The North Sea Cycle&lt;subtitle&gt;An Overview Of 2Nd-Order Transgressive/Regressive Facies Cycles In Western Europe&lt;/subtitle&gt;

Jacquin, Thierry; Dardeau, G.; Durlet, Christophe; Graciansky, Pierre-Charles De; Hantzpergue, Pierre

doi:10.2110/pec.98.02.0445

Cited by 72 publications

(71 citation statements)

References 0 publications

Supporting

Mentioning

Contrasting

Unclassified

Order By: Relevance

“…The reconstruction of changes in sea level around the Callovian-Oxfordian boundary is controversial: Norris and Hallam (1995) recognized a transgression over western Europe; Jacquin et al (1998) placed the top of a regressive cycle at the base of the Late Callovian Lamberti Zone and the top of the following transgressive cycle within the lower part of the Early Oxfordian Cordatum Zone; Dromart et al (2003a,b) postulated an abrupt sea-level fall within the Lamberti Zone followed by a sea-level rise starting at the Callovian-Oxfordian boundary.…”

Section: Ammonitesmentioning

confidence: 99%

Paleoclimatic control of biogeographic and sedimentary events in Tethyan and peri-Tethyan areas during the Oxfordian (Late Jurassic)

Cecca¹,

Martin-Garin²,

Marchand³

et al. 2005

Palaeogeography, Palaeoclimatology, Palaeoecology

118

View full text Add to dashboard Cite

The paleobiogeographical distribution of Oxfordian ammonites and coral reefs in northern and Central Europe, the Mediterranean area, North and East Africa, and the Middle East and Central Asia is compared with the distribution in time and space of the most important lithofacies. Interest in the Oxfordian is focused on changes in facies and in biogeographical patterns that can be interpreted as the results of climatic events. Paleotemperature trends inferred from oxygen isotopes and paleoclimatic simulations are tested against fossil and facies data. A Late Callovian-Early Oxfordian crisis in carbonate production is indicated by the widespread absence of Lower Oxfordian reefal formations. There is a gap (hiatus) in deposition on epicontinental platforms, with Middle Oxfordian deposits resting paraconformably on Upper Callovian, while shales accumulated in adjacent intracratonic basins. Simultaneously, in Mediterranean Tethys, radiolarites accumulated in deep troughs while Rosso Ammonitico facies formed on pelagic swells. However, deposition on swells was also discontinuous with numerous gaps (hiatuses) and sequences that are much reduced in thickness. Middle Callovian deposits are generally overlain by Middle Oxfordian limestones. The dearth of carbonates is consistent with a cooling event lasting about 1 My. By the middle Oxfordian a warming, leading to bgreenhouseQ type conditions, is suggested on the basis of both biogeographical (mostly coralreef distribution) and geochemical data. Carbonates spread onto an extensive European platform while radiolarites reached a maximum development in the Mediterranean Tethys. Two distinct latitudinal belts, with seemingly different accumulation regimes, are therefore inferred. Similar latitudinal belts were also present in the late Oxfordian, when carbonates were widespread. The distribution of reefal facies in the late Oxfordian-early Kimmeridgian fits relatively well with GCMs simulations that imply low rainfall in the Tethyan Mediterranean area and slightly higher precipitation in central and northern Europe. Local salinity variations, reflecting more arid or humid conditions, may bias the paleotemperature signal inferred from

show abstract

Section: Ammonitesmentioning

confidence: 99%

Paleoclimatic control of biogeographic and sedimentary events in Tethyan and peri-Tethyan areas during the Oxfordian (Late Jurassic)

Cecca¹,

Martin-Garin²,

Marchand³

et al. 2005

Palaeogeography, Palaeoclimatology, Palaeoecology

118

View full text Add to dashboard Cite

show abstract

“…Dix-sept séquences de dépôt dites de troisième ordre, notées To1 à To7, Aa1, Aa2, Bj1 à Bj5, Bt1 à Bt3 ( fig. 2 ; [Graciansky et al, 1998a et b ;Jacquin et al, 1998 ;Hardenbol et al, 1998] ont été identifiées sur ces sections de part et d'autre de la discontinuité mi-cimmérienne. Les cartes isopaques des tranches de sédiment comprises entre chacune des limites de séquences, considérées comme autant de surfaces isochrones , ont été dessinées automatiquement par interpolation (krigeage) entre les 262 points de contrôle suivant un maillage kilométrique couvrant un rectangle de 335 km (N-S) par 500 km (E-W).…”

Section: La Méthodeunclassified

“…Le maximum de régression à long terme d'âge finiaalénien à bajocien inférieur se traduit par un maximum de progradation des plates-formes carbonatées de cet âge en direction du SE de la France [Graciansky et al, 1993 ;Jacquin et al, 1998] duction de la sédimentation qui lui est associée ( fig. 9) illustre le rôle du bassin de Paris comme un haut fond temporaire, relativement aux aires de sédimentation réparties à sa périphérie, le bassin dauphinois par exemple.…”

Section: Les Manifestations Principales Des éVénements Cimmériensunclassified

Microstructural evolution of metabasalts within a contact metamorphic aureole : a preliminary quantitative bi-dimensional approach

Hébert¹,

Guézou²,

Souque³

et al. 2003

Bulletin De La Société Géologique De France

View full text Add to dashboard Cite

The emplacement of the Saint-Brieuc diorite (533 ± 12 Ma ; Brittany, France) developed a narrow contact aureole in metabasaltic host-rocks which were previously submitted to a regional-scale deformation and metamorphism at around 590-570 Ma. This study aims to qualify and quantify the microstructural changes of rocks that occur within the contact aureole and that are the result of the static recrystallization due to the thermal effect of the diorite. In order to quantify the textural evolution of rocks, an image analysis has been performed on thin sections. It focused on the measurements of morphological features of hornblende and opaque phases. They are anisotropy shape factors (stretching and elongation) of minerals, the preferred orientation of minerals and the distribution size (areas) of minerals. The quantification of these different parameters shows that the static recrystallization, which increases when approaching the contact with the intrusive, (i) is responsible of a reduction of the anisotropy shape and elongation parameters of grains, (ii) causes coarsening and (iii) is responsible for the disappearance of preferred orientation of minerals. Both together, the qualitative description and quantitative measurements show that the solid-state transformations due to contact metamorphism tend to make the rocks isotropic and equigranular.

show abstract

“…Oli vero et al (1997. Hardenbol et al (1998) and Jacquin et al (1998).Palaeoichnological, taphonomic and sedimentological re sults confnll1, therefore, the development of a deepening phase associated with sedimentary starvation, within 3rd and 2nd or der cycles, in the Bas-Auran area, during the Early Bathonian. The maximum deepening of a 2nd-order transgressivelregres sive facies cycle (T/R 7, Upper Aalenian-Upper Bathonian, in Graciansky et al 1993Graciansky et al .…”

mentioning

confidence: 95%

“…The maximum deepening of a 2nd-order transgressivelregres sive facies cycle (T/R 7, Upper Aalenian-Upper Bathonian, in Graciansky et al 1993Graciansky et al . 1998) is at the end of the Early Bathonian, which corresponds to an extensional and deepening phase of the basin.…”

Section: Introductionmentioning

confidence: 99%

Formal proposal for the Bathonian GSSP (Middle Jurassic) in the Ravin du Bès Section (Bas-Auran, SE France)

Fernández-López

Pavia²,

Erba

et al. 2009

Swiss J. Geosci.

View full text Add to dashboard Cite

The Bathonian Global Stratotype Section and Point (GSSP) is proposed at the base of limestone bed RB071 (bed 23 in Sturani 1967) in the Ravin du Bes Section (43057' 38" N, 6° IS' 55" E), Bas-Auran area, "Alpes de Haute Provence" French department. The Ravin du BesSectioll , as formal candidate GSSP for the base of the Bathonian Stage, satisfies most of the requirements recommended by the International Commission on Stratigraphy: 1) The ex posure extends over 13 m in thickness. At the Bajocian-Bathonian transition, no vertical (bio-, ichno-or tap ho-) facies changes, condensation, stratigraphic gaps or hiatuses have been recorded. Structural complexity, synsedimentary and tectonic disturbances, or important alterations by metamorphism are not relevant constraints. 2) There is a well-preserved, abundant and diverse fos sil record across the boundary interval, with key markers (ammonites and IntroductionThe present paper corresponds to part of the scientifIc dossier recently prepared by several specialists and sent to all mem bers of the Bathonian Working Group (International Subcom mission on Jurassic Stratigraphy, November 2007), in order to achieve the formal ballot on the selection and proposal of the Global Stratotype Section and Point (hereafter GSSP The Bathonian Working Group (BtWG) was established in 1984, during the 1st International Symposium on Jurassic Stratigraphy in Erlangen, in order to improve the geologic data relative to the Bajocian/Bathonian boundary. The Bas-Auran section was first proposed as stratotype in a presentation to the Luxembourg II (1967) Colloquium by Torren� but not pub lished until 1974lished until (Morton 1974Torrens 1974a Torrens , b, 1987 Torrens , 2002 fig. 8; pI. 19, fIgS. 1-2) are the index species, respectively, of the Bathonian basal zone and subzone. The Zigzag Zone was distinguished from the underlying Parkinsoni Zone by Oppel (1857Oppel ( . p. 579. 1862. and later assigned to the "Bath-Gruppe·· (Oppel 1865. p. 309) in a discussion of the section at "Mon tagne de Crussol" in the Ardeche (France). The Convergens Subzone was mentioned by Maubeuge (1950, p. 4), based on the "Convergens horizon" that was used in letters by Arkell (1951-59. p.10; 1956. p. 62). The Bajocian/Bathonian bound ary established between the Parkinsoni and Zigzag zones was recommended at the two congresses denominated "Colloque du Jurassique" held in Luxembourg in 1962(Rioult 1964 Tor rens 1965) and 1967(Torrens 1974a. The localities of Bath (England) and the "Montagne de Crussol" (France), however, have been considered quite unsuitable for a typological defini tion of the Bathonian Stage, because they are condensed sec tions with discontinuous and lenticular beds (Torrens 1974a(Torrens , b, 2002Page 1996b). After the publication of Sturani (1967) (Sturani 1967). The Parvum Sub zone has been proposed by Mangold (1990) to denote the first Bathonian subzone of the Zigzag Zone in the Sub-Mediter ranean Province, equivalent to the Convergens Sub zone of the Northwest European Province...

show abstract

The North Sea Cycle<subtitle>An Overview Of 2Nd-Order Transgressive/Regressive Facies Cycles In Western Europe</subtitle>

Cited by 72 publications

References 0 publications

Paleoclimatic control of biogeographic and sedimentary events in Tethyan and peri-Tethyan areas during the Oxfordian (Late Jurassic)

Paleoclimatic control of biogeographic and sedimentary events in Tethyan and peri-Tethyan areas during the Oxfordian (Late Jurassic)

Microstructural evolution of metabasalts within a contact metamorphic aureole : a preliminary quantitative bi-dimensional approach

Formal proposal for the Bathonian GSSP (Middle Jurassic) in the Ravin du Bès Section (Bas-Auran, SE France)

Contact Info

Product

Resources

About