Notes: The origin of third-order depositional sequences remains debatable, and in many cases it is not clear whether they were controlled by tectonic activity and/or by eustatic sea-level changes. In Oxfordian and Berriasian–Valanginian carbonate-dominated sections of Switzerland, France, Germany and Spain, high-resolution sequence-stratigraphic and cyclostratigraphic analyses show that the sedimentary record reflects Milankovitch cyclicity. Orbitally induced insolation changes translated into sea-level fluctuations, which in turn controlled accommodation changes. Beds and bedsets formed in rhythm with the precession and 100-kyr eccentricity cycles, whereas the 400-kyr eccentricity cycle contributed to the creation of major depositional sequences. Biostratigraphical data allow the correlation of many of the 400-kyr sequence boundaries with third-order sequence boundaries recognized in European basins. This implies that climatically controlled sea-level changes contributed to the formation of third-order sequences. Furthermore, this cyclostratigraphical approach improves the relative dating of stratigraphic intervals.

Notes: Outcrop sections from the Swiss Jura, consisting of carbonate-siliciclastic deposits spanning the Middle-Late Oxfordian boundary, provide a palaeogeographical cross-section ranging from coastal to shallow platform and intra-platform basin environments. Using a sedimentological and a 3rd order sequence stratigraphic framework based on those sections, the distribution of sedimentary organic matter (palynofacies) has been spatially studied in relation to sequence stratigraphy.The main factors influencing the spatial variations of sedimentary organic matter are the proximity of land, organic productivity, level of biodegradation and hydrodynamic conditions of the palaeoenvironment. These factors determine the distribution of the land-derived, relatively allochthonous organic constituents (phytoclasts, pollen and spores), and marine, relatively autochthonous constituents (phytoplankton and foraminifera linings).Five main palynofacies parameters appear as good indicators of proximal-distal trends: the relative proportion of total phytoclasts; the proportion of fresh, translucent fragments among these phytoclasts; the ratio of marine to continental palynomorphs; and the relative amount and species diversity of dinoflagellate cysts. In lowstand deposits, high-energy hydrodynamic conditions may affect these trends on the shallow platform, where storms tend to increase the proportion of the marine organic fraction landwards. These five palynofacies parameters are largely related to water depth. Therefore, when compared with the established 3rd order sequence stratigraphic framework, their stratigraphic variations indicate relative sea-level changes or, alternatively, proximality changes. Parameters indicative of more distal conditions increase in the transgressive and early highstand, and decrease in the late highstand. The opposite occurs for parameters indicative of more proximal conditions. Foraminifera linings seem to be particularly concentrated near the shelf edge and on the slope. Finally, bisaccate pollen may display cyclicity associated with alternating humid and dry periods. This palaeoclimatic signature may be related to orbital cyclicity.

Notes: Abstract Barremian and Aptian shallow-water carbonate facies (uppermost Lekhwair, Kharaib and Shuaiba Formations) are described from outcrops in northern Oman. Based on facies analysis and bedding pattern, three orders of depositional sequences are defined (third to fifth order) and correlated between sections. Over the course of three third-order sequences, covering the Barremian to Lower Aptian, a third-order depositional pattern is documented that consists of a succession of three distinct faunal assemblages: discoidal orbitolinids and calcareous algae were deposited during early transgression; microbialites and microencrusters dominate the late transgressive to early highstand facies; and a rudist- and miliolid-dominated facies is typical of the highstand. This ecological succession was controlled largely by palaeoenvironmental changes, such as trophic level and clay influx, rather than sedimentological factors controlled by variations in accommodation space. Orbitolinid beds and carbonates formed by microbialites and microencrusters seem to be the shallow-water carbonate response to global changes affecting Late Barremian to Aptian palaeoclimate and palaeoceanography.