西藏岗巴地区古新世-始新世界线地层及底栖大有孔虫的演替

古新世与始新世界线(P/E)事件中底栖大有孔虫的绝灭(BEE)以及演替(LFT)在古近纪底栖大有孔虫演化过程中起着非常重要的作用。西藏南部岗巴地区发育有良好的海相界线地层,在宗浦Ⅱ剖面中,对底栖大有孔虫动物群及碳、氧稳定同位素的研究显示全球界线事件对该地区造成明显影响。在界线附近,底栖大有孔虫出现大量灭绝,总灭绝率达71%,界线之上开始出现复苏,底栖大有孔虫的新生率为72%。事件过后,底栖大有孔虫SBZ4动物群被SBZ5-SBZ13动物群代替,以古新统宗浦组的Miscellanea miscella,Lockhartia hai mei,Glomalveolinapri maeva的灭绝和Operculina属的消失及始新统遮普惹组Nummulites willcox,Alveolina ellipsoidalis和Orbi-tolites complanatus出现为特征。在古新世界线顶部,碳稳定同位素值出现明显负偏,峰值为-7.9‰,与全球同一时期碳稳定同位素事件表现一致;氧稳定同位素表现则与全球事件不太相同,这可能是由于成岩作用的影响。     

古新统/始新统界线与特提斯大有孔虫生物带

21世纪初,古新统/始新统界线(简称P/E界线)被国际地层委员会正式定义为古新世-始新世极热事件(简称PETM)期间碳同位素负漂的开始。然而,P/E界线在特提斯大有孔虫生物带(简称SBZ)中的具体位置却一直争论不休。本文回顾了国内外学者近二十年来对P/E界线的研究成果,认为P/E界线应该位于SBZ5的内部,而非SBZ4和SBZ5的界线处。在P/E界线处,大有孔虫没有发生明显的组分上的变化。而在P/E界线后的5—12万年内,大有孔虫发生了一次绝灭。这个绝灭事件被称为大有孔虫的绝灭和新生(简称LFEO)。大有孔虫的绝灭和新生不同于传统上认为的大有孔虫更替事件(简称LFT)。前者可能是由PETM后期强烈的陆地风化剥蚀引起海水富营养化后所造成的一次灾变事件,而后者代表了大有孔虫在长期稳定的浅海环境中形成的演化上的成功。通过回顾P/E界线的研究历史,笔者认为绝大部分地层剖面在P/E界线处的不连续性/不完整性是产生这些争议的主要原因。     

南海北部陆丰凹陷LF14-4-1D井中新世浮游有孔虫生物地层研究

通过对前人在南海北部地区的中新世浮游有孔虫生物地层研究结果的对比,发现其中分带方案有一定的差异,而且分带依据和生物事件年龄也存在争议,特别是利用岩屑样品进行地层划分与对比的钻井尤为突出,对于后续研究和南海地区的地层对比都有较大的不利影响。基于此,我们对比了前人在南海北部中新世浮游有孔虫生物地层的研究成果,结合"2012国际地质年代表"和ODP184航次提供的经天文调谐的浮游有孔虫生物事件年龄,总结了研究区中新世以浮游有孔虫生物事件末现面为基础的13个地层分带,为南海北部地区浮游有孔虫生物地层的划分与对比,特别是生产单位利用岩屑样品进行研究的钻井地层划分,提供了可供对比的基础与依据。并依据上述分带方案,将南海北部陆丰凹陷LF14-4-1D井中新世地层详细划分出早中新世至上新世期间共9个有孔虫化石带或联合带,即早中新世M3带,早-中中新世M4-6联合带,中中新世M7带,M8带,M9带,M10带,M11带,晚中新世M12带和晚中新世-早上新世M13-PL1联合带。     

中更新世撞击事件对海洋环境的影响--南海ODP1144站的高分辨率记录

本文对采自南海北部ODP1144站(20°3.18′N,117°25.14′E,水深2 037m)385.8-386.4m层段的28个沉积物样品进行了微玻陨石、浮游有孔虫及其同位素分析,以评估中更新世撞击事件对环境的影响.微玻陨石见于孔深386.12-386.38m,而集中分布在386.22-386.25m厚约3cm的地层中.研究结果表明,中更新世撞击事件对环境的影响很可能只是小幅度和短时间(百年左右)的,尽管引起了南海表层海水温度约2℃的下降及其相应的δ18O的加重、浮游有孔虫冷水种含量的上升和暖水种含量的减少,但没有造成海水稳定同位素重大偏移和全球气候的灾难性影响,也没有引起浮游有孔虫在生物演化上的变化.     

东印度洋赤道南北两侧春季活体浮游有孔虫的组成与分布

2017年3月通过对在东印度洋海区6个站位53个垂直分层拖网浮游有孔虫样品进行的定量分析,探讨了该海区春季现代浮游有孔虫的组成、分布及其影响因素。东印度洋春季0～3 000m水层内共鉴定出17个浮游有孔虫属种,主要是Globigerinoides ruber,Globorotaloides hexagona,Globigerinoides sacculifer,Globigerinella aequilateralis,Neogloboquadrina dutertrei,Globorotalia menardii,Globiberinella calida,Pulleniatina obliquiloculata和Globorotalia theyeri等,它们是典型的热带亚热带暖水种浮游有孔虫群落。G.ruber,G.sacculifer最大丰度层在0～50m水层;G.conglomerata,G.hexagona最大丰度层均出现在50～100m;G.theyeris在100～1 000m间的水层均有活体出现,100～150m水层中该种浮游有孔虫丰度最高;G.scitula为深层水浮游有孔虫分子,主要出现于300～2 000m的深水水层。东印度洋春季浮游有孔虫群落的丰度在赤道中心区最低,由赤道向南北两侧扩展,其丰度逐渐递增的特点。浮游有孔虫丰度明显呈上层高,下层低的特点,在50～100m水层浮游有孔虫丰度最高,明显高于0～50m水层浮游的有孔虫丰度,这与印度洋50～100m水体中叶绿素最大值层相对应,表明浮游有孔虫受水体初级生产力影响明显。     

南极乔治王岛长城湾现代有孔虫

一、本区有孔虫研究简况 在南极有孔虫研究中,南极半岛、乔治王岛所在的南设得兰群岛周围及其邻近海域的有孔虫研究最为详细,迄今为止已发表了许多有关这一地区有孔虫研究报告。自1914年Faure-Fremiet发表法国波科伊公司第二次南极有孔虫类考察报告之后,1933年Earland报道了南乔治亚岛有孔虫;嗣后,1934年他又发表马尔维那斯(福克兰)群岛有孔虫,文中对布兰斯菲尔德海峡和南设得兰群岛周围有孔虫组合和分布规律进行了讨论。     

渤海莱州湾表层沉积物中底栖有孔虫分布特征及其环境意义

对渤海莱州湾海域240个站位表层沉积物中底栖有孔虫群落进行了分析,共鉴定常见的底栖有孔虫42种。结果表明,莱州湾表层沉积物中底栖有孔虫主要以玻璃质壳为主(平均丰度达70.9%),瓷质壳含量次之,胶结壳含量最低;玻璃质壳占有孔虫全群的百分含量,随水深的增加而增加;从黄河口向外海方向,有孔虫分异度和丰度都逐渐增大。该海域底栖有孔虫平面分布的主要控制因素为盐度和底质沉积物类型,大体可分为两个组合分区,I区为Ammonia beccarii-Quinqueloculina spp.组合,代表盐度较低的近岸海陆过渡浅水环境;II区为Cribrononionsub-incertum-Protelphidium tuberculatum组合,代表盐度较高的远岸内陆架环境。     

南海北部琼东南盆地BD-2井中新世有孔虫生物地层及沉积环境

南海北部琼东南盆地BD-2井中新世地层沉积连续,是琼东南盆地中新统较典型的钻井剖面之一。该井中新世地层中含丰富的有孔虫化石,共鉴定有孔虫62属98种,其中浮游有孔虫13属41种,底栖有孔虫49属57种。根据有孔虫标志种及螺旋浮游有孔虫旋向优势度的变化,对该井的有孔虫生物地层进行了详细划分,从早中新世至晚中新世共识别出11个有孔虫化石带或联合化石带。探讨了下中新统与中中新统,中中新统与上中新统界线的有孔虫划分标志。依据有孔虫丰度、分异度及组合特征,讨论了BD-2井从早中新世至晚中新世沉积环境演化特征。     

海南岛近岸沉积物中的有孔虫特征与分布

对位于海南岛近岸7-170 m水深、180个站位沉积物表层样的有孔虫分析表明,研究区浮游有孔虫类型较少、共发现浮游有孔虫19种,单个站位最多含有浮游有孔虫16种,而且浮游有孔虫含量(丰度)亦较低.底栖有孔虫则较为丰富,仅在较粗砂中底栖有孔虫丰度相对较低.常见近40多个底栖有孔虫属种,多数样品中以含有螺旋式与平旋式玻璃质底栖有孔虫为主,少数样品以胶结壳、列式玻璃质壳或大型底栖有孔虫为优势特征.本研究在详细阐述了底栖有孔虫主要特征属种的基础上进行了有孔虫分区,从而揭示其所包含的环境意义.     

西藏定日县贡扎上白垩统浮游有孔虫与桑顿阶/坎潘阶界线的厘定

白垩纪是大洋缺氧及生物灭绝等重大地质事件频发的一个时期,也是全球气候变暖的重要时期。因此,白垩纪研究对于探讨地质历史时期地球的系统演化,尤其是生物与环境之间的协同演化关系,具有十分重要的意义。西藏定日贡扎剖面保存着上白垩统较为完整的地层序列,文中对上白垩统岗巴村口组和宗山组剖面岩石样品中获得的有孔虫化石进行研究,鉴定出有孔虫化石8属22种,识别出Dicarinella asymetrica、Globotruncanita elevata、Globotruncana ventricosa、Radotruncana calcarata等4个有孔虫化石带。根据有孔虫化石确定贡扎剖面的地层时代为晚白垩世桑顿期(Santonian)至坎潘期(Campanian),桑顿阶/坎潘阶界线位于Dicarinella asymetrica带与Globotruncanita elevata带之间。     

西藏南部岗巴地区白垩纪中期钙质超微化石带和Cenomanian-Turonian界线

我国西藏南部海相白垩系含有较丰富的钙质超微化石。文中着重研究岗巴地区两个剖面 (即剖面A ,B)Albian Santonian钙质超微化石的分布。根据标志种的存在 ,识别出 5个初现面事件 ,相应地建立 6个钙质超微化石带 ,自下至上是Prediscosphaeracretacea带 ,Eiffellithusturriseiffeli带 ,Lithraphiditesacutum带 ,Gartneragoobliquum带 ,Quadrumgartneri带 ,Lucianorhabduscayeuxii带。同时 ,通过洲际对比 ,建议以G .obliquum初现面作为划分本区Cenomanian和Turonian界线的标志。此外 ,Q .gartneri带和I .cayeuxii带之间缺失多个化石带 ,据此推测Turonian至Santonian期间本区可能存在沉积间断。     

Facies pattern and sea-level dynamics of the early Late Cretaceous transgression: a case study from the lower Danubian Cretaceous Group (Bavaria,southern Germany)

The facies development and onlap pattern of the lower Danubian Cretaceous Group (Bavaria, southern Germany) have been evaluated based on detailed logging, subdivision, and correlation of four key sections using an integrated stratigraphic approach as well as litho-, bio-, and microfacies analyses. Contrary to statements in the literature, the transgressive onlap of the Regensburg Formation started in the Regensburg–Kelheim area already in the early Early Cenomanian Mantelliceras mantelli ammonite Zone and not in the Late Cenomanian. In the Early Cenomanian, nearshore glauconitic-bioclastic sandstones prevailed (Saal Member), followed by Middle to lower Upper Cenomanian mid-shelf siliceous carbonates intercalated with fine-sandy to silty marls (Bad Abbach Member). Starting in the mid-Late Cenomanian (Metoicoceras geslinianum ammonite Zone), a considerable deepening pulse during the Cenomanian–Turonian Boundary Event (CTBE) initiated the deposition of the deeper shelf silty marls of the Eibrunn Formation, which range into the early Early Turonian. During the CTBE transgression, also the proximal Bodenwöhrer Senke (ca. 40 km NE of Regensburg) was flooded, indicated by the onlap of the Regensburg Formation onto Variscan granites of the Bohemian Massif, overlain by a thin tongue of lowermost Turonian Eibrunn Formation. A detailed record of the positive δ¹³C excursion of the global Oceanic Anoxic Event (OAE) 2 has been retrieved from this shallow-water setting. An integrated approach of bio-, event-, carbon stable isotope and sequence stratigraphy was applied to correlate the sections and to decipher the dynamics of this overall transgressive depositional system. The Cenomanian successions show five prominent unconformities, which correlate with those being known from basins in Europe and elsewhere, indicating their eustatic origin. The rate of sea-level rise during the CTBE suggests glacio-eustasy as a driving mechanism for Late Cenomanian sea-level changes. The Regensburg and Eibrunn formations of the lower Danubian Cretaceous Group are highly diachronous lithostratigraphic units. Their regional distribution and northeast-directed onlap pattern onto the southwestern margin of the Bohemian Massif can readily be explained by the lateral movements of roughly coast-parallel (i.e., NW/SE-trending) facies belts of a graded shelf system transgressing on a northeastward-rising substrate. It took the Cenomanian coastline ca. 6 Ma to transgress from southwest of Regensburg to the topographically elevated granite cliffs southeast of Roding in the Bodenwöhrer Senke (=60 km distance).     

Paleoenvironmental changes across the Cenomanian/Turonian Boundary Event (Oceanic Anoxic Event 2) as indicated by benthic foraminifera from the Demerara Rise (ODP Leg 207)

This study is based on Cenomanian to lower Turonian sediments of Ocean Drilling Program (ODP) Sites 1258, 1259, 1260, and 1261 from the Demerara Rise (Leg 207, western tropical Atlantic, off Suriname) that are oriented along a paleodepth transect. Studied sediments include the Cenomanian/Turonian Boundary Event (CTBE) or Oceanic Anoxic Event 2 (OAE 2) and consist of laminated black shales with TOC values between 5% and 10% below and above OAE 2 and up to 29% within the OAE 2 interval. Benthic foraminiferal assemblages in this eutrophic environment are generally characterized by low diversities and strong fluctuations of abundances, indicating oxygen depletion and high organic matter fluxes. Dominant taxa at all sites are Bolivina anambra, Gavelinella dakotensis, Tappanina sp., Praebulimina prolixa, and Neobulimina albertensis. Based on the positive stable carbon isotope excursion characteristics of OAE 2 we subdivided the studied successions into three intervals: (1) the interval below OAE 2; (2) the carbon isotope excursion reflecting OAE 2; and (3) the interval above OAE 2. In the bathymetrically shallower Sites 1260 and 1261 benthic foraminiferal assemblages indicate anoxic to sometimes slightly dysoxic bottom-water conditions below the OAE 2 interval. The bathymetrically deepest Site 1258, in contrast, reflects more oxygenated bottom waters with an almost continuous occurrence of benthic foraminifera. It is therefore suggested that the shallower sites were located within the oxygen minimum zone (OMZ), whereas Site 1258 was below the OMZ. During OAE 2 anoxic conditions prevailed at the shallower sites. At Site 1258 benthic foraminifera indicate severe dysoxic but not anoxic conditions. This pattern is proposed to reflect a strengthening of the OMZ possibly related to increased primary production during OAE 2. A short-term repopulation event of benthic foraminifera in the lower third of the OAE 2 interval was observed at all sites, reflecting a brief bottom-water oxygenation event. This short-lived event parallels a surface-water cooling and is probably equivalent to the “Plenus Cool Event” in Europe and the “benthonic zone” in the U.S. Western Interior. The benthic foraminifera of a ~0.5 Ma interval following OAE 2 still indicate oxygen depletion of bottom waters. Subsequently, however, a strong increase in benthic foraminiferal abundance and diversity reflects better oxygenation of the bottom-water masses, probably related to a weakening of the OMZ due to decreasing organic matter flux.     

Cenomanian-Turonian carbon isotope events recorded in terrestrial organic matter from northern Japan

Carbon isotopic fluctuations recorded in terrestrial organic matter from the Upper Cretaceous Cenomanian-Turonian succession of Hokkaido, Japan show a remarkably similar pattern to isotopic fluctuation in carbonate carbon reported from southern England and the Italian Apennines. Chronological correlation for the Cenomanian-Turonian section of Japan is based on planktonic foraminiferal biostratigraphy with some additional data from macrofossils, allowing a detailed comparison of isotope stratigraphies for Japan and Europe. Three distinct features of the isotope profile, namely a positive spike near the Cenomanian/Turonian boundary, a shoulder in the lower-middle Turonian and a level segment in the middle-upper Turonian are observed in Japan. These features are biostratigraphically comparable and correlative with isotope profiles reported from Europe. The single factor influencing isotopic composition of both terrestrial organic carbon and marine carbonate carbon is isotopic change in the global CO₂ reservoir of the ocean-atmosphere system. If these three carbon isotope features are synchronous, they may be inferred as having been caused by global phenomena and as providing global high-resolution chemo-stratigraphic markers. Carbon isotope stratigraphy could be an important bridge between terrestrial inland sequences and marine sequences.     

Late Cretaceous (Cenomanian to Campanian) paleoenvironmental history of the Eastern Canadian margin of the Western Interior Seaway: bonebeds and anoxic events

Upper Cretaceous strata in the Pasquia Hills of the northern Manitoba Escarpment, eastern Saskatchewan, Canada provide a detailed paleoenvironmental and sea-level record of the eastern margin of the Western Interior Seaway. Sediments deposited during the Cenomanian/Turonian Greenhorn marine cycle are dominantly black mudstones deposited in a stratified water column, with bottom-water anoxia recurrently reaching into the photic zone. A middle Cenomanian sea-level lowstand event followed by transgression left a series of bonebeds within the Belle Fourche Member of the Ashville Formation, indicating a sedimentary environment starved of coarse siliciclastics. Maximum sea level resulted in the formation of limestone beds within the Favel Formation, further favoured by reduced terrigenous sediment input compared to the western margin. Limestone sedimentation was followed by a phase of increased freshwater input under lower sea level conditions, and reducing zoo- and phytoplankton diversities. During final Greenhorn regression, eastern Saskatchewan probably turned into a restricted basin severely limiting marine circulation. Poor or absent benthic foraminiferal assemblages and biomarker analysis suggest prevailing watermass stratification throughout the Cenomanian/Turonian transgressive/regressive cycle. This was caused either by a freshwater lid, stratification of Boreal and Tethyan-derived watermasses, or both, to various intensities affected by changing sea level. Basin oxygenation during Niobrara time varies between localities along the eastern margin as documented by presence/absence of benthic and planktic foraminifera.     

Lithostratigraphy and facies development of upper cretaceous carbonates in east central Sinai,Egypt

Summary The Upper Cretaceous exposures in east central Sinai are represented by carbonate-dominated successions interbedding few sandstone, chert, shale and marl horizons. The recognised rock units are correlated with their counterparts commonly used in the Gulf of Suez region and central Sinai including from base to top: the Raha Formation, Abu Qada Formation, Wata Formation, Matulla Formation and the Sudr Chalk. Twelve limestone microfacies are encountered and are categorised as mudstones (pelmicrite and ostracod micrite), wackestones (pelagic biomicrite and foraminiferal biomicrite), grainstones (foraminiferal biopelsparite and oosparite), boundstones (bindstone and framestone), floatstones (coated-grained biomicrudite, rudist biomicrudite and shelly biomicrudite) and rudstones (shelly biosparudite). The dolostone microfacies include fine-medium crystalline ostracod dolostones and shelly dolostones. These microfacies have been compared with the Standard Microfacies Types and their depositional environments are discussed. The encountered litho- and biofacies suggest that the Cenomanian shallow transgressive sea had covered east central Sinai as far south as the Dahab region. By the advent of the Turonian, open marine subtidal conditions prevailed. This was followed by transitional conditions with shoals and tidal bars in the Late Turonian pointing to a regressive phase more pronounced at the southern localities. The rocks of the Matulla Formation were deposited in an oscillating environment of shallow subtidal to intertidal conditions during Coniacian-Santonian. In the Late Santonian and during most of the Campanian-Maastrichtian, sedimentation was influenced by open marine conditions with low sedimentation rates; local shallow subtidal regressive events occurred.     

Benthic foraminiferal assemblages of the Cretaceous platform carbonate succession in the Yavca area (Bolkar Mountains, S Turkey): biostratigraphy and paleoenvironments

The microbiostratigraphic analysis of the three outcrop sections from the Cretaceous inner platform carbonate succession in the Yavca area (Bolkar Mountains) allows to recognize the four local benthic foraminiferal zones. These are: (1) Voloshinoides murgensis and Praechrysalidina infracretacea Cenozone in the Lower Aptian; (2) Pseudorhapydionina dubia and Biconcava bentori Cenozone in the Middle-Upper Cenomanian; (3) Ostracoda and Miliolidae Interval Zone in the probable Turonian, represented by dolomitized limestones without any significant markers; (4) Moncharmontia compressa and Dicyclina schlumbergeri Cenozone in the Coniacian-Santonian. The benthic foraminiferal assemblages correspond to those in other areas of the Mediterranean realm, with the exception of a lack of alveolinids and orbitolinids due to unfavorable environmental conditions (inner platform, restricted shelf). After the regionally well-known emergence during the late Aptian, Albian and early Cenomanian, very shallow subtidal to intertidal conditions were re-established during the middle-late Cenomanian time. The Coniacian-Santonian benthic foraminiferal assemblage shows an increase in diversity and abundance as a result of open marine influence, confirmed by the presence of larger foraminifera (Dicyclina), Rotaliidae and radiolitid fragments. Thaumatoporella and Aeolisaccus-bearing wackestone intercalations still indicate the existence of sporadic restricted environment conditions. The Cretaceous shallow-water platform carbonate succession of the Yavca area is conformably overlain by gray pelagic limestones with calcispheres and planktonic foraminifera. The Campanian flooding of the Bolkar Da? carbonate platform resulted in drowning of the pre-existing biota and facies.     

Biometry of Cenomanian–Turonian placoliths: a proxy for changes of fertility and surface‐water temperature?

Most publications discussing Cenomanian–Turonian calcareous nannofossils focus on abundance fluctuations across the boundary interval. So far, there have been no studies that deal with the influence of palaeoenvironmental changes on the size of common Cenomanian–Turonian nannofossil taxa. The genera Biscutum, Broinsonia, Prediscosphaera, Retecapsa and Watznaueria have therefore been analysed from 19 samples of Cenomanian–Turonian age from the Goban Spur, northeast Atlantic. The genus Biscutum shows a slight decrease of mean length from 4.14 μm in the Cenomanian to 3.94 μm in the Turonian. Broinsonia is marked by a decrease from 6.07 μm in the Cenomanian to 5.64 μm in the Turonian. On the other hand, Prediscospheara increases in size from 4.98 μm in the Cenomanian to 5.61 μm in the Turonian. Two genera (Retecapsa, Watznaueria) show no significant changes in their mean length. The mean size of Biscutum is perhaps controlled by nutrients, where larger specimens may have preferred the more fertile palaeoenvironment of the Late Cenomanian. The size decrease of Biscutum in the Turonian is probably related to reduced nutrient availability. The genus Prediscosphaera spp., may have favoured low‐fertility conditions, as its mean size increases in the Turonian. A worldwide decline of the frequency of Broinsonia spp. during the Cenomanian–Turonian transition implies that this genus is not solely controlled by the nutrient content. The size of Broinsonia spp. may have been therefore influenced by the latest Cenomanian warming event. The increase in sea‐surface temperature may have been unfavourable for Broinsonia spp. as reflected by decreasing mean size and frequency. □Calcareous nannofossils, biometry, morphometry, Oceanic Anoxic Event 2.     

Platform configuration, microfacies and cyclicities of the upper Albian to Turonian of west-central Jordan

We present a comprehensive facies scheme for west-central Jordan platform deposits of upper Albian to Turonian age, discuss Cenomanian and Turonian carbonate cycles, and reconstruct the paleogeographic evolution of the platform. Comparisons with adjacent shelf areas (Israel, Sinai) emphasize local characteristics as well as the regional platform development. Platform deposits are subdivided into fifteen microfacies types that define eight environments of deposition of three facies belts. Main facies differences between Cenomanian and Turonian platforms are: rudist-bearing packstones that characterise the higher-energy shallow subtidal (transition zone) during the Cenomanian, and fossiliferous (commonly with diverse foraminifer assemblages) wackestones and packstones of an open shallow subtidal environment. On Turonian platforms high-energy environments are predominantly characterised by oolithic or bioclastic grainstones and packstones, whereas peritidal facies are indicated by dolomitic wackestones with thin, wavy (cryptmicrobial) lamination. Rhythmic facies changes define peritidal or subtidal shallowing-up carbonate cycles in several Cenomanian and Turonian platform intervals. Cyclicities are also analysed on the base of accommodation plots (Fischer Plots). High-frequency accommodation changes within lower Cenomanian cyclic bedded limestones of the central and southern area exhibit two major cyclic sets (set I and II) each containing regionally comparable peaks. Accommodation patterns within cyclic set II coincide with the sequence boundary zone of CeJo1. The lateral and vertical facies distributions on the inner shelf allow the reconstruction of paleogeographic conditions during five time intervals (Interval A to E). An increased subsidence is assumed for the central study area, locally (area of Wadi Al Karak) persisting from middle Cenomanian to middle Turonian times. In contrast, inversion and the development of a paleo-high have been postulated for an adjacent area (Wadi Mujib) during late Cenomanian to early Turonian times, while small-scale sub-basins with an occasionally dysoxic facies developed northwards and further south during this time interval. A connection between these structural elements in Jordan with basins and uplift areas in Egypt and Israel during equivalent time intervals is assumed. This emphasises the mostly concordant development of that Levant Platform segment.