Cénomanien

Cénomanien

Cénomanien (100,5 - 93,9 I, is a duration of 6,6 My, according to the international charter of 2012) is a particularly informed floor because it corresponds to a rise eustatique remarkable, maybe the highest of all times geological. Seas épicontinentales are very widely developed and settle pelagic carbonated muds and hémipélagiques there. Cénomanien can be considered as a big transgressive phase, punctuated by several regressive episodes of more short duration and lesser amplitude. The sequential stratigraphy (Robaszynski and al ., on 1998; Wilmsen, on 2003) recognizes generally 6 sequences of deposit (DDS), of a duration of the order of a million years.

sequences_cenomanien

The sequences of Cénomanien, according to Robaszynski and al ., on 1998

Bioevents of Cénomanien, according to Mr Wilmsen (2012)

Towards the end of Cénomanien occurs the anoxic oceanic event OAE2 in the course of which the oceans become impoverished in oxygen and a big quantity of organic matter is held in deep sediments (black shales). The up-wellings of these waters sub-oxygenated on platforms are going to lead the disappearance about 27 % of the marine kinds. An excursion is positive of d13C mark this event (the organic matter grows rich preferentially in this isotope). The phenomena on platforms are more complex. The concomitant rise of the marine level in the limit C/T (Cénomanien / Turonien) is one of stronger registered.
The essential characteristics of the OAE2 are (Nzoussi, on 2003):

  • An extension téthysienne short-term (approximately 0,5 My),
  • A content raised in essentially marine M.O.,
  • A very high positive anomaly of d13C,
  • A content raised in certain elements-tracks: Ag, Cd, Mb, Sb, V, Zn,
  • A rate of low sedimentation,
  • A rarity of bioturbations,
  • A poverty in fauna benthique.

The causes of this event are not still totally clarified (for example, anomalies in iridium lead certain authors to compare him with the impact météoritique of the limit K/T). Among the likely causes:

  • The vast transgression which spreads seas épicontinentales favors the development of the marine primary productivity and destroys the forests of the low plains;
  • The high temperatures and especially the low gradient latitudinal which slows down the thermal machine;
  • The configuration latitudinale of Téthys which slows down the exchanges between polar waters and warm waters and favors the stratification thermohaline; the stagnance of waters leads to the expansion of the zone with minimum of oxygen;
  • The enrichment of oceanic waters by the CO2 mantellique (ridges, trouble spots Caribbean and Ontong Java))

THE OAE2 corresponds to a maximum of the long eccentricity (Mange and Voigt, on 2006). The effects of the climatic signal precession / eccentricity must be amplified by an important volcanic degassing. 3 phases would so follow (to follow curve of d13C on the following face):

1) Reduction eustatique in 10 m in the base of her Zone in Geslinianum (Shortly before the end of Cénomanien, before marls in plenus) bound to the astronomical forcing, the increase of the productivity bound to the nourishing contributions of rivers and increase of d13C;

2) Reduction of her pCO2 Of the atmosphere and the greenhouse effect which is attached to him, rough cooling was showed by him d18O and by extinctions of biological sorts and the changes of type of fauna at the beginning of Turonien.

3) Volcanic degassing, increase of the greenhouse effect, the rise of the level of the seas of 20 m, oceanic anoxia and increase of d13C.
The anomaly osmium (Turgeon and Creaser, on 2008) ) in the coats of Furio (Italy) and the drilling ODP 1260B, contemporary of the training of the Caribbean plate would indicate that deep volcanism mantellique would be responsible for this anoxic period.

fin du cenomanien

The end of Cénomanien, according to Mange

Another event marks the environment of Cénomanien, referenced MCE1 or Mid-Cenomanian Event 1 " hypothetical equivalent and in a lesser scale of the AOE2. He begins on the verge of zones in C. Inerme And T. costatus and marks by a low diminution of d13C followed by an increase of the order of 0,5 ° / °°. A double oscillation affects the level eustatique (Hancock, on 2003), with 2 minima, the one MCE1a in the zone in Costatus (Primus event), other MCE1b in the base of the zone in acutus.

Sequence It 3 and It 4 - Variation of d13C with both peaks - Screwed - extract modified according to Reboulet and al ., on 2012

Globally, the transgression cénomanienne peaks in the third superior of upper Cénomanien (at the end of the zone to Calycoceras guerangeri-naviculare).

The stratigraphy of Cénomanien of the Country of Callus is established well (Juignet, on 1974; Owen, on 1996; Amédro and Robaszynski, on 2001)), mainly by its macrofauna of ammonites and of inocérames. Cliffs between Havre and Etretat (valleuse of Antiiron) cover the set of the floor; in the Course Fagnet (FFécamp) only the terminal part appears in the base of the cliff.

Compared with the classic cups (Isle of Wight, Beachy Head, Folkstone, White-nose), Cénomanien du Bec-de-Caux possesses a reduced thickness (between 40 and 50 m), resulting from a rate of lower sedimentation (less thick stanzae) but especially from episodic condensations underlined by hard-grounds. Flints establish the peculiarity sédimentologique the most typical of this region; the top of the elementary sequences is almost systematically concerned by such a transformation diagénétique. Flints appear more prematurely in the Beak of Callus than in England. The sedimentary area is considered as a high zone, weakly subsidente, outside an emerged Armorican massif.

For the following descriptions, the sequential stratigraphy supplies the main pattern. A cutting in more high-resolution is brought by the factual stratigraphy. The cyclostratigraphie is applicable, apparently. But because of recurring hiatuses, the wedging with stanzae defined in England remains at the moment problematic. The subdivisions adopted are the ones of Robaszynski and al. (1998). They understand 5 sequence and the bottom of the sixth, Ce1 to Ce6. Wilmsen (2003) also recognizes in Lower Saxony the same cutting with for notation SB Ce I to VI.

Turonien
HG antiiron 3
Ce6
HG antiiron 1 Guerangeri / geslinianum
Ce5
HG Pavilly Rhotomagense / jukesbrownnei
Ce4
HG Rouen 1 Dixoni / inerme
Ce3
HG Bruneval 1 Saxbii / dixoni
Ce2
HG saint Jouin Schlueteri / saxbii
Ce1
Surface Octeville

Subdivisions of Cénomanien in the Country of Callus

In the continuation, we shall examine the series cénomanienne in 5 successive cups recovering partially:

  1. The base of Cénomanien in the beach of Saint-Jouin Bruneval
  2. The part averages of Cénomanien lower than Grouin (Bruneval)
  3. Lower Cénomanien p.p. and average Cénomanien in the descent of saint Jouin's terminal
  4. Average Cénomanien to the Valleuse du Fourquet
  5. Upper Cénomanien, between the Point of Fourquet and Valleuse d' Antifer