The tectonic context of the English-Parisian Pond

Globally, our sea of the chalk is situated in him W of the continent eurasiatique. This continent is an inheritance of the super-continent of Pangée which existed of the end of the Carboniferous period at the beginning of the Jurassic. At these times, the north wing of Pangée which includes Europe trains Laurasia, whereas the south wing includes Africa, Antarctica, Australia and India. Pangée splits up then: Laurasia parts from Africa, Eurasia parts from North America because of the opening of Atlantic Ocean. This opening is not synchronous, it propagates of the South northward. Grabens (ditches of collapse) forms in Europe with an Atlantic direction. In the lower Cretaceous opens Bay of Biscay.

Tectonic card centered on Western Europe, modified according to Ziegler (1990)

In the upper Cretaceous, in the Coniacien, before the magnetic anomaly C34, the pole of rotation between the European plate and the African plate modifies its position, which brings the convergence of these two patches, always current. In the continuation, Europe is going to register deformations which are going to be translated in particular by a tectonic inversion of the Mesozoic grabens (from tthe extension towards the compression).

Tectonic card of north-western Europe (Ziegler, on 1990) showing zones affected by the tectonics subhercynienne.

The previous card (modified according to Ziegler, on 1990) watch represented turns zones affected by the tectonics subhercynienne (upper Cretaceous). They are situated in Was born the axis of base London - Brabant. This tectonics subhercynienne takes place during the sedimentation of the chalk.
The graben of the North Sea undergoes an inversion from the upper Cretaceous.
In the of Paris Basin, two orogènes begin to be set up in the upper Cretaceous, Pyrenees and the Alps.

Tectonic card of Western Europe and northern Africa in Santonien (anomaly 34), extracts modified by Stampfli and al ., on 2002.

The tectonic evolution of Pyrenees is coupled with that of the opening of the Bay of Biscay. The first tracks of oceanic accretion in the latter date upper Albien, during the CNS (Cretaceous Normal Superchron). During the rifting, the Armorican Massif remains emerged, representing a retaining wall of rift valley. The magnetic anomalies allow to move forward that Aptien (1110 My) ) enters and Campanien (anomaly 33, 75 My), the Iberia moved about 200 km towards him. This movement places her then in approximately 100 km in S of its current position. The first travels compressifs, at the level of Pyrenees, will begin as soon as possible only in Maastrichtien (TThinon and al ., on 2001).

Travel of the Iberia enters Aptien (110 my) and Campanien (75 My)

In him E of the iberian micro-plate, at the level of the block parade-Sardinian, because of the position of the pole of rotation, the relative movement with regard to Europe is of type transpressif (Rosenbaum And al. 2002). Provence registers first constraints compressives in the lower Cretaceous passage / upper Cretaceous, responsible for the convexity durancien (oor inhabitant of the Var) ) and of the generative emersion of bauxites. Weaknesses of base (Aix, Durance) are reactivated from terminal Santonien and produce syn-tectonic alluvial cones (Leleu, on 2005)). The implementation of the tectonic tablecloths will begin only in the lower Eocene

Type de mouvement entre l'Ibérie et l'Europe, modifié d'après Rosenbaum et al., 2002

Type of movement between the Iberia and Europe, modified according to Rosenbaum and al ., on 2002

In the upper Cretaceous Africa with its headland apulien and Europe convergent. But the alpine ocean is not closed yet. Eastward, are set up tablecloths during Turonien - Coniacien, resulting from the poinçonnement of Europe by the block Adria and the block Moesia (Haas and Péro, on 2004)). These tablecloths establish:

  • The set Alcapa (Austro-alpine, centro-western The Carpathians, Pelso),
  • The mega-units of Tisza and Dacia.

Extract of the tectonic card (Global Paleogeography, ed. Ron Blakey), there is 100 My the beginning of Cénomanien)

Extract of tectonic card, there is 75 My (average Campanien) according to Global Paleogeography, ed. Ron Blakey

Chronology of the deformations

Three tectonic phases are distinguished:

1-a a sub-Hercynian phase (Turonien-Campanien) [etymology: region of Germany in N mounts of the Harz] with for marks:

  • The opening of the Labrador Sea in Turonien lower than 92 My;
  • The training of Pyrenees which begins in Santonien-Campanien.

This phase affects at a distance the English-Parisian Pond.
She is subdivided:

  • Premature phase Ilsede (upper Turonien),
  • Phase Ilsede de Stille (average Coniacien),
  • Phase Wernigerode (upper Santonien),
  • Phase Saddens (lower Campanien).

Tectonic phases and relative marine level, d

2 - A phase laramide (Paléogène = Paléocène with Oligocene), particularly in the limit Paléocène - Eocene between the magnetic anomalies C25-C24 (56 - 53 My) and the opening of the Mer de Norvège-Groënland.

3 - An oligo-Miocene phase, particularly between Chattien 25 My, an anomaly C7 and a Burdigalien 20 My, anomaly C6.
Since the end of the Pliocene (2,5 My), the uprising of the trays of the western border of the Pond of Paris globally considered at 150-200 m (Pomerol, on 1978; Lautridou and al .,
During the last million years, the average speed of uprising is estimated at 55 / 60 m (5 5 in 6 m / 100 ka), on the basis of the section of the systems of terraces of the big valleys (Lautridou and al ., 1999a; Antoine and al ., on 2000).

Expression of the deformations

The various diets of constraints which acted on the chalk from the beginning of its deposit (Cénomanien) until our days were translated by phenomena among which the nature, the duration and the spatial area are very different.

  • Earthquakes occurring during the sedimentation of the chalk and which affect especially coats most freshly put down (in-depth fragile break, slidings, slumpings, strains, resédimentation on-surface), qualified of séismites.
  • Wrinklings (flexible deformations) which affect a set of coats of previously put down chalks. The seismic profiles demonstrate that number of these wrinklings is bound to the rejeu of former big weaknesses affecting the paléo-Mesozoic base, often with a horizontal rejection.
    • Example 1: Mortimore (on 2010, fig. 38) represents a complex system of folds in level aligned in South Downs, on approximately 80 km in the WNW of Beachy Head.
    • Example 2: the weakness of Bray-Vittel which goes on by the zone faillée of the Channel of Bristol (Wales) is bound to the périclines of Sandown and Brixton (Mortimore, on 2010)
  • Weaknesses (breakable deformation) which affect even there a set of coats of previously put down chalks, but play over time during the deposit of chalky muds. The weakness of Fécamp-Lillebonne is one of these scenarios with abnormally thick average Coniacien, established by elementary sequences plurimétriques.
  • Condensations or sedimentary thickenings accompany the tectonic deformation of the sea bed. At the level of axes anticlinaux, chalks noduleuses, hard-grounds and stratigraphical gaps are more pronounced. This effect is felt, for example, on the axis anticlinal of Bresle, with the development of hard-grounds Seas in upper Turonien.

Recent seismicity

In Manche, recent earthquakes of weak amplitudes were listed by the networks of measure. They are replaced here on this Google card Maps (travel and zoom possible, click the icon to know the date).

View Earthquakes In has larger map

The most recent earthquake is the small earthquake of July 14th, 2011 between Havre and Isle of Wight. In XVIII Ème And XIX Ème Centuries, subjective indications (obviously no seismological network in this time) state earthquakes felt in the region of Fécamp in 1757, 1766, 1772, on 1833 et1881.