Aquitaine Basin - Knowledge

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groundwater helped immensely in unravelling these structures. Similar to the Northern Province, the major structures are again trains of parallel anticlines whose wavelength steadily diminishes approaching the Pyrenean front. Inversely the effects of the salt movements become stronger towards the south. The anticlines were formed during the uplift of the Pyrenees during the Eocene/Oligocene. The structures were set in place by Miocene times. The following anticlines can be distinguished (from north to south):

460: 2249:), was wedged southward. This gave the Atlantic the chance to directly reach the Aquitaine Basin for the first time. In the wake of the southward drifting Iberia during the Lower Cretaceous, the Bay of Biscay opened up. The microcontinent Iberia underwent in addition to its southward drifting motion a counterclockwise rotational movement that eventually brought it in close contact with southern France (reflected in first tectonic movements in the Pyrenees during the 1687: 1358:, a regression commences. After the initial deposition of bioclastic rudist-bearing limestones and the formation of some reef complexes composed of rudists and single corals, the sea level started dropping. Northern Aquitaine became emersed and the sea withdrew in stages southward to the line Arcachon-Toulouse. At the same time, the northern edge of the basin experienced another folding episode with low-amplitude folds striking northwest–southeast. 99: 170: 1783: 1543:-bearing limestones in the northern Médoc and in the Libournais and with mammal-bearing molasses in the Agenais, the sea made a big retreat at the end of the Oligocene. This retreat was accompanied by tectonic movements creating trains of deeper-seated anticlines in the central and northern Aquitaine Basin. The debris-carrying alluvial fans issuing from the rising Pyrenees reached into the 1115:. During the Tithonian, the shrinkage of the basin became even more evident, only to end in a nearly complete withdrawal of the sea from the Aquitaine Plateau before the close of the Tithonian (the south is not affected by this). During the Tithonian, iron-bearing calcareous oolites interbedded with marls, as well as dolomite and border facies deposits develop—dated by 833:) evolving towards a lacustrine facies (green shales, coloured marls, dolomitic limestones and platy limestones rich in dwarf fossils, and evaporitic interlayers). The sediments of the Sinemurian are again fully marine and carry a pelagic fauna (soft banded limestones and hard lithographic limestones). At the end of the Sinemurian, a sudden regression occurred, forming 1583:. Shortly thereafter the sea attained its highstand. It was rimmed completely by continental deposits whose thickness increased towards the southeast. For the first time, the alluvial fans along the Pyrenean front receded, the reason being increased subsidence in front of the orogen; yet they still stretched as far north as the Agenais. 1516:), a regression set in. The Subpyrenean Basin became completely filled with the erosional debris of the rising Pyrenees. In the Médoc, nummulite-bearing marls and limestones were still being laid down, but east of Bordeaux already continental molasses appeared that change farther south into gypsum-bearing formations. 2172:

in the Aquitanian Basin is 36 km, following more or less the path of the Garonne River. Towards the Massif Central in the northeast, the discontinuity flattens out to 30 km. The same holds for approaching the northern edge of the Pyrenees, here the discontinuity is also at 30 km depth.

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develops. At the same time, the sediments on the Aquitaine Plateau farther north are folded into gentle wavetrains following the Hercynian strike (northwest-southeast). All these movements are correlated with the first tectonic stirrings in the Western Pyrenees. Towards the end of the Albian, the sea

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The second sequence of the Malm starts in the Upper Kimmeridgian, only in places does it show regressive traits, nevertheless the sedimentary character changes. Laid down are breccias and the sediments also show synsedimentary reworkings; periodically interbedded limestones and marls carrying lignite

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movements during the Plio-Quaternary at the northeastern edge of the Aquitaine basin lead to an uplift and rejuvenation of the peneplained basement in the Massif Central. In the Aquitaine basin itself, these movements follow already existing basement structures and entrain the tilting of some of the

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follows after a pronounced unconformity. The southern flysch basins began to expand northward. Near Pau before the onset of the flysch sedimentation, a very strong erosion removed the entire Lower Cretaceous, the entire Jurassic and sometimes even cut right down to the basement. North of Pau, the

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with its west-northwest-east-southeast-striking structural grain. The Pyrenean orogen likewise has not merely a compressional origin but also a strong, in this case, sinistral transtensional component. The Pyrenean orogen exerted a very profound influence upon the Aquitaine Basin up to this day,

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is bounded by these transtensional dextral shear zones and can hence be interpreted as an east–west-oriented pull-apart basin. Within the context of the opening of the Bay of Biscay, the Parentis Basin can furthermore be regarded as a failed attempt of the Atlantic to wedge into the continent's

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high ground in between. Compared with the Northern Province its sediments show a pronounced increase in thickness (5,000–11,500 altogether). The Triassic and the Jurassic combined reach 2,000–3,000 , the Lower Cretaceous 500–1,500 m. The Upper Cretaceous can vary between 500 and

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Late Campanian-Maastrichtian phase. This phase enhanced the structures already formed in the Jurassic phase. The following anticlinal ridges, which run more or less parallel to the northeastern basin margin and can be traced for more than 200 km, were being generated (from north to south):

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forms a typical continental shelf region with reduced sedimentation and several periods of emersion (during the entire Lower Cretaceous and during parts of the Upper Cretaceous and the Cenozoic). The basement is rarely encountered deeper than 2,000 m. Triassic and Jurassic together have an

1501:. On the northern flank of the fans, lakes formed, precipitating lacustrine limestones. The detrital sediments with provenance from the meanwhile strongly eroded Massif Central (muds, sands, gravels) then affected only a small fringe zone in the northeast. In the Périgord and in the Quercy, the 1247:

is very unsettled. The flysch sedimentation then continues right through the Upper Cretaceous, mainly interbedded sandstones and shales with some carbonaceous layers were laid down. Towards the end of the Upper Cretaceous, there are signs of the start of a regression and the sea then actually

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The tectonic movements were much more complicated in the Southern Province, having superimposed on them very strong halokinetic motions (salt diapirism). A large part of the formed structures is concealed under Plio-Quaternary detritus. The many exploration wells drilled for hydrocarbons and

1617:, ending with a nearly complete withdrawal from the basin. In areas left behind by the sea in the Armagnac, unfossiliferous sands and muds were deposited. At the same time in the north and in the east, today's river network draining the Massif Central was already being beginning to form. 702:. In the north of the Aquitanian plateau, only a continental Upper Triassic is preserved. In the south, the sediments are marine and show their full development. The Triassic marine transgression probably invaded the southern Aquitaine Basin from the southeast or from the south (from the 2620:

subjecting it not only to more or less north–south-directed compression but also to transtension. The effects were of a penetrative nature—tectonic repercussions of the Pyrenean orogeny can even be seen at the northeastern basin margin in the immediate vicinity of the Massif Central.

706:) via the then still immersed Pyrenean region. The sediments indicate a restricted shallow marine environment with drying-up periods that created evaporites. The Triassic sediments can attain a maximum thickness of 1,000 m and reach as far north as the line Garonne estuary – 1105:. This strongly disturbed depositional environment with a coexistence of open marine facies and muds deposited under reducing conditions in a restrictive setting seems to coincide with a first sedimentary individualisation of the Pyrenean realm. The event has received its name 2606:

farther north also strikes northwest–southeast, but additionally has a distinct dextral wrenching movement. Like the South Armorican Shear Zone, the anticlinal ridges too are affected by similar shearing movements and are not purely compressional in origin. Even the

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Foreland basin megasequence. Eocene till recent. The collision of Iberia with France in the Eocene terminated the transtensional tectonics. The rising orogen of the Pyrenees shed flysch sediments during the Eocene and molasses during the Miocene into the foreland

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Generally the Northern Province is characterised by rather simple structures (syn- and antiforms, low-amplitude fold trains, faults) that follow hercynian, armorican and variscan strike directions. The structures were formed during several tectonic phases:

1301:. At this point, the Upper Cretaceous sea had reached its highstand. This also coincides with a climatic optimum with global average sea-water temperatures around 24 °C compared to today's 13 °C. The Turonian can be subdivided into two parts: 2292:. During the Neocomian nonmarine and shallow-marine clastics and carbonates formed, followed by thick shelf carbonates during the Aptian and Albian. The megasequence ends in the Cenomanian with inversion tectonics along preexisting tensional faults. 800:

towards the end of the Lias and at the beginning of the Dogger the sea had onlapped the basement rocks of the Massif Central and the western Vendée (reaching today's limits) by 30 km. On the Aquitaine Plateau in the north, an interior

1660:. The drainage system of the Garonne already resembled more or less today's pattern, the river avoiding the Miocene gravel accumulations as much as possible and then following between Toulouse, Agen and Bordeaux a weekly subsiding graben. 990:. The reefs are associated with calcareous oolites and mark a high-energy zone. On the shallow shelf-domain east of the reefs, neritic limestones were deposited in the north and dolomites in the south; in the Quercy, even supratidal 2189:

For a better understanding of the geological successions and structures in the Aquitaine Basin, it is important to consider the greater geodynamic setting. Two geodynamic developments are of primordial importance for the basin:

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Tectonic movements are still at work in the Aquitaine Basin today—strong earthquakes in the Pyrenees (with destroyed villages and churches) and somewhat milder tremors near the island of Oléron keep reminding us of that fact.

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The progressive landfall of the Aquitaine Basin proceeded from the northeast and was coupled with an important subaerial erosion. As a consequence several peneplanations were carved out from the detrital alluvial plains:

1219:-Carcassonne. The region of the later formed North Pyrenean Thrust is a decisive facies boundary at this time: to the north, shelf sedimentation continued but to the south rapidly subsiding basins developed into which 1133:

has less pronounced sequences. The Lower Cretaceous sediments are restricted to close to the Pyrenees. Most likely the exchange of ocean water masses was better towards the Tethyan realm than towards the Atlantic.

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farther east). During the Middle and the Upper Oxfordian, marine limestones are laid down which incorporate occasional reefs. The Lower Kimmeridgian sediments are sedimented close to the shore, they bear oysters,

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aeolian deposits. They cover more than a third of the Aquitaine region and can be found mainly in the Médoc and in the Landes. They were deposited during the last two cold stages of the Würm glaciation. The

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Jurassic phase. The resulting structures are mainly of synsedimentary origin and follow variscan strike directions. They profoundly influenced facies distributions and transgressive style during the Upper

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An upper cycle with regressive tendencies. In the northwest, sandy rudist-bearing limestones and oyster-bearing marly shales were deposited; in the northeast, very shallow marine gypsum-bearing shales and

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Postrift megasequence. Cenomanian till Paleocene. Sinistral motions of Iberia relative to France created several transtensional sub-basins (pull-apart structures). Turbidite sedimentation in the south.

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and in places with breccia-bearing detritus. This is followed by neritic limestones precipitated in calm conditions. Yet in the south, dolomites continue to be deposited. The sequence finishes in the

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Structural and sedimentological investigations of the basin have been carried out in over 70 drilled wells that encountered the Variscan basement sometimes below 6,000 m of sedimentary cover.

1211:. In the northern part of the Aquitanian Basin, the Cenomanian sea reclaimed nearly the same areas that had been occupied by the Jurassic sea; in the east, however, it only reached the line Brive- 1141:. During the Lower Cretaceous the Parentis Basin received 2,000 m of sediment and the Adour Basin 4,000 m. The remainder of the Aquitaine Basin is meanwhile subjected to strong erosion. 2245:

about 150 million years ago, a rift arm infiltrated along today's continental margin of northwestern France. Consequently, Iberia, so far being positioned right below the Armorican Massif (

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explorations the Variscan basement hidden under the sediments of the Aquitaine Basin can be subdivided into several northwest–southeast-striking tectono-metamorphic zones (from north to south):

1078:, the first sequence of the Malm seems to follow the Callovian without a distinctive break. Yet cellular limestones and breccias indicate sediment reworking (this was certainly the case in the 1547:

and attained their largest extent. They pushed the surrounding belt of lakes ahead of them (in northerly directions) thereby spreading lacustrine limestones well into the Quercy, onto the

561:, and into a much deeper, tightly folded, southern region. The tabular platform in the north contains only a much reduced sedimentary succession that is gently undulating and occasionally 2432:(manufacture of tiles, bricks, terracotta, etc.). Horizons are found mainly in the Toarcian, in the Eocene (Lutetian), in the Oligocene, and in the Miocene (Aquitanian, Burdigalian, 2638:

Vertebrate paleobiodiversity of the Early Cretaceous (Berriasian) Angeac-Charente Lagerstätte (southwestern France): implications for continental faunal turnover at the J/K boundary

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is calcareous in the northeast, whereas in the southeast it keeps its dolomitic character. The end of the sequence in the Lower Bathonian shows regressive tendencies with lignites,

994:-bearing limestones were formed. In the western domain open towards the Atlantic, the pelagic sediments comprise ammonite-bearing limy marls very rich in filamentous microfossils ( 2285:

Prerift megasequence. Triassic till Upper Jurassic. Mainly clastic sediments and carbonates followed by thick evaporites during the Triassic; shelf carbonates during the Jurassic.

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accumulated sediment thickness of 1,000–1,700 m. The Lower Cretaceous is completely missing and the Upper Cretaceous only reaches a thickness of several hundred metres. The

2141:(and also the North Aquitaine Flexure) and follows the line Arcachon-Agen-Toulouse. It is made up of nappes of the orogen's external zone which were thrust southward during the 1580: 1379:

north of this line, the sediments possess continental character – red mudstones, sands, and lacustrine limestones. The sea made a short-lived advance into this domain and left

892:) marls indicating a shelf environment open to the spreading Atlantic Ocean. During the Lower Domerian, a connection to the Paris Basin is breached for the first time via the 1137:

Sedimentation increased again after a longer hiatus in the Lower Cretaceous, but only in two locales—the Parentis Basin and the Adour Basin. Both sub-basins manifest a huge

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over basement rocks or Permo-Triassic sediments. At that time, the first open-marine sediments (yet rather poor in fossils) were being deposited in the Aquitaine Basin. The

1313:) on the top. It consists of massive, partially brecciated rudist limestones at its base followed by ocre calcareous sands. The resistant Angoumian formed extensive cliffs. 1190:, strong halokinetic movements affect the southern Aquitaine Basin and in turn profoundly influence sedimentation patterns. As a result, breccias, thick conglomerates, and 2603: 2106: 1645: 829:, and fairly thick layers of sand- and mud-stones rich in plant material. The rest of the Hettangian is made up of marine sediments deposited in a restricted environment ( 2277:

By taking as a reference point the onset of rifting in the Bay of Biscay during the Tithonian the geodynamic evolution of the Aquitaine Basin can be subdivided into four

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At the northern edge of the basin, more differentiated coastal facies develop. In the north, the Cenomanian is made up of three sedimentary cycles (from young to old):

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began to grow, splitting the Aquitaine Basin into two major facies domains. Prominent reef complexes are situated east of Angoulême, northwest of Périgueux and east of

901: 1466:) were sedimented in the continental north and northeast. The provenance area of these continental deposits up to Middle Ypresian times was mainly the Massif Central. 1047:

and limestones were deposited, whereas in the eastern domain the sediments are calcareous dolomites. The retreat of the Jurassic sea became noticeable during the late

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A generally deeper marine middle-cycle with marls. These sediments spread into the Quercy. In the Périgord, littoral facies and lignites accumulated near paleohighs.

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In the eastern section, one can discern several low-amplitude structures that are parallel to the Pyrenees farther south and strike west-northwest-east-southeast:

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The first sequence in the Dogger (note: sequences are only distinguished in the eastern shelf-domain) starts transgressing in a restricted environment during the

2152: 2090: 1056: 543: 2155:. It is bounded in the south by the North Pyrenean Thrust Front and is equivalent to the Southern Province. This continental foreland block already belonged to 1017:, and lacustrine fossils in the Quercy. No ammonites are found in the eastern domain right up to the Kimmeridgian—a great handicap for correct dating purposes. 2217:) about 230 million years ago, the supercontinent Pangaea started slowly to break up. In the Atlantic domain, the disintegration began in the area of the 2134: 2112: 1249: 1024: 1721:—are also documented in the Aquitaine Basin, mainly by different levels of river terraces. Additionally amongst glacial phenomena the following can be cited: 897: 2206: 1485:

and eastward into the Agenais. The Subpyrenean Basin deepened and was simultaneously being filled by conglomerates brought in from the east, the so-called

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The Coniacian and the Santonian are expressed as typical chalky limestones in the north, but both stages take on a more sandy character east of Périgueux.

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which is reflected in the sediments of the northeastern Aquitaine Basin as a strong input of detritus, mainly sands in the upper part of the Angoumian.

617: 2616: 2352: 1298: 382: 1172: 943:, the sediments turn into sandy limestones indicating another regression. Interlayered with these sandy limestones are oyster beds, iron oolite and 2344: 1629: 1156: 573: 565:. The folding intensity in the southern region increases steadily towards the south, the structures being further complicated by superimposed salt 444: 1641: 1404: 1412: 870:). They are mainly calcareous and rich in quartz grains and pebbles of reworked Sinemurian. The Upper Carixian consists of very fossiliferous ( 2241:

times, the Central Atlantic was fully marine. Spreading continued and gradually also began to affect the Northern Atlantic domain. During the

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are without doubt of prime importance for the French economy. Major sources are found in the following sub-basins of Lower Cretaceous age:

949: 2530:. Large forests in the Landes and in the Dordogne form the basis for a diversified industry (firewood for power stations and private use, 955: 2265:

uplifting the mountain chain and subjecting it to severe erosion at the same time. The main phase of uplift ended with the close of the

1644:. The alluvial fans restricted their activity to the immediate vicinity of the Pyrenean mountain front and created the alluvial fans of 2173:

In the oceanic part of the Parentis Basin, it is already encountered at 20 km depth. This implies a significant stretching of the

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direction is also followed by the continental edge of northwestern France which formed during the evolution of the Bay of Biscay. The

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Source/host rocks are Jurassic (Kimmeridgian) and Lower Cretaceous limestones and dolomites. Lower Aptian shales function as seals.

2005: 2253:; also documented by metamorphism in the Pyrenees dated between 108 and 93 million years ago and by the transgression of the 478:. Here it meets for 330 km the straight, more or less north–south-trending Atlantic coastline but continues offshore to the 91: 431:, occupying a large part of the country's southwestern quadrant. Its surface area covers 66,000 km onshore. It formed on 2730: 2571:

The structural and hence sedimentary organisation in the Aquitaine Basin was ultimately influenced by two principal factors:

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an aquitanian, strongly silicified peneplain. This is very well developed in the Périgord, in the Agenais, and in the Quercy.

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mineralisations occurring in the basal Sinemurian. Found in the Charente and near Figeac, yet economically no longer viable.

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Synrift megasequence. Lower Cretaceous (Tithonian till Albian). The Bay of Biscay opened and became partially underlain by

2510:. Contained within the Eocene age Sidérolithique, mainly in the Périgord and in the Quercy. Economically no longer viable. 1810:. This fault zone extends from Arcachon to Carcassonne and represents the continuation of the continental slope onshore. 1163:, marine shallow-water carbonates were precipitated, changing to detritic sediments in the northern Parentis Basin. Near 2586:

in the basement has profoundly influenced the structural and the sedimentary evolution of the Aquitaine Basin. The same

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and a switch-over in detritus provenance from the Massif Central in the north to the Pyrenees in the south. Coalescing

1450:-rich marls and limestones were formed. The newly inundated areas receive sands and limestones rich in alveolinids and 297: 2711: 2693: 2675: 2657: 1535:-bearing limestones of the southern Médoc are lagoonal deposits. After a short-lived advance at the beginning of the 189: 65: 43: 36: 2378:. With its 220 billion cubic meters of gas, the Adour Basin stocks practically all the gas reserves of France. 920:

facies rocks can change into iron-rich oolites along their margins. The sequence finishes again with hardgrounds.

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is, if present, very thin in the north but increases in thickness towards the south where it is overlain by thin

1059:, extremely littoral sediments in the Quercy, lacustrine limestones in the Parentis Basin, and anhydrites in the 122: 2221:. Already in the Lower Jurassic, the initial rifting process had given way to the marine drifting stage. In the 1293:

A shallow marine lower-cycle with rudist reefs in the northwest and continent-derived lignites in the northeast.

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Eocene-Oligocene phase. More anticlines at a deeper level that are not detectable at the surface were created:

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microfauna were deposited. In the rest of the Aquitaine Basin, continental sands were laid down, the so-called

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attains a maximum thickness of about 300 m along a north–south-trending zone running from Angoulême to

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interior. The reason for this is the counterclockwise rotational motion of Iberia blocked further rifting.

1571:). Marine, littoral, and lacustrine facies interchange. During a minor regression, a huge lake formed near 1228: 115: 1798:

and a calcite-filled pull-apart. Thus the anticline was also affected by transtensional wrenching motions.

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a pliocene (zanclean) peneplain, characterised by gravel-bearing clays in the Bordelais and in the Landes.

821:. On this shelf the generally detritic transgression sediments of the Hettangian normally comprise a base 2455: 2066:

pliocene peneplains. This in turn has a strong effect upon the hydrographic network, for example in the

1343:. In the northern Aquitaine Basin, the sediments become more homogenised and settle out as fully marine 2740: 1910: 966:) begun in the Triassic carries on right through the Lias; it reaches a thickness of up to 500 m. 904:. During the Upper Domerian, another regression sets in leaving sandy limestones very rich in fossils ( 638:

Sedimentation started in the very south of the Aquitaine Basin during the Lower Triassic with coloured

1873:. This structure is an asymmetric anticline near Mareuil, becoming a high-offset normal fault between 660:

and coloured mudstones. During the Upper Triassic evaporites continued being precipitated, crowned by

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and also reaches 11 km depth; it is a symmetrical basin oriented east–west and comes ashore near

2169: 1888:. It forms a typical anticline near La Tour-Blanche. Near Saint-Cyprien, it is mainly a normal fault. 1395:, deep water conditions prevailed in the west, shallowing out towards the east. The sediments in the 2735: 2450:. Mainly found in residual pockets of Eocene age filling depressions and caves in Upper Cretaceous 2356: 1527:), a permanently marine environment persists in the south with marls and sands rich in nummulites, 511: 386: 293: 30: 927:

without any detrital deposits at its base, the sediments being black ammonite-bearing marls (with

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The entirely marine Jurassic cycle can be subdivided into seven second-order sequences bounded by

2142: 1145: 777: 680: 482:. To the south, it is delimitated for 350 km by the west-northwest–east-southeast trending 1746: 906: 876:) marly limestone layers interlayered with grey marls. These are followed by ammonite-bearing ( 822: 47: 2181:. As a comparison, underneath the Central Pyrenees the continental crust is 50 km thick. 1416: 1900: 1874: 1770:

finds and their sites in the Aquitaine Basin merit mentioning, especially in the Département

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Structurally the Aquitaine Basin can be divided into two provinces separated by a prominent

1477:). The area covered by alveolinid- and nummulite-bearing limestones increased, northward to 1183:. The Urgonian facies completely surrounds the Parentis Basin and persists into the Albian. 962:

In the southern part of the Aquitanian basin, the evaporite deposition (including layers of

2015: 1609:) witnessed a drastic withdrawal of the sea to the west. This process started first in the 793: 510:. The northeastern boundary of the basin is formed by the arcuate basement outcrops of the 1267:

facies) are sedimented during the Upper Cretaceous, including the type localities for the

1063:. The seaways that had opened in the Lias closed again and a single reef persisted in the 630:

close to the North Pyrenean Thrust. From here, it slowly started spreading farther north.

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farther north. It forms the polymetamorphic core region of the Variscan orogen in Europe.

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The second sequence of the Lias again is marine-transgressive and commences during the

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River and divides the basin into a relatively shallow northern platform, the so-called

345: 185: 2640:. Geodiversitas, Museum National d’Histoire Naturelle Paris, In press. ffhal-03264773f 1718: 687:

horizons along which Triassic sediments were squeezed northwards to the line Arcachon–

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3,000 m and even the Neogene still attains a thickness of nearly 1,000 m.

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The transgression that began in the late Albian spread rapidly northward during the

522:. In the far north, the basin abuts the east–west-oriented Variscan basement of the 2636:

Ronan Allain, Romain Vullo, Lee Rozada, Jérémy Anquetin, Renaud Bourgeais, et al..

2348: 2317: 1937: 1411:. Near the Petits Pyrénées, the sediments change into shallow-water facies rich in 1199:

level is rising and the Urgonian calcareous reefs are consequently draped by muds.

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The geological provinces of France, the Aquitaine Basin on the lower left hand side

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affecting the sedimentary cover is also arranged in this direction. The prominent

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of the Garonne and Adour, the rivers' courses were changed or entirely abandoned.

1840: 1803: 1714: 1325: 1096: 1068: 1006: 893: 727: 647: 597: 562: 515: 321: 2497: 2367: 2067: 1881: 1079: 1040: 784:, as it is also called, started to encroach on the entire Aquitaine during the 731: 661: 539: 495: 475: 391: 338: 326: 314: 250: 242: 459: 2724: 2289: 2230: 2226: 2199: 2128: 1528: 1400: 1355: 1297:

The Turonian reflects a transgressive period with the sea spreading into the

917: 797: 585: 137: 124: 1930: 1442:; in the southeast it even reached the Montagne Noire. In the Aturian Gulf, 2375: 2329: 2178: 1795: 1794:; east-southeast-west-northwest-oriented strike-slip fault with horizontal 1678:

On the pliocene peneplain, today's drainage system was firmly established.

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The retreat of the alluvial fans also continued during the Middle Miocene (

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became established in both sub-basins—fossiliferous limestones composed of

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which extends out into the Atlantic. The Parentis Basin is situated in the

507: 451:—both sub-basins of the main Aquitaine Basin—by 11,000 m of sediment. 399: 361: 1310: 814: 810: 2608: 2465: 2391: 2336: 2225:

about 180 million years ago, the Central Atlantic was spreading and

2043: 1703: 1695: 1691: 1101: 806: 764:; farther south, e.g. in the Subpyrenean Basin, the cycle has many gaps. 741:

Lotharingian-Carixian-Domerian sequence (Upper Sinemurian–Pliensbachian).

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Since the Cenomanian, the Aquitaine Basin is under the influence of the

1563:, the sea began transgressing towards the north and the east during the 1064: 572:

This somewhat simplified structural subdivision gets complicated by the

2447: 2401:. Recently a gigantic aquifer has been discovered in Eocene sands near 2254: 2083: 2025: 1767: 1726: 1686: 1657: 1513: 1459: 1447: 1236: 1208: 1149: 1138: 1130: 1084: 935: 929: 785: 773: 723: 589: 499: 2359:. The Parentis Basin contains most oil reserves of continental France. 1896: 1023:

The second sequence in the Dogger begins in the Middle Bathonian with

2501: 2443: 2437: 2402: 2262: 2242: 2238: 2102: 2033: 2009: 1997: 1903:

anticline. This structure is an anticline near Jonzac and Sauveterre.

1823: 1791: 1606: 1602: 1532: 1520: 1474: 1451: 1387:(northern half of the southern basin), a shelf built out to the line 1380: 1372: 1335: 1276: 1272: 1268: 1253: 1244: 1191: 1160: 1048: 1028: 1010: 963: 878: 872: 861: 853: 672: 654: 650: 639: 566: 471: 373: 157: 1976:

is characterised by the deep Parentis and Adour sub-basins with the

1439: 1375:, the coastline roughly followed the line Arcachon-Toulouse. In the 1263:

In the remainder of the Aquitaine Basin, mainly pelagic limestones (

1248:

retreats before the K/T boundary. In the Subpyrenean Basin near the

1155:

The first deposits in the two sub-basins were littoral sediments in

1095:

horizons begin to form. The sediments can be dated by the ammonites

523: 2555: 2531: 2487: 2469: 2433: 2421: 2398: 2246: 2222: 2156: 2124: 2115:. The zone is bounded on the south by the line La Rochelle-Saintes- 2077: 2062: 1959: 1906: 1771: 1738: 1633: 1625: 1621: 1614: 1610: 1587: 1536: 1524: 1506: 1470: 1434:), another transgressive period saw the sea advance north into the 1431: 1388: 1240: 1232: 1002: 995: 940: 924: 888: 849: 688: 668: 643: 627: 581: 503: 483: 440: 432: 417: 413: 354: 350: 260: 246: 203: 199: 2559: 2001: 1579:, in which grey lacustrine-limestones precipitated, the so-called 1435: 1320:(Latin name for the Massif Central) at the base—wavy chalky marls. 2493: 2475: 2394: 2371: 2214: 2195: 1990: 1977: 1963: 1941: 1926: 1885: 1846: 1827: 1787: 1760: 1706: 1653: 1649: 1637: 1594:). Consequently, the lacustrine band reached as far south as the 1564: 1548: 1544: 1540: 1463: 1455: 1348: 1111: 1014: 991: 975: 866: 699: 620:

are considered to belong to the basement of the Massif Central.)

554: 550: 542:. It reaches its deepest part of 11 km just in front of the 474:, is roughly funnel-shaped with its opening pointing towards the 436: 395: 333: 283: 207: 2198:

and the opening history of the Northern Atlantic (and hence the

1782: 1324:

Towards the end of the Turonian, the Massif Central experienced

1020:

The Pyrenean realm meanwhile is characterised by a long hiatus.

2537: 2258: 2250: 2234: 2037: 2019: 1914: 1892: 1742: 1427: 1257: 1220: 1212: 1187: 1180: 1168: 1148:

is a major fossil deposit in the Aquitane Basin, dating to the

979: 944: 883: 830: 826: 818: 789: 761: 676: 657: 626:

The sedimentary evolution in the Aquitaine Basin begins in the

424: 175: 2269:, followed mainly by isostatic movements lasting to this day. 1763:

estuary goes back about 20,000 years into the late Würm.

1399:(Golfe Aturién) in the west are pelagic limestones containing 1231:, the flysch sediments are even accompanied by volcanic rocks— 698:

in character, i.e. very similar to the Triassic succession in

2513: 2451: 2429: 2098: 2094: 1880:

The Périgueux anticline. This structure can be followed from

1478: 1344: 1264: 1216: 1176: 707: 939:). Towards the end of the Toarcian and the beginning of the 896:

and also to the Jurassic sea of southeastern France via the

753:

Oxfordian–Sequanian sequence (Oxfordian–Lower Kimmeridgian).

2702:

Winnock E. (1996). Bassin d'Aquitaine. Contribution in the

2551: 2541: 2527: 2521: 2517: 2507: 2461: 2425: 2417: 2051: 1734: 1423:, the sediments become totally continental and lacustrine. 1164: 1071:. In the end, the sea withdrew south of the Garonne River. 1044: 983: 923:

The third and last sequence of the Lias sets in during the

756:

Kimmeridgian–Portlandian sequence (Kimmeridgian-Tithonian).

664: 2554:. World-famous wines like the Cognac, Bordeaux, Armagnac, 2163: 2584:

northwest-southeast-striking tectono-metamorphic zonation

2332: 1239:

lavas. The sedimentation in the flysch basins during the

584:. This sub-basin is underlain on its far western side by 2650:

Carte géologique de la France à l'échelle du millionème.

2397:

are found in Upper Cretaceous and Cenozoic rocks of the

2123:. It is composed of southward-thrust basement nappes of 1777: 2328:

Amongst the many resources in the Aquitaine Basin, the

2575:

By structural inheritance from the Variscan basement.

1737:

parallel to the Atlantic shoreline formed during the

959:. The sequence ends with an erosional unconformity. 760:

The complete Jurassic cycle is only preserved in the

1469:

The sea-level kept rising during the Middle Eocene (

1043:. In the western domain, initially ammonite-bearing 1454:. Meanwhile, iron-rich sands (in the Charente) and 788:, characterised by calcareous-dolomitic, partially 2446:. This is the raw material for the manufacture of 2405:—of great importance for the region Pau-Toulouse. 1725:cave infills. These are very important for dating 1628:), the sea occupied merely a small strip near the 1446:-bearing marls were deposited, while farther east 1415:, echinids, and operculinids. Farther east in the 2722: 2078:Tectono-metamorphic organisation of the basement 1925:Northeast-southwest-striking domal upwarps near 1039:The facies dividing reef-zone persists into the 518:in the northeast, the basin is connected to the 2093:. The zone is limited on the south by the line 2534:, palettes, timber, furniture industry, etc.). 2257:sea). The final collision happened during the 2137:. Its southern boundary is identical with the 1505:accumulated—iron-rich sediments that resemble 1167:, they change to lagoonal anhydrites. In the 2424:. They are the raw material for innumerable 1194:are shed. In the Parentis Basin, a distinct 467:The Aquitaine Basin, named after the French 2648:Chantraine J, Autran A, Cavelier C, et al. 1936:The northwest–southeast-striking upwarp of 1698:. The first representation of a human face. 1159:, mainly sandstones and shales. During the 1559:Following its retreat in the southwestern 1491:beginning of uplift in the Pyrenean orogen 1227:) from the Pyrenean realm were shed. Near 675:). The evaporites were later activated as 486:. In the southeast, the basin reaches the 435:basement which was peneplained during the 2482:; Upper Miocene/Pliocene deposits in the 1752:colluvium masking hillsides and hilltops. 805:was constructed as far south as the line 646:, followed during the Middle Triassic by 538:The Aquitaine Basin is a very asymmetric 106:Location of the Aquitaine Basin in France 66:Learn how and when to remove this message 2594:finds its prolongation in the superdeep 2578:By the evolution of the Pyrenean orogen. 2472:horizons in the Médoc (Gironde estuary). 2307: 1781: 1685: 1252:, the sea lingers on till the lowermost 458: 439:and then started subsiding in the early 29:This article includes a list of general 2385: 2164:Depths of the Mohorovicic Discontinuity 1009:. In places, Aalenian is reworked. The 588:dated at 100–95 million years BP ( 553:follows more or less the course of the 270:66,000 km (25,000 sq mi) 98: 2723: 2688:Guides géologiques régionaux. Masson. 2670:Guides géologiques régionaux. Masson. 1031:with littoral border-facies deposits. 612:(Note: Permo-Triassic basins like the 506:, the basin is overridden by Pyrenean 2184: 1884:via La Tour-Blanche to Périgueux and 1778:Structural organisation and tectonics 1129:In comparison with the Jurassic, the 848:. The sediments can be well dated by 2496:. In Jurassic karst pockets between 2205:The movements of the microcontinent 1950:The east–west-striking anticline of 1551:, and even onto the Massif Central. 947:layers; they contain ammonites like 750:Middle Bathonian–Callovian sequence. 15: 2413:Further notable resources include: 1391:-Carcassonne. Farther south in the 1383:-bearing limestones behind. In the 1339:Campanian is a marly facies called 1202: 1124: 1051:with dolomites and breccias in the 13: 2408: 1509:indicating a subtropical climate. 747:Bajocian–Lower Bathonian sequence. 533: 35:it lacks sufficient corresponding 14: 2752: 2666:Gèze B & Cavaillé A. (1977). 2630: 2562:are grown in the Aquitaine Basin. 502:range in the south. Just west of 443:. The basement is covered in the 366: 2454:developments. For example, near 2272: 168: 97: 90: 20: 2323: 738:Hettangian-Sinemurian sequence. 607: 526:, the southernmost part of the 298:Étang de Cazaux et de Sanguinet 2566: 1636:. Sandy shales very rich in a 1223:sediments (and partially also 776:-Sinemurian sequence is fully 1: 2623: 2151:, also called microcontinent 1681: 498:on its northern side and the 2731:Sedimentary basins of Europe 2303: 1905:Between the anticlines are 1755:creeping cryoclastic debris. 1366: 694:The sediments are typically 683:and the mudstones served as 600:) and probably represents a 592:). It is bounded by dextral 454: 7: 2478:. In the Cenomanian of the 2312:Oil pumping station on the 2139:South Variscan Thrust Front 1361: 792:sediments. Despite smaller 744:Toarcian-Aalenian sequence. 713: 633: 514:. Via the 100 km wide 10: 2757: 2604:South Armorican Shear Zone 2504:. Economically not viable. 2107:South Armorican Shear Zone 1581:Calcaire gris de l'Agenais 1554: 2704:Encyclopaedia Universalis 2170:Mohorovicic Discontinuity 2168:The maximum depth of the 1871:Mareuil-Meyssac Anticline 1790:from the La Tour-Blanche 1512:During the Upper Eocene ( 1497:built out north into the 969: 372: 360: 344: 332: 320: 308: 303: 289: 279: 274: 266: 256: 230: 222: 217: 195: 181: 163: 153: 114: 85: 80: 2105:running parallel to the 1179:, coralline polyps, and 261:Pyrenean foreland basins 2281:(somewhat simplified): 2213:In the Upper Triassic ( 1808:North Aquitaine Flexure 1759:The development of the 1186:Since the onset of the 1146:Angeac-Charente bonebed 1034: 767: 50:more precise citations. 2686:Aquitaine occidentale. 2320: 1947:The Bordeaux syncline. 1929:, near Blaye and near 1799: 1747:The Great Dune of Pyla 1699: 1487:Poudingues de Palassou 1385:Central Aquitaine Zone 902:Détroit de Carcassonne 879:Amaltheus margaritatus 464: 412:is the second largest 2486:are strip-mined near 2311: 2177:and the beginning of 2119:and pinches out near 2091:Ligero-arvernian Zone 1901:Sauveterre-la-Lemance 1785: 1689: 1118:Gravesia portlandicum 1102:Aspidoceras orthocera 1025:lacustrine limestones 930:Harpoceras falciferum 544:North Pyrenean Thrust 462: 294:Lac d'Hourtin-Carcans 2684:Vigneaux M. (1975). 2668:Aquitaine orientale. 2386:Groundwater aquifers 2237:were separating. By 2135:North Aquitaine Zone 2113:South Armorican Zone 1806:zone, the so-called 1668:an eocene peneplain. 1531:, and echinids. The 1393:South Aquitaine Zone 1377:North Aquitaine Zone 1347:-bearing calcareous 1055:, evaporites in the 907:Pleuroceras spinatum 873:Aegoceras capricornu 2314:Étang de Biscarosse 1601:The Upper Miocene ( 1225:wildflysch breccias 1171:, the reef-forming 950:Pleydellia aalensis 134: / 2366:. Gas is found in 2347:. Oil is found in 2321: 2185:Geodynamic setting 1852:Toulouse antiform. 1800: 1786:Lower Portlandian 1766:Finally, the rich 1700: 1489:. This marked the 982:. Along this zone 956:Leioceras opalinum 936:Hildoceras bifrons 913:Pecten aequivalvis 782:Lias Transgression 492:Seuil du Lauragais 465: 186:Nouvelle-Aquitaine 2741:Geology of France 2600:anticlinal ridges 2596:Subpyrenean Basin 2175:continental crust 2159:'s northern edge. 1974:Southern Province 1962:-Miramont in the 1849:graben structure. 1819:Aquitaine Plateau 1815:Northern Province 1696:Upper Paleolithic 1279:in the Charente. 578:Golfe de Gascogne 559:Aquitaine Plateau 549:The 2,000 m 488:Seuil de Naurouze 480:continental slope 449:Subpyrenean Basin 421:sedimentary basin 406: 405: 76: 75: 68: 2748: 2717: 2699: 2681: 2663: 2641: 2634: 2617:Pyrenean orogeny 2598:. The system of 2592:continental edge 2544:in the Agenais ( 2318:Parentis-en-Born 2219:Central Atlantic 2194:The break-up of 1421:Corbières Massif 1203:Upper Cretaceous 1125:Lower Cretaceous 1109:from the oyster 898:Détroit de Rodez 889:Gryphaea cymbium 867:Uptonia jamesoni 681:Pyrenean orogeny 602:pull-apart basin 598:transform faults 528:Armorican Massif 235:Armorican Massif 174: 172: 171: 149: 148: 146: 145: 144: 139: 138:44.267°N 0.167°W 135: 132: 131: 130: 127: 101: 100: 94: 78: 77: 71: 64: 60: 57: 51: 46:this article by 37:inline citations 24: 23: 16: 2756: 2755: 2751: 2750: 2749: 2747: 2746: 2745: 2736:Foreland basins 2721: 2720: 2715: 2697: 2679: 2661: 2645: 2644: 2635: 2631: 2626: 2569: 2430:brick factories 2411: 2409:Other resources 2388: 2326: 2306: 2275: 2187: 2166: 2149:Aquitaine block 2080: 2068:drainage basins 1904: 1841:Tarn-et-Garonne 1837:Quercy synform. 1780: 1702:The three last 1684: 1557: 1521:Lower Oligocene 1369: 1364: 1250:Petits Pyrénées 1243:and during the 1205: 1173:Urgonian facies 1127: 1112:Exogyra virgula 1097:Aulacostephanus 1076:Lower Oxfordian 1069:La Tour-Blanche 1037: 972: 894:Seuil du Poitou 770: 730:and two in the 722:, three in the 716: 636: 610: 536: 534:Basin structure 516:Seuil du Poitou 457: 410:Aquitaine Basin 390: 218:Characteristics 169: 167: 142: 140: 136: 133: 128: 125: 123: 121: 120: 110: 109: 108: 107: 104: 103: 102: 81:Aquitaine Basin 72: 61: 55: 52: 42:Please help to 41: 25: 21: 12: 11: 5: 2754: 2744: 2743: 2738: 2733: 2719: 2718: 2700: 2682: 2664: 2652:(1996). BRGM. 2643: 2642: 2628: 2627: 2625: 2622: 2580: 2579: 2576: 2568: 2565: 2564: 2563: 2549: 2546:Pruneau d'Agen 2535: 2525: 2511: 2505: 2491: 2473: 2459: 2441: 2410: 2407: 2387: 2384: 2380: 2379: 2368:Lacq gas field 2360: 2345:Parentis Basin 2325: 2322: 2305: 2302: 2301: 2300: 2296: 2293: 2286: 2274: 2271: 2211: 2210: 2203: 2186: 2183: 2165: 2162: 2161: 2160: 2146: 2132: 2110: 2079: 2076: 2060: 2059: 2048:Sainte-Suzanne 2041: 2023: 2013: 1994: 1970: 1969: 1968: 1967: 1948: 1945: 1934: 1920: 1919: 1918: 1889: 1878: 1863: 1854: 1853: 1850: 1844: 1838: 1779: 1776: 1757: 1756: 1753: 1750: 1745:largest dune, 1741:. It contains 1730: 1683: 1680: 1676: 1675: 1672: 1669: 1630:Arcachon Basin 1577:Lac de Saucats 1556: 1553: 1529:lamellibranchs 1503:Sidérolithique 1368: 1365: 1363: 1360: 1322: 1321: 1316:The so-called 1314: 1305:The so-called 1295: 1294: 1291: 1288: 1204: 1201: 1157:Wealden facies 1126: 1123: 1080:Grands Causses 1036: 1033: 971: 968: 925:Lower Toarcian 769: 766: 758: 757: 754: 751: 748: 745: 742: 739: 720:unconformities 715: 712: 635: 632: 628:Lower Triassic 618:Grésigne Basin 609: 606: 574:Parentis Basin 540:foreland basin 535: 532: 512:Massif Central 496:Montagne Noire 494:) between the 476:Atlantic Ocean 456: 453: 445:Parentis Basin 404: 403: 376: 370: 369: 364: 358: 357: 351:Early Triassic 348: 342: 341: 336: 330: 329: 324: 318: 317: 315:Foreland basin 312: 306: 305: 301: 300: 291: 287: 286: 281: 277: 276: 272: 271: 268: 264: 263: 258: 254: 253: 251:Atlantic Ocean 243:Massif Central 232: 228: 227: 224: 220: 219: 215: 214: 197: 193: 192: 183: 179: 178: 165: 161: 160: 155: 151: 150: 143:44.267; -0.167 118: 112: 111: 105: 96: 95: 89: 88: 87: 86: 83: 82: 74: 73: 28: 26: 19: 9: 6: 4: 3: 2: 2753: 2742: 2739: 2737: 2734: 2732: 2729: 2728: 2726: 2713: 2712:2-85229-290-4 2709: 2705: 2701: 2695: 2694:2-225-41118-2 2691: 2687: 2683: 2677: 2676:2-225-44935-X 2673: 2669: 2665: 2659: 2658:2-7159-2128-4 2655: 2651: 2647: 2646: 2639: 2633: 2629: 2621: 2618: 2613: 2610: 2605: 2601: 2597: 2593: 2589: 2585: 2577: 2574: 2573: 2572: 2561: 2557: 2553: 2550: 2547: 2543: 2539: 2536: 2533: 2529: 2526: 2523: 2519: 2515: 2512: 2509: 2506: 2503: 2499: 2495: 2492: 2489: 2485: 2481: 2477: 2474: 2471: 2467: 2463: 2460: 2457: 2453: 2449: 2445: 2442: 2439: 2435: 2431: 2427: 2423: 2419: 2416: 2415: 2414: 2406: 2404: 2400: 2396: 2393: 2383: 2377: 2373: 2369: 2365: 2361: 2358: 2354: 2350: 2346: 2342: 2341: 2340: 2338: 2334: 2331: 2319: 2315: 2310: 2297: 2294: 2291: 2290:oceanic crust 2287: 2284: 2283: 2282: 2280: 2279:megasequences 2273:Megasequences 2270: 2268: 2264: 2260: 2256: 2252: 2248: 2244: 2240: 2236: 2232: 2231:South America 2228: 2227:North America 2224: 2220: 2216: 2208: 2204: 2201: 2200:Bay of Biscay 2197: 2193: 2192: 2191: 2182: 2180: 2176: 2171: 2158: 2154: 2150: 2147: 2144: 2143:Pennsylvanian 2140: 2136: 2133: 2130: 2129:Carboniferous 2126: 2122: 2118: 2114: 2111: 2108: 2104: 2100: 2096: 2092: 2089: 2088: 2087: 2085: 2082:According to 2075: 2071: 2069: 2064: 2057: 2053: 2049: 2045: 2042: 2039: 2035: 2031: 2027: 2024: 2021: 2017: 2014: 2011: 2007: 2003: 1999: 1995: 1992: 1988: 1987: 1986: 1982: 1979: 1975: 1965: 1961: 1957: 1953: 1949: 1946: 1943: 1939: 1938:Sainte-Hélène 1935: 1932: 1928: 1924: 1923: 1921: 1916: 1912: 1908: 1902: 1898: 1894: 1890: 1887: 1886:Saint-Cyprien 1883: 1879: 1876: 1872: 1868: 1867: 1864: 1860: 1859: 1858: 1851: 1848: 1845: 1842: 1839: 1836: 1835: 1834: 1831: 1829: 1825: 1820: 1816: 1811: 1809: 1805: 1797: 1793: 1789: 1784: 1775: 1773: 1769: 1764: 1762: 1754: 1751: 1748: 1744: 1740: 1736: 1731: 1728: 1727:archeological 1724: 1723: 1722: 1720: 1716: 1712: 1708: 1705: 1697: 1693: 1690:The Venus of 1688: 1679: 1673: 1670: 1667: 1666: 1665: 1661: 1659: 1655: 1651: 1647: 1643: 1642:Sables fauves 1639: 1635: 1631: 1627: 1623: 1618: 1616: 1612: 1608: 1604: 1599: 1597: 1593: 1589: 1584: 1582: 1578: 1574: 1570: 1566: 1565:Lower Miocene 1562: 1552: 1550: 1546: 1542: 1538: 1534: 1530: 1526: 1522: 1517: 1515: 1510: 1508: 1504: 1500: 1496: 1495:alluvial fans 1492: 1488: 1484: 1480: 1476: 1472: 1467: 1465: 1461: 1457: 1453: 1449: 1445: 1441: 1438:and south of 1437: 1433: 1429: 1424: 1422: 1418: 1414: 1410: 1406: 1402: 1401:globigerinids 1398: 1394: 1390: 1386: 1382: 1378: 1374: 1359: 1357: 1356:Maastrichtian 1352: 1350: 1346: 1342: 1337: 1332: 1329: 1327: 1319: 1315: 1312: 1309:(named after 1308: 1304: 1303: 1302: 1300: 1292: 1289: 1285: 1284: 1283: 1280: 1278: 1274: 1270: 1266: 1261: 1259: 1255: 1251: 1246: 1242: 1238: 1234: 1230: 1229:Saint-Gaudens 1226: 1222: 1218: 1214: 1210: 1200: 1197: 1193: 1189: 1184: 1182: 1178: 1174: 1170: 1166: 1162: 1158: 1153: 1151: 1147: 1142: 1140: 1135: 1132: 1122: 1120: 1119: 1114: 1113: 1108: 1104: 1103: 1098: 1092: 1090: 1086: 1081: 1077: 1072: 1070: 1066: 1062: 1058: 1054: 1050: 1046: 1042: 1032: 1030: 1026: 1021: 1018: 1016: 1012: 1008: 1004: 999: 997: 993: 989: 985: 981: 977: 967: 965: 960: 958: 957: 952: 951: 946: 942: 938: 937: 932: 931: 926: 921: 919: 915: 914: 909: 908: 903: 899: 895: 891: 890: 885: 881: 880: 875: 874: 869: 868: 863: 859: 855: 851: 847: 843: 838: 836: 832: 828: 824: 820: 816: 812: 808: 804: 799: 798:Pliensbachian 795: 791: 787: 783: 779: 778:transgressive 775: 765: 763: 755: 752: 749: 746: 743: 740: 737: 736: 735: 733: 729: 726:, two in the 725: 721: 711: 709: 705: 701: 697: 692: 690: 686: 682: 678: 674: 670: 666: 663: 659: 656: 652: 649: 645: 641: 631: 629: 624: 621: 619: 615: 605: 603: 599: 595: 594:wrench faults 591: 587: 586:oceanic crust 583: 579: 575: 570: 568: 564: 560: 556: 552: 547: 545: 541: 531: 529: 525: 521: 517: 513: 509: 505: 501: 497: 493: 490:(also called 489: 485: 481: 477: 473: 470: 461: 452: 450: 446: 442: 438: 434: 430: 426: 422: 419: 415: 411: 401: 397: 393: 388: 384: 380: 377: 375: 371: 368: 365: 363: 359: 356: 352: 349: 347: 343: 340: 337: 335: 331: 328: 325: 323: 319: 316: 313: 311: 307: 302: 299: 295: 292: 288: 285: 282: 278: 273: 269: 265: 262: 259: 255: 252: 248: 244: 240: 236: 233: 229: 225: 221: 216: 213: 209: 205: 201: 198: 194: 191: 187: 184: 180: 177: 166: 162: 159: 156: 152: 147: 119: 117: 113: 93: 84: 79: 70: 67: 59: 49: 45: 39: 38: 32: 27: 18: 17: 2703: 2685: 2667: 2649: 2632: 2614: 2599: 2591: 2587: 2583: 2581: 2570: 2545: 2412: 2389: 2381: 2376:Saint-Marcet 2330:hydrocarbons 2327: 2324:Hydrocarbons 2276: 2218: 2212: 2188: 2179:oceanisation 2167: 2148: 2138: 2081: 2072: 2061: 1983: 1973: 1971: 1877:and Meyssac. 1855: 1832: 1818: 1814: 1812: 1807: 1801: 1765: 1758: 1701: 1677: 1662: 1619: 1600: 1592:Serravallian 1585: 1576: 1558: 1518: 1511: 1490: 1483:Saint-Palais 1468: 1444:Globorotalia 1428:Lower Eocene 1425: 1413:madreporians 1405:operculinids 1397:Aturian Gulf 1396: 1392: 1384: 1376: 1370: 1353: 1340: 1333: 1330: 1323: 1317: 1306: 1296: 1281: 1262: 1224: 1206: 1196:unconformity 1185: 1169:Upper Aptian 1154: 1143: 1136: 1128: 1116: 1110: 1106: 1100: 1093: 1089:ripple marks 1073: 1038: 1022: 1019: 1000: 973: 961: 954: 948: 934: 928: 922: 911: 905: 887: 877: 871: 865: 858:Oxynoticeras 845: 842:Lotharingian 841: 839: 823:conglomerate 781: 771: 759: 717: 695: 693: 637: 625: 622: 611: 608:Stratigraphy 571: 558: 548: 537: 491: 466: 409: 407: 400:Saint-Marcet 367:Stratigraphy 362:Stratigraphy 62: 53: 34: 2716:(in French) 2698:(in French) 2680:(in French) 2662:(in French) 2609:Paris Basin 2582:The strong 2567:Conclusions 2466:Pleistocene 2392:groundwater 2364:Adour Basin 2097:-Angoulême- 2084:geophysical 2044:Peyrehorade 1956:Villagrains 1891:The Oléron- 1862:Cretaceous. 1796:slickolites 1768:prehistoric 1704:Pleistocene 1692:Brassempouy 1620:During the 1613:and in the 1519:During the 1462:and in the 1419:and in the 1409:alveolinids 1371:During the 1354:During the 1053:Adour Basin 835:hardgrounds 807:La Rochelle 796:during the 794:regressions 696:germanotype 685:decollement 679:during the 614:Brive Basin 520:Paris Basin 447:and in the 429:Paris Basin 239:Paris Basin 223:On/Offshore 141: / 116:Coordinates 56:August 2017 48:introducing 2725:Categories 2624:References 2456:Les Eyzies 2267:Aquitanian 2255:Cenomanian 2026:Saubrigues 2018:-Audignan- 1931:Couquèques 1682:Quaternary 1658:Lannemezan 1569:Aquitanian 1514:Priabonian 1460:Libournais 1452:nummulites 1448:turritella 1237:ultrabasic 1209:Cenomanian 1192:turbidites 1150:Berriasian 1139:subsidence 1131:Cretaceous 886:-bearing ( 786:Sinemurian 774:Hettangian 772:The basal 673:tholeiites 651:limestones 640:sandstones 596:(possible 590:Cenomanian 500:Mouthoumet 427:after the 310:Basin type 231:Boundaries 31:references 2588:hercynian 2516:. Mainly 2502:Lavelanet 2480:Sarladais 2444:Kaolinite 2438:Tortonian 2422:mudstones 2403:Lussagnet 2399:Bordelais 2304:Resources 2263:Oligocene 2243:Tithonian 2239:Callovian 2153:Aquitania 2103:Montauban 2063:Isostatic 2034:Bastennes 2010:Lavardens 1998:Roquefort 1989:Parentis- 1875:Terrasson 1843:antiform. 1824:Paleogene 1792:anticline 1735:dune belt 1632:south of 1611:Bordelais 1607:Messinian 1603:Tortonian 1507:laterites 1475:Bartonian 1373:Paleocene 1367:Paleogene 1336:Campanian 1311:Angoulême 1307:Angoumian 1277:Campanian 1273:Santonian 1269:Coniacian 1254:Paleocene 1245:Coniacian 1233:trachytes 1161:Barremian 1107:Virgulian 1049:Tithonian 1029:Callovian 1011:Bathonian 996:bryozoans 964:anhydrite 916:). These 862:Deroceras 854:Arietites 850:ammonites 815:Périgueux 811:Angoulême 669:dolerites 655:evaporite 648:dolomitic 644:mudstones 567:diapirism 472:Aquitaine 455:Geography 275:Hydrology 190:Occitanie 158:Aquitaine 154:Etymology 2556:Chalosse 2532:charcoal 2488:Arjuzanx 2470:Holocene 2434:Langhian 2395:aquifers 2390:Classic 2357:Lavergne 2349:Parentis 2247:Brittany 2223:Toarcian 2157:Gondwana 2125:Devonian 2121:Bergerac 2030:Biarotte 1996:Mimizan- 1960:Landiras 1952:La Teste 1907:synforms 1772:Dordogne 1743:Europe's 1739:Holocene 1707:ice ages 1634:Soustons 1626:Zanclean 1622:Pliocene 1615:Bazadais 1596:Armagnac 1588:Langhian 1537:Chattian 1525:Rupelian 1499:Castrais 1471:Lutetian 1458:(in the 1456:molasses 1432:Ypresian 1389:Audignon 1362:Cenozoic 1349:micrites 1318:Ligerian 1241:Turonian 1065:Périgord 1057:Charente 1015:breccias 1007:dolomite 1003:Bajocian 941:Aalenian 918:littoral 900:and the 846:Carixian 831:lagoonal 714:Jurassic 689:Toulouse 634:Triassic 616:and the 582:Arcachon 504:Narbonne 484:Pyrenees 441:Triassic 433:Variscan 418:Cenozoic 414:Mesozoic 387:Lavergne 379:Parentis 374:Field(s) 355:Holocene 327:Eurasian 280:River(s) 247:Pyrenees 204:Toulouse 200:Bordeaux 182:State(s) 2494:Bauxite 2476:Lignite 2372:Meillon 2362:In the 2343:In the 2215:Carnian 2196:Pangaea 2117:Chalais 2056:Meilhon 1991:Bouglon 1978:Mimizan 1964:Guyenne 1942:Carcans 1927:Listrac 1911:Saintes 1897:Ribérac 1847:Castres 1828:Neogene 1788:micrite 1761:Gironde 1654:Cieutat 1650:Orignac 1638:benthic 1555:Neogene 1549:Causses 1545:Agenais 1541:seastar 1533:anomiid 1464:Agenais 1426:In the 1381:echinid 1341:Aturian 1181:rudists 1085:urchins 1074:In the 992:lignite 844:/Lower 827:arkoses 790:oolitic 700:Germany 677:diapirs 667:flows ( 662:ophitic 563:faulted 555:Garonne 551:isobath 508:thrusts 437:Permian 396:Meillon 334:Orogeny 304:Geology 290:Lake(s) 284:Garonne 257:Part of 226:Onshore 208:Bayonne 164:Country 126:44°16′N 44:improve 2710: 2692: 2674: 2656: 2558:, and 2538:Fruits 2514:Metals 2484:Landes 2436:, and 2374:, and 2353:Cazaux 2299:basin. 2259:Eocene 2251:Albian 2235:Africa 2207:Iberia 2038:Garlin 2020:Nogaro 2006:Cezans 1993:-Agen. 1915:Sarlat 1893:Jonzac 1882:Cognac 1729:finds. 1717:, and 1711:Mindel 1656:, and 1575:, the 1573:Condom 1561:Landes 1440:Oléron 1417:Ariège 1407:, and 1326:uplift 1287:sands. 1275:, and 1258:Danian 1235:, and 1221:flysch 1215:-Agen- 1213:Cahors 1188:Albian 1087:, and 980:Tarbes 976:Dogger 970:Dogger 945:gypsum 884:oyster 882:) and 864:, and 819:Figeac 762:Quercy 728:Dogger 704:Tethys 658:strata 524:Vendée 469:region 425:France 383:Cazaux 339:Alpine 196:Cities 176:France 173: 129:0°10′W 33:, but 2560:Béarn 2542:Plums 2452:karst 2448:china 2418:Clays 2316:near 2099:Fumel 2095:Niort 2054:-Pau- 2002:Créon 1909:near 1804:fault 1539:with 1479:Blaye 1436:Médoc 1345:flint 1265:chalk 1217:Muret 1177:algae 1045:marls 1005:with 984:reefs 803:shelf 708:Brive 402:(gas) 389:(oil) 322:Plate 2708:ISBN 2690:ISBN 2672:ISBN 2654:ISBN 2552:Wine 2528:Wood 2522:zinc 2518:lead 2508:Iron 2500:and 2498:Pech 2468:and 2462:Peat 2428:and 2426:tile 2420:and 2355:and 2335:and 2233:and 2131:age. 2052:Lacq 2016:Boos 1972:The 1913:and 1869:The 1813:The 1719:Würm 1715:Riss 1605:and 1590:and 1481:and 1473:and 1334:The 1165:Lacq 1144:The 1099:and 1061:Gers 1041:Malm 1035:Malm 974:The 953:and 933:and 768:Lias 732:Malm 724:Lias 671:and 665:lava 642:and 416:and 408:The 392:Lacq 267:Area 2337:gas 2333:oil 1817:or 1646:Ger 1299:Lot 1260:). 1067:at 998:). 988:Pau 423:in 346:Age 212:Pau 2727:: 2714:. 2706:. 2696:. 2678:. 2660:. 2548:). 2540:. 2464:. 2440:). 2370:, 2351:, 2229:, 2202:). 1830:. 1774:. 1713:, 1694:, 1648:, 1598:. 1403:, 1351:. 1271:, 1152:. 1121:. 1091:. 910:, 860:, 856:, 852:—( 837:. 825:, 734:: 710:. 691:. 653:, 604:. 569:. 546:. 530:. 398:, 394:, 385:, 381:, 296:, 249:, 245:, 241:, 237:, 210:, 206:, 202:, 188:, 2520:- 2490:. 2458:. 2261:/ 2209:. 2145:. 2127:/ 2101:- 2058:. 2050:- 2046:- 2040:. 2036:- 2032:- 2028:- 2022:. 2012:. 2008:- 2004:- 2000:- 1966:. 1958:- 1954:- 1944:. 1940:- 1933:. 1917:. 1899:- 1895:- 1749:. 1709:— 1652:- 1624:( 1567:( 1523:( 1430:( 1256:( 817:- 813:- 809:- 353:- 69:) 63:( 58:) 54:( 40:.

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