elementos proporcionan informacion semicuantitativa sobre la acumulacion sedimentaria en los ambientes de deposito (source to sink). La sintesis de los resultados llega a la reconstruccion de la paleogeografia del complejo deltaico del Sobrarbe. Finalmente, el analisis de la subsidencia de la cuenca de Ainsa ha permitido de reconstruir la evolucion de la sedimentacion y de la cuenca sedimentaria entre el Luteciense y el Oligoceno. Un estudio integrado afloramiento-modelizacion sismica sintetica-analogo real de subsuelo proporciona una combinacion de datos arquitecturales y dimensionales util para mejorar interpretaciones sismicas de sistemas reservorios fluvio-deltaicos. Dichos estudios reducen de manera considerable incertidumbres asociadas a la resolucion de los datos de subsuelo, lo que permite una mejor evaluacion economica de los reservorios.

L'étude du système aquifère du Chari Baguirmi vise à améliorer sa connaissance en vue d'une gestion durable etprudente de la ressource en eaux souterraines. Dans la zone d'étude qui couvre 70000 Km2, des campagnes demesures et d'échantillonnages des eaux et de sédiments ont été réalisés. Les eaux échantillonnées ont fait l'objetd'analyses chimiques et isotopiques (O18 et 2H) afin de comprendre le comportement hydrogéochimique dusystème aquifère. La synthèse des données géologiques existantes et la mise en évidence de l'hétérogénéité litho-stratigraphiquepar l'étude granulométrique ont confirmé la complexité hydrogéologique de la zone d'étude. La minéralogie desargiles a montré que le dépôt des différents sédiments se fait de la périphérie vers le centre de la dépression. Cemode de sédimentation permet d'avancer l'hypothèse de l'existence d'une dépression vers laquelle les sédimentsseraient entrainés par l'agent de transport. Cette hypothèse de “ dépression structurale ” réfute l'hypothèseadmise jusqu'à présent d'une origine hydrogéologique (forte évaporation) de cette dépression piézométrique.L'étude basée sur la piézométrie et les données chimiques et isotopiques (O18 et 2H) des eaux a permis decomprendre les processus hydrogéochimiques qui gouvernent la minéralisation des eaux. En plus des isotopes(O18 et 2H), l'utilisation des ratios Br/Cl, Sr/Ca et l'indice d'échanges de bases a permis de mettre en évidenced'une part, l'origine de la salinité des eaux de la dépression piézométrique et d'autre part, les phénomènesd'échanges de bases liés au long temps de séjour des eaux au contact des roches encaissantes et les zones derecharge potentielles de la nappe. / The study of the Chari Baguirmi aquifer system aims to improve the knowledge about this system forsustainable groundwater resource management. In the study area, which covers 70,000 km2, measurementcampaigns and sampling of water and sediments were undertaken. The waters have been sampled for chemicaland isotopic analyzes (18O and 2H) to understand the hydrogeochemical behavior of the aquifer system.The synthesis of existing geological data and highlighting the litho-stratigraphic heterogeneity through thegranulometric study confirmed the hydrogeological complexity of the study area. Clay mineralogy showed thatthe deposition of different sediments occurred from the periphery to the center of the depression. This mode ofsedimentation can hypothesize the existence of a depression into which sediments are trained by the transportagent. This assumption of "structural depression" refutes the hypothesis of a hitherto accepted hydrogeologicalorigin (high evaporation) of the piezometric depression. The study based on the piezometry and chemical and isotopic data (18O and 2H) of water enabled to understand the hydrogeochemical processes that govern the mineralization of the water. In addition to isotopes (2H and 18O), the use of ratios Br/Cl, Sr/Ca and base exchanges index has highlighted on the one hand, the origin of the salinity of waters in the piezometric depression and secondly, the phenomena of base exchanges related to longresidence time of water in contact with rocks and areas of potential groundwater recharge. Numerical modeling of the aquifer was performed in steady state and the results confirm the prevalence of the phenomenon of evaporation in the western p

The Permo-Triassic lower Beaufort Group fluvial deposits extend over 100s of kilometres within the Karoo Basin, South Africa. A detailed study of the depositional architecture and stacking patterns of sand bodies within a 900 m thick succession has enabled interpretation of the controls on ancient river channel and overbank processes. Facies include very fine- to medium-grained sandstone, intra-formational conglomerate, mudstone and palaeosols. Channel-belts are dominated by upper flow regime structures, consistent with a flashy to ephemeral fluvial system. The overbank deposits comprise splays interbedded with purple, green and grey mudstone; these floodplain colour changes signify water table fluctuations. A hierarchy of channel-related elements has been established that recognises beds, bedsets, storeys, channel-belts, complexes and complex sets. Each channel-belt may be single- or multi-storey, whereby one storey represents the complete cut and fill cycle of a single migrating river, comprising bar accretion elements and channel-abandonment fill. The abandonment fill elements often consist of heterolithic plugs of climbing ripple-laminated very fine-grained sandstone, or interbedded claystone with siltstone. The Beaufort channel-belts preserve either lateral- or downstream-accretion patterns, or a combination. Each belt has either a lenticular or tabular geometry, recognisable by an erosional base overlain by intra-formational conglomerate lag and barform deposits. Genetically related channel-belts cluster to form complexes, of which two broad styles have been identified: Type A) laterally and vertically stacked channel-belts, and Type B) sub-vertically stacked channel-belts. There is evidence of localised clustering of sub-vertically stacked channel-belts adjacent to extensive overbank mudstone deposits. The apparent lack of a well-defined ‘container’ surface with mappable margins, suggests that this stacked channel-belt architecture represents an avulsion complex rather than a palaeovalley-fill. The lateral and stratigraphic variability in fluvial-overbank architecture is interpreted as the interplay of several controls. Allogenic forcing factors include, tectonic subsidence that influences accommodation, sediment supply, and high frequency climate cycles associated with the flashy discharge regime and expressed in the mudrock colour changes and distribution of palaeosols. The depositional river style, variability in channel-belt stacking patterns and compensational stacking of some channel-belt/splay complexes is interpreted to be the result of autogenic channel avulsion, supported by an absence of significant erosion. The relative merits of basin-axial trunk river and distributive fluvial system (DFS) models are assessed from detailed architectural and stratigraphic outcrop studies.