CRETACEOUS CLIMATE-OCEAN DYNAMICS: FUTURE DIRECTIONS FOR IODP

 

A JOI/USSSP AND NSF SPONSORED WORKSHOP

 

 

CONVENED BY

 

Karen L. Bice, Timothy J. Bralower, Robert A. Duncan, Brian T. Huber,

R. Mark Leckie, and Bradley B. Sageman

 

 

The Nature Place, Florissant, Colorado

July 14-17, 2002

 

 

 

 

 

SESSION CONVENORS

 

1. Cretaceous Climate Record as Revealed by Stable Isotopes - Paul Wilson, Ken MacLeod

2. Biotic Records of Global Change during the Cretaceous - Mark Leckie, Brad Sageman, and Jochen Erbacher

3. Oceanic Anoxic Events: Causes and Consequences - Hugh Jenkyns, Lisa Pratt, Wolfgang Kuhnt

4. Sea Level Record and Mechanisms for Global Eustatic Change - Brian Huber, Mark Leckie, Lonnie Leithold

5. Atmosphere and Ocean Circulation in a Greenhouse World - Karen Bice, Chris Poulsen

6. Environmental and Biotic Consequences of Large Igneous Provinces - Bob Duncan, Tim Bralower

 


INTRODUCTION

 

In recent years, a surge in the amount and quality of paleoclimatic data has renewed interest in Cretaceous climate and ocean dynamics.  New data have provided a more precise picture of paleotemperatures and climate variations, and research on Cretaceous climate has entered an exciting, multidisciplinary phase in which geological, geochemical, geophysical and paleontological data can be integrated between marine and terrestrial realms and into modeling studies, with the goal of better constraining the controls on climate change during intervals of overall warmth. In July, 2002, the JOI-USSSP/NSF-sponsored Workshop on Cretaceous Climate and Ocean Dynamics brought together a mulitnational group of 90 scientists with diverse research interests and expertise (Appendix 1). The conference objective was to summarize the current state-of-the-art in our understanding of Cretaceous paleoclimate and to discuss future priorities. Ocean drilling has been crucial in our advances to date and is critical for the future of research in this field.

 

Social Relevance of Cretaceous Climate Research

Ultimately, our interest in Cretaceous climate stems from the current concern over modern global warming.  Extreme warmth in the middle part of the Cretaceous represents one of the best examples of  "greenhouse" climate conditions in the geological record (Barron, 1983).  Substantial evidence for this warmth includes upper ocean isotopic paleotemperatures of 22-28°C at southern high latitude sites (Huber et al., 1995), bathyal temperatures reaching 20°C in the subtropical North Atlantic (Norris and Wilson, 1998; Fassell and Bralower, 1999; Huber et al., 1999), and a large champsosaurid reptile that was intolerant of freezing conditions discovered at 78°N (Tarduno et al., 1998).  These data suggest that globally averaged surface temperatures in the mid Cretaceous were more than 10ºC higher than today.

Some of the most important earth science questions of our time relate to understanding how human activities may be modifying current and future climates. Will Earth enter another warm climate state due to rising atmospheric greenhouse gas concentrations? If so, what kinds of biota are likely to adapt/evolve and which face extinction? Will a future warm Earth system exhibit climatic and biotic stability or abrupt change and extreme states? Will Earth enter a "permanent" El Niño or will the system exhibit variability that allows for periods of increased/decreased marine productivity? From the standpoint of marine productivity, is upwelling an effective process during a warm climate interval? If not, what is? How much above modern values can tropical sea surface temperatures rise? How accurately do climate models predict the effects of increasing greenhouse gas concentrations? Cretaceous climate studies may be the best key we have to answering these questions.

One of the most critical questions involves how the biosphere will (or will not) adapt to global warming. Because sea level was high, there is a rich terrestrial record for the Cretaceous. This paleontological record serves as a "natural laboratory," an archive of biotic responses to climate change in terms of migration, extinction, adaptation and diversification. Cretaceous research allows us to assess the biotic responses to factors such as warming/cooling, humidity/aridity, and sea level change. The Western Interior Seaway is a particularly useful tableau in which these changes played out because continental impacts are so evident, thereby providing an accessible, high-resolution record with a large signal to uncertainty ratio. The Cretaceous Western Interior Seaway and other epicontinental seas also serve as important archives because the geography of these regions approximates the coastal plain-maritime interface that is today so densely populated and exhibits the fastest rate of population increase.

Of all the past warm climate periods, the Cretaceous may be the one most richly described with respect to its terrestrial fossil and marine chemical records.  These sediments therefore present a special opportunity to investigate how terrestrial and marine environments are coupled on a warmer Earth. Because Cretaceous climate was far from stable, with evident precessional and sub-precessional cycles in both terrestrial and marine records, we have the opportunity to examine climate change within a warm world on several time scales. Cretaceous climate data can therefore help to inform the public about both near- and long-term possible effects of anthropogenic climate changes. This perspective is simply not available in modern and historical records. Although the Cretaceous can not serve as a direct analog for a future greenhouse Earth (because of the very different land-sea configuration), it is clear that Cretaceous sediments may hold the best record with which to improve our understanding of climate variability and biotic responses to change on an overall warm Earth.

 

Challenges in Cretaceous Climate Research

One of the major challenges facing researchers is that most coupled and uncoupled ocean-atmosphere models underestimate the polar warmth that is indicated by mid Cretaceous fossil and geochemical data (e.g., DeConto et al., 2000), especially for Cenomanian-Turonian time when the latitudinal thermal gradient may have been at its lowest.  This failure suggests deficiencies in our ability to properly interpret the warm climate data record, our understanding of greenhouse climate dynamics, and/or deficiencies in the models. In cases where the latter is true, the immediate lesson relevant to future climate change is that these models--the same ones used in much modern climate research--are dramatically underestimating potential future polar warming. Where different models exhibit different greenhouse gas sensitivities, it is only by comparing these models to paleoclimate data that we can begin to say which extreme in CO2 sensitivity may be more reasonable than another. Model-data discrepancies have also highlighted the importance of accuracy in regional modeling and helped us to improve our ability to model the effects of elevation and vegetation on local and regional climates. While the paleoclimate community is challenged by model-data discrepancies, it is also uniquely positioned to evaluate the reliability of models used in future climate research when atmospheric conditions differ from the modern.

While the mid Cretaceous had an extreme warm climate, other times during the Cretaceous, such as the Aptian and Maastrichtian, were characterized by cooler deep water temperatures and possible ice-sheets in East Antarctica.  Evidence for marine regression suggests glacio-eustatic control of sea level during the mid-Maastrichtian (Miller et al., 1999).  Geochemical evidence has also been cited for continental glaciation during parts of the Early and Late Cretaceous (Stoll and Schrag, 1996, 2000). The recognition that the Cretaceous was not a long interval of stable, "equable," warm climate allows us to investigate climate variability on a variety of timescales using Cretaceous records. The long term overall warming trend from the Aptian to the mid Cretaceous extreme warmth, followed by an overall cooling trend to the Maastrichtian is the longest timescale variation to be explained. On shorter time scales, considerable effort is devoted to understanding what drove periods of dysoxic and anoxic marine conditions or oceanic anoxic events (OAEs)--stagnant intervals that corresponded to pulses of extinction and evolution of marine nekton and plankton (e.g., Fischer and Arthur, 1977; Bralower and Thierstein, 1984; Elder, 1991; Erba, 1994; Bralower et al., 1994). On even shorter timescales, we need to explain dramatic variations in subtropical oceans at the precessional scale (Wilson and Norris, 2001).

The Cretaceous was a time of unusually high rates of production of oceanic crust both at spreading centers and through the eruption of Large Igneous Provinces (LIPs) (e.g., Larson 1991; Tarduno et al., 1991; Coffin and Eldholm, 1994) such as Ontong Java and Kerguelen plateaus.  LIPs represent exceedingly large (> 105 km3) outpourings of predominately basaltic magma. The Ontong Java Plateau, for example, represents more than 50 million km3 of basaltic magma extruded onto the seafloor to form a 30 km thick plateau encompassing an area equal to one third of the contiguous United States.  Events of this magnitude are unknown to human experience, but the consequences must have been dramatic.  The release of gases (e.g., CO2, SO2, Cl, F, H2O) from Earth’s interior accompanying such great eruptions likely had significant consequences for the composition of the ocean and atmosphere, affected the evolution and extinction of terrestrial and marine biota (Larson, 1991; Larson and Erba, 1999; Tarduno et al., 1998; Kerr, 1998), and may have played a primary role in oceanic anoxic events.  The mechanisms linking volcanic activity, extinction/evolution and OAEs are, however, yet to be determined.  Recent and future drilling efforts will lead to a firmer understanding of the age and evolution of several LIPs, and a clearer picture of the emplacement mechanism and potential environmental perturbations.

The most significant remaining questions regarding the dynamics and forcing of Cretaceous climate and oceans include: (1) obtaining an accurate reconstruction of Cretaceous climate from proxy records, (2) understanding the mechanics of turnover in biotic communities, (3) determining mechanisms for abrupt and gradual changes in oceanic circulation and triggers for oceanic anoxic events, (4) understanding the controls on eustatic sea level change, and (5) understanding the mechanisms by which oceanic magmatism, especially LIP events, affect ocean and atmospheric chemistry, and thus life history. 

 

Workshop Structure

The challenges and questions outlined above formed the basis of six plenary sessions and keynote addresses (Appendix 2) that served as an overview of our current understanding of Cretaceous climate. On the third day of the meeting, the group went into the field to view evidence of Cenomanian-Campanian tectonic-eustatic marine cycles exposed in the Rock Canyon Anticline near Pueblo, Colorado. The final day of the meeting included break-out group discussions designed to identify the critical questions in four areas and future research directions needed to address these questions. The following report is organized by thematic plenary sessions with a summary of the presentations followed by an overview of remaining questions and avenues for future research.  Finally, we provide a list of drilling targets that will help achieve these goals. Where sources are cited with no publication year given, the reference is to a workshop abstract (2002, Available on the World Wide Web: http://cis.whoi.edu/science/GG/ccod/searchAbstracts.cfm). Another outcome of the meeting is a community web site, which continues to be updated in order to facilitate communication regarding meetings and future drilling. The original workshop web page for the Florissant meeting can be accessed through this site.

 


SCIENTIFIC OBJECTIVES FOR POST-2003 DRILLING

 

Cretaceous Climate Record as Revealed by Stable Isotopes

 

Stable Isotopes Figures with Captions                                 Return to top of Report

 

Overview

Estimating paleotemperatures continues to be a fundamental aspect of Cretaceous isotopic studies. Analyses of exquisitely preserved foraminifera (those that exhibit "glassy" preservation) have invigorated these efforts (Norris et al., Figure 1-1). Glassy Turonian foraminifera from Demerara Rise in the western tropical Atlantic yield the warmest (up to 36°C) sea-surface temperatures (SSTs) yet reported for the entire Cretaceous-Cenozoic (Wilson et al., 2002). These findings support the hypothesised "Cretaceous greenhouse" and strengthen the case for a Turonian Cretaceous thermal maximum (KTM), thereby highlighting a 20–40 m.y. mismatch between peak Cretaceous-Cenozoic global warmth (and sea level) and peak inferred tectonic CO2 production. This mismatch most likely represents either an artefact of an as yet unidentified Turonian pulse in global ocean-crust cycling, or the influence of other factors, such as CaCO3 subduction (Wilson et al., 2002) or ocean gateway change (Poulsen et al., 2003). These results from the tropics have prompted Bice et al. (in review) to re-examine material used to estimate contemporaneous high-latitude SSTs (e.g. DSDP Site 511, Falkland Plateau). In the absence of pronounced regional perturbation from mean Cretaceous sea water d18O (assumed –1‰ SMOW), d18O data from planktonic foraminiferal calcite at this site are indicative of extreme high latitude warmth during the Turonian (up to 32°C, Figure 1-2). Such extreme high latitude warmth seems difficult to explain in the absence of extreme greenhouse forcing (pCO2, 4500 to 7500 ppmv; Bice and Norris, 2003). Yet textural observations, interspecific isotopic offsets, pore water chemistry, and burial history all argue against a diagenetic explanation.  Salinites as low as 27 psu are required to explain the data as a result of freshwater input, but such brackish conditions are inconsistent with the microfossil assemblages.

MacLeod and Huber show that the concept of globally similar climate responses is not borne out by a d18O time series from three sites on Blake Nose in the western North Atlantic. Although the 5-6 million year long Maastrichtian stage is generally thought to have been a time of widespread cooling, there was 4-6°C of apparent warming at Blake Nose (Figure 1-3). Theoretical models and empirical data show that these estimates are conservative because diagenesis was acting in the opposite direction to the trend observed.  Further, low-resolution data from other sites suggests that Maastrichtian warming can be seen throughout the North Atlantic and perhaps extended into Tethys (but not into the Pacific). Thus, ocean basin scale factors that influence regional heat distribution must have played an important role during the Cretaceous. Such regional controls are clearly important today but have yet to be included in Cretaceous studies. If we are going to address these complexities, though, we need data with better temporal and spatial resolution, as well as an improved ability to separate temperature, seawater d18O (dw), and diagenetic effects on carbonate d18O. Clarke and Schouten et al. discuss efforts to separate temperature and dw effects on d18O values using preliminary Mg/Ca data and a new organic-based paleothermometer, respectively.

Another area of Cretaceous isotope studies that has undergone recent re-birth is the quest to improve our understanding of the nature and cause of oceanic anoxic events. Jenkyns and Tsilkos showed that both d15N of bulk samples and total organic carbon exhibit positive shifts in Cenomanian-Turonian black shales. A similar correlation is observed in Quaternary upwelling areas and in Toarcian (Jurassic) black shales and point to elevated productivity and denitrification in the water column over the oceanic anoxic event.  Further, examination of Cenomanian/Turonian boundary sections globally indicates that the original concept of oceanic anoxic events (OAEs), involving global stratigraphically synchronous black shales, breaks down at high-resolution (Figure 1-4). Therefore, we need to move from a lithostratigraphic definition of OAEs to a chemostratigraphic one. d13C records continue to both provide the lynch-pin in this regard and to be interpreted in terms of global partitioning of carbon between reduced and oxidized reservoirs. Pronounced d13C excursions appear to provide reliable markers even though various factors (e.g. palaeoecology, diagenesis and local carbon cycling) can tend to obscure such chemostratigraphic signals. Examining the Cenomanian-Turonian OAE2 in platform carbonates of southern Mexico, Elrick and Molina showed an abrupt -3 ‰ excursion in d13C that immediately preceded a more gradual 3-4‰ positive that is consistently expressed in multiple sections (Figure 1-5). The higher sediment accumulation rates of platform carbonates permits previously unattainable high-resolution data on the relationship between geochemical and physical processes occurring in pelagic and/or hemi-pelagic systems (anoxia, black shale deposition) and those occurring in onshore, benthic-dominated systems. Ludvigson et al. show that OAEs are also associated with environmental changes on land. They used d13C chemostratigraphy to correlate lacustrine carbonates with the marine Aptian-Albian sections. Systematic differences in d13C (~1.5 ‰) between the sections studied are attribute to floral response to moisture stress in the site immediately leeward of the Sevier mountains. d18O curves for the two study sites diverge for the time interval corresponding to OAE1b suggesting a local intensification of aridity associated with oceanic anoxia.

A series of presentations focused on isotopic constraints on the hydrological and carbon cycles in the terrestrial realm. Fricke measured phosphate d18O of dinosaur tooth enamel to infer the d18O of water ingested by the animal and concluded that, relative to the present, the Late Cretaceous of North America was typified by higher temperatures and increased vapour transport to higher latitudes. Parallel d13C measurements on trace carbonate within the tooth apatite suggest herbivorous dinosaur taxa partitioned available food resources.  Both Gonzales et al. and White et al. reported analyses of d18O of pedogenic siderite that confirm enhanced Cretaceous hydrologic cycling and provided quantitative estimates of the increase relative the present and model predictions.  Pratt et al. discussed how d13C studies of lacustrine organic matter could provide better estimates of pCO2 during times when temporal trends in d13C or carbonate and organic matter are de-coupled. One important recent finding is that we have no convincing evidence of C4 plant adaptation by Cretaceous time, even under extreme water stress conditions. A second important recent discovery is the existence of strata with significant concentrations of biomarkers indicative of forest fires. Mass balance considerations indicate that biomass burning is an under-explored explanation for pronounced negative excursions in Cretaceous d13C records. Finally, Finkelstein et al. examined the abundance of fusinite and polycyclic aromatic hydrocarbons (PAHs) in  lacustrine samples from the Late Cretaceous Fort Crittenden Formation. Both are indicative of fire and multiple abundance peaks through the section suggests repeated wildfires or peat fires in the watershed.  Assuming the hydrologic cycle was more vigorous, a seasonally wet paleoclimate could have resulted in biomass build-up and hotter fires, enhanced landscape denudation, and accelerated erosion in the watershed post fires, thus, explaining the correlation between turbidites and indicators of fire.

 

Future Directions

Worshop participants identified the following as critical needs in the areas of d18O paleothermometry and d13C records:

 

d18O Paleothermometry:

 

1) To fully evaluate the roles played by taphonomy, palaeoecology and non-equilibrium behaviour in Cretaceous palaeothermometry.

 

2) To increase stratigraphic and geographic resolution of our records and thereby assess the issue of the stability of warm climates

 

3) To determine the full magnitude of high-latitude warmth during  peak greenhouse forcing

 

4) To integrate d18O data with additional palaeo-temperature proxies  (e.g. Mg/Ca)

 

5) To further examine the issue of d18Osw in the context of sensitivity to short-term changes in continental ice volume and long-term changes in hydrothermal weathering regimes.

 

6) To improve our understanding of the paleohydrological cycle.

 

d13C Records:

 

1) To generate more multi-substrate records (e.g. benthic-planktic foraminiferal pairs, CO3-Corg) and thereby assess competing hypotheses for carbon cycle perturbations

 

2) To improve the stratigraphic resolution and reduce errors associated with pCO2 estimates

 

3) To improve our understanding and records of new isotope proxies for pCO2 and weathering (e.g. d11B; 187Os/188Os).

 

Because of the need to access undisturbed, expanded sections containing well-preserved microfossils, IODP is the key platform for advancing our understanding in these areas. One priority for future drilling is the need for a high-latitude counterpart for forthcoming ODP Leg 207. The depth-transect approach (cf. sea level section) will continue to be an important strategy.

 

 

Biotic Records of Global Change during the Cretaceous

 

Biotic Records Figures with Captions                  Return to top of Report

 

Overview

      The patterns of how life responds to the Earth's changing environments can provide important insights into the processes and rates of global change, and biotic records provide an independent and complementary proxy to geochemical tools. Tectonic forcing of climate and ocean fertility had a profound impact on terrestrial and marine ecosystems and the evolution of life during the Cretaceous. At times, greater emissions of CO2 led to increased weathering of the continents and greater delivery and availability of nutrients in the marine realm. In addition, there were possible linkages between increased hydrothermal activity on the seafloor and enhanced productivity in the surface waters (e.g., late Valanginian and mid-Cretaceous Oceanic Anoxic Events). Climate fluctuations due to greenhouse warming or reverse greenhouse cooling as a feedback to excessive burial of organic carbon, were further modulated by eustatic sea level fluctuations and albedo effects. Changing Cretaceous paleogeography created new opportunities for many groups of organisms. However, other ecosystems were stressed with the opening and closing oceanic gateways, redistribution of heat by the ocean-climate system, and the partitioning of nutrients between land and sea, and surface and deep ocean.  A number of themes emerged from the diverse array of abstracts submitted; these can be grouped by major ecosystems and by key intervals or events during the Cretaceous.

 

Pelagic Ecosystems: Since the Late Triassic, when the nannoplankton began to produce calcareous platelets thereby causing a major shift in carbonate deposition from the shelves into the deep oceans, this diverse and abundant group of unicellular, planktonic marine algae have been intimately linked to global change. In modern oceans, it has been demonstrated that the distributions of certain sensitive nannoplankton taxa mirror discrete water-masses, the existence of which is a function of ocean circulation and climate. Thus, global climate exerts, and must have exerted in the past, a major influence over calcareous nannoplankton and their distributions (Lees).

Lees delimited nannofossil palaeobiogeographic zones (PBZs) for the Late Cretaceous Indian and Pacific Oceans. These latitudinally-distributed PBZs are interpreted as indicating discrete water-masses, possessing differing temperature and nutrient properties. Movements of the fronts separating these PBZs through time can be used as proxies to primarily indicate warming or cooling trends (Figure 2-1). Comparison of available oxygen isotope sea-surface temperatures (SSTs) with the PBZ-derived warming and cooling trends shows a good correlation between the two proxies, underlining the utility of nannofossils as proxies for Mesozoic climate change.

Bown analyzed coccolithophorid and other calcareous nannoplankton evolution and diversity patterns through the Cretaceous. The data reveal no clear relationship between long-term diversity trends and previously recognized major global environmental change events in the Cretaceous. Oceanic Anoxic Events 1a (early Aptian) and 2 (latest Cenomanian) occurred well within nannoplankton diversity minima and were followed in both cases by periods of protracted diversity increase. However, the most rapid increases in diversity broadly correlate with cooler climate intervals. In particular, Bown suggests that enhanced species diversity in the Campanian was related to the onset of late Mesozoic climatic cooling with much of the diversification the result of greater palaeobiogeographic differentiation including the evolution of high-latitude-restricted phytoplankton.

The first radiation of planktonic foraminifera was thought to begin close to the base of the Aptian. However, Premoli Silva demonstrates that this group started to diversify much earlier. The first diversification occurred in the early Valanginian with the appearance of the first hedbergellids. This small fauna in both species number and size seems to persist without apparent changes through most of the Hauterivian, the end of which is characterized by an abrupt short flourishing of the gorbachikellids. The earliest Barremian coincided with a remarkable increase both in abundance and number of planktonic species and genera that continued through the Barremian accompanied by an overall increase in size (Figure 2-2). This trend continued through the early and mid-Aptian with a further increase in number of species and overall abundance and size of specimens after the early Aptian Oceanic Anoxic Event 1a (OAE1a). This increase was accompanied by the progressive appearance of more ornamented morphotypes. Premoli Silva found no turnover in planktonic foraminifera coinciding with OAE1a. The OAE1a represented only a temporary paleoenvironmental perturbation characterized in the upper water column by alternating low oxygen levels (proliferation of leupoldinids), to slightly richer oxygen levels (clavate morphotypes) or to better oxygenated waters (round-chambered taxa) (Figure 2-3). The effects of the perturbation related to the OAE1a appear to have terminated only about one million years after the event.

 

Tropical Ecosystems: Changes in the environment have modified the ecological role of reef builders through geologic time, and major extinctions have reset evolutionary patterns. In Cretaceous reefs, the relative ecologic role of scleractinian corals and rudist bivalves shifted during the mid-Cretaceous, and rudist bivalves took over as the dominant skeletal organisms for the remainder of the period (Johnson). The  role of bivalves as proxies for reefal conditions remains questionable. Johnson statistically analyzed the paleobiogeographic distributions of scleractinian corals of the Caribbean and circum-Caribbean region for all stages of the Cretaceous (Figure 2-4). Dispersion patterns for corals and rudists infer that the geographic extent of the Cretaceous tropics was greater than that of our present-day interglacial period. Knowledge of the paleolatitudinal extent of the ancient tropics is essential for analyzing the role of the tropics in ocean and atmospheric heat transport.

 

Terrestrial Ecosystems: The statistical relationship between leaf physiognomy and climate for modern plants is widely used by paleobotanists to reconstruct Late Cretaceous climate. Methods such as simple linear regression (SLR) and multiple regression (MR) are used to derive leaf/climate relationships for modern floras, which then are used to estimate temperature and precipitation from paleofloras. When applied to modern test sites, physiognomic methods provide good "ballpark estimates" of mean annual temperature (MAT) and mean annual precipitation (MAP) but can show significant discrepancies between estimated and measured climate. The magnitude of the discrepancy (up to 5°C for MAT) is determined by the choice of equation used to quantify the leaf/climate relationship, referred to here as the physiognomic transfer function (Scherer).

To determine the extent to which estimates of Cretaceous climate are biased by the choice of physiognomic transfer function, Scherer applied a variety of published physiognomic transfer functions to a well-preserved leaf megaflora from the latest Cretaceous (Maastrichtian) Jose Creek Member of the McRae Formation, southern New Mexico. For the Jose Creek assemblage, calculated MAT is 16-25°C and calculated MAP is 600-1200 mm/yr, a range of over 8°C for MAT and 600 mm/year for MAP. Variation in calculated temperature and precipitation, relative to the mean of all estimates, can exceed + 35%. However, the range of values is congruent with more qualitative estimates of climate derived from paleosols and plant life form, which indicate a warm subhumid subtropical climate for the Jose Creek Member. This implies that physiognomic transfer functions are probably accurate to the level of climate zone.

Terrestrial climates near the time of the end-Cretaceous mass extinctions are poorly understood. Wilf et al. estimated and correlated paleotemperatures for the terminal Cretaceous  (~66.7 to 65.5 Ma), using megafloral data from North Dakota and foraminiferal data from four middle- and high-latitude sites. Both plants and foraminifera indicate warming near 66.0 Ma, a warming peak from ~65.8 to 65.6 Ma, and cooling near 65.6 Ma to pre-warming temperatures, which lasted into the early Paleocene (Figure 2-5). At similar temperatures, Cretaceous floras from North Dakota were rich, but Paleocene floras were impoverished. Climatic and facies changes are insufficient explanations for plant extinctions in this area, which we attribute to the effects of bolide impact (Wilf et al.).

 

High Arctic: The Cretaceous of the Canadian High Arctic is represented by sedimentary and volcanic rocks of the Sverdrup Basin that are exceptionally well exposed on Axel Heiberg and Ellesmere Islands. These sequences contain evidence for short-term episodes of extreme warmth and cooling during the Late and Early Cretaceous, respectively (Tarduno et al.). A Turonian to Coniacian (~92 to 86 Ma) vertebrate assemblage from a site with a paleolatitude of approximately 71˚N implies that polar climates were warm (mean annual temperature exceeding 14˚C; Tarduno et al., 1998). This episode may correlate with evidence for extreme high-latitude warmth from oxygen isotope paleotemperature estimates from the Southern Ocean (Huber, 1998). The Arctic assemblage includes large (>2.4 m) champsosaurs, which are extinct crocodile-like reptiles. The vertebrate fossils overlie subaerially erupted flood basalts of the Cretaceous Strand Fiord Formation. These lavas are part of a large magmatic pulse (or large igneous province) that may include large parts of Ellesmere Island and the Arctic Ocean basin. This magmatism, coupled with coeval volcanism at six other large igneous provinces, suggests that volcanic carbon dioxide emissions may have helped cause the peak in global warmth. In contrast to the extreme warmth of the Late Cretaceous, Arctic sedimentary rocks of mid- and Early Cretaceous age show evidence of cool conditions in the form of glendonite horizons. Glendonites (pseudomorphs after the hydrated calcium-carbonate mineral ikaite), are associated with glacial marine sediments of Permian to recent age (Figure 2-6). Preliminary biostratigraphic, magnetostratigraphic and geochemistry data of Tarduno et al. suggest that Valanginian age glendonite horizons represent relatively short (<100-400 kyr) episodes at a time of low eustatic sea level.

 

Epicontinental Seas: Fisher applied an innovative technique to reconstruct the temperature and circulation of ancient surface water masses from the Cretaceous Western Interior Sea. Foraminifera construct more porous shells in warmer waters and less saline waters. Modern planktic foraminifera are less diverse at lower salinities, so shell porosity of diverse ancient planktic foraminiferal assemblages must be primarily in response to paleotemperature. Both properties are largely responsible for water density, and therefore porosity may be a proxy for relative water mass density, which is useful in interpreting paleo-ocean circulation. Specimens of the widely distributed mid-Cretaceous species Hedbergella delrioensis have been temporally studied through several sections and spatially studied along time-lines from many geographic localities across the Cenomanian-Turonian Greenhorn Sea. Stratigraphic studies show that porosity increases from the upper Cenomanian into the lower Turonian. The porosity increase is coincident with previously proposed sea level rise. The porosity increase is interpreted as an increase in the influence of warm water that entered from the Tethyan Ocean (Figure 2-7). Geographic studies along time-lines reveal high porosities in the central seaway, with porosity decreasing shoreward and northward. The distributions are interpreted as a stratified seaway, consisting of a warm central near-surface watermass underlain by deeper waters that surfaced shoreward and northward. As sea level rose the warmer central core expanded north and shoreward (Figure 2-8). If porosities are used as relative density proxy data, contour maps of porosity can be used to reconstruct geostrophic flow.

 

Late Valanginian Productivity Event: Using quantitative analyses of calcareous nannofloras and geochemistry, Tremolada et al. showed that the calcareous nannoplankton group nannoconids experienced a sharp decline across a globally documented positive carbon isotope excursion in the Berrisian-Hauterivian in northern Italy. The nannofossil assemblages of the late Valanginian are dominated by W. barnesae, with relative increase of Diazomatolithus spp., probably indicating higher fertility conditions as further supported by the decline in the oligotrophic nannoconids. Rising Sr/Ca ratios in the upper Valanginian carbonates supports the interpretation of enhanced productivity. This increase slightly leads the carbon isotope excursion, and is coeval with the onset of the nannoconid decline. According to Tremolada et al., the nannoconid decline and productivity increase probably were induced by changes in nutrient content caused by the Early Cretaceous volcanic activity connected with the emplacement of the Paranà Plateau and the "pulse" in the seafloor production. These volcanic and tectonic events provoked excessive CO2 levels in the atmosphere favoring warm and humid conditions that induced an accelerated transfer of nutrients from the continents to the oceans increasing the fertility of surface waters. Also, a nutrification event might have been directly caused by hydrothermal processes connected with the igneous activity (Figure 2-9).

 

Biotic Response to Oceanic Anoxic Events: Leckie et al. (2002) documented the evolutionary patterns of calcareous plankton (planktic foraminifera and calcareous nannoplankton) during the mid-Cretaceous (Barremian-Turonian stages, ~124-90 Ma). When combined with the radiolarian record through the same interval (Erbacher et al., 1996), there is compelling evidence that the highest rates of evolutionary turnover, i.e., speciation plus extinction, occur at or near the major Oceanic Anoxic Events. These episodes of widespread organic carbon burial occur in the early Aptian (~120.5 Ma; OAE1a), across the Aptian/Albian boundary (~113-109 Ma; OAE1b), in the latest Albian (~99.5 Ma; OAE1d), and across the Cenomanian/Turonian boundary (~93.5 Ma; OAE2). Strontium isotopic evidence suggests a possible link to times of rapid oceanic plateau formation and/or increased rates of ridge crest volcanism (Bralower et al., 1997; Jones and Jenkyns, 2001; Leckie et al., 2002). The association of plankton turnover and carbon isotopic excursions with each of the major OAEs suggests widespread changes in the ocean-climate system (Figure 2-10). The episodes of accelerated evolutionary activity in the plankton have been attributed to changing upper water column structure, increased delivery of nutrients including dissolved iron, greater oceanic productivity, and carbonate dissolution (Erba, 1994; Erbacher et al., 1996; Leckie et al., 2002). Leckie et al. (2002) concluded that plankton evolution was tectonically-forced, particularly by increased submarine volcanism and hydrothermal activity, due to tectonic influences on global climate, ocean chemistry, nutrient availability, ocean circulation, and water column structure.

According to Erba, OAE1a (late Early Aptian) and OAE2 (latest Cenomanian) correlate with the onset and end of the mid-Cretaceous greenhouse climate, interrupted by some brief cooling episodes in the Aptian to Cenomanian interval alternating with extremely warm conditions leading to black shale deposition during OAEs. High-resolution stratigraphy indicates that biotic events correlate with major igneous/tectonic events. Both OAE1a and OAE2 are interpreted as high productivity episodes probably induced by high concentrations of dissolved and particulate biolimiting metals in the oceans and increased CO2 in the atmosphere during submarine volcanism (Ontong Java and Manihiki Plateaus, and Caribbean plate, respectively). Mid-Cretaceous OAEs and cooling episodes seem correlatable with subaerial volcanism related to the formation of Kerguelen Plateau and Broken Ridge (Figure 2-11).

Changes in the nature of oceanic surface water masses during Oceanic Anoxic Events (OAE) were significant drivers of phytoplankton evolution. As an example, Watkins analyzed well-preserved nannofossil assemblages in upper Albian and lower Cenomanian hemipelagic sections from Ocean Drilling Program (ODP) Leg 171b, which record the early history of the establishment and adaptive radiation of the genus Eiffellithus. Seven distinct taxa evolved during the relatively short interval from 101.5 to 100.0 Ma. Newly evolved species tended to remain at low abundance levels until a significant disruption in the pelagic realm resulted in the precipitous decline of the dominant species. These major disruptions correspond to significant changes or shifts in the sedimentological and carbon isotopic records associated with late Albian OAE1d. The close correspondence of species originations, changes in dominance, and species extinctions to changes in sediment TOC and significant carbon isotope shifts indicates that the variability in the surface water mass during OAE1d was the principle environmental forcing mechanism behind the adaptive radiation of this genus during the late Albian (Watkins).

Holbourn and Kuhnt examined records of well preserved benthic foraminiferal assemblages across Cretaceous OAE1a, OAE1b, OAE1c and OAE2 from North Atlantic bathyal and abyssal DSDP/ODP Sites and from bathyal to neritic onshore sections in Morocco, Spain, southeast France and northern Germany (Figure 2-12). Diversity, taxonomic composition and preservation potential of benthic foraminiferal assemblages at shelf localities are strongly influenced by changes in paleo-water depth, particularly at times of major sea level change. Thus, most of the observed faunal changes at shelf sites express environmental change and taphonomic bias, rather than true extinction and radiation events. They found no evidence for a major benthic foraminiferal turnover during OAE1 and OAE2 at middle and upper bathyal sites (Figure 2-13). Most taxa recorded at these locations have stratigraphic ranges extending across oceanic anoxic events. The changes in biofacies recorded across the OAEs coincide with changes in hydrography and sedimentological facies. By contrast, abyssal benthic foraminifers underwent a marked radiation after the latest Cenomanian OAE2 in the Atlantic Ocean and the Mediterranean Tethys, which may be triggered by a general change towards better oxygenated deep-water.

With ammonite/inoceramid species loss of up to 85% in the Western Interior basin, the Cenomanian-Turonian boundary event represents a significant biotic crisis (Meyers and Sageman). Hypotheses proposed for the driving mechanism of species turnover include mainly changes in benthic and water column oxygen levels associated with OAE2, and changes in substrate consistency associated with limestone-marlstone alternation. Meyers and Sageman examined the main hypotheses for biotic turnover in light of new sediment and geochemical accumulation rates, as well as recalculated evolutionary rates across the stage boundary. These new rates are based on a high-resolution time scale developed through cyclostratigraphic analysis of the Cenomanian-Turonian Bridge Creek Limestone Member. The new high-resolution time scale facilitates an independent quantitative assessment of the rates of accumulation of environmentally sensitive geochemical proxies, and calculation of rates of evolutionary change in the C-T boundary interval. A series of major modal switches in sedimentation are identified. These modal switches may represent fundamental changes in the ocean-climate-sediment transport system. Interestingly, the highest rates of extinction do not correspond to intervals with the greatest indication of sulfidic conditions (Figure 2-14). Further comparisons of paleoenvironmental data with molluscan evolutionary rate allow evaluation of alternate biotic controls, such as substrate consistency, turbidity, and nature/frequency of environmental disturbance (Meyers and Sageman).

 

Future Directions

Based on data obtained from continental records and ocean drilling, considerable progress has been made in the last two decades toward describing and explaining Cretaceous biosphere changes. However, important unsolved problems remain in our understanding of the ocean-climate system and its impact on the biosphere. How is widespread marine biological productivity sustained for 104-105 years? How important was 400 kyr and 100 kyr cyclicity in controlling sedimentary and biotic patterns? Did metals or other trace elements play a major role in the Oceanic Anoxic Events of the Early Cretaceous and mid-Cretaceous? What was the relative role of greenhouse warming vs. reverse greenhouse cooling in controlling the availability of nutrients, burial of organic matter, water mass production, and biotic evolution during the mid-Cretaceous? What is the relative importance of upwelling vs. continental runoff as a nutrient supply mechanism and how might this have varied through different climate events? What were the rates of climate change during the OAEs? What was the frequency and extent of wildfires, and what was their impact on the carbon cycle?

 The rich Cretaceous terrestrial record, increasingly well-characterized marine records, and an increasing number of proxies and model approaches will allow us to better understand terrestrial and marine responses to internal and external climate change. Workshop participants emphsized the need to better integrate terrestrial and marine records using transects across the land-sea transitions. Lacustrine deposits were identified as a possibly under-utilized source of information. The increasing use of organic biomarkers for molecular "fingerprinting" should yield important information about community makeup and environments. Given the vast amount of hydrocarbons sourced from Cretaceous sediments, the portion of our community applying biogeochemical approaches might especially benefit from greater collaboration with the petroleum industry.

 

 

Oceanic Anoxic Events: Causes and Consequences

 

OAE Figures with Captions                                             Return to top of Report

 

Overview

 The discovery of black carbon-rich shales in deep-sea drilling sites from the Atlantic, Indian and Pacific Oceans (from DSDP Leg 1 onwards) led in the mid-1970s to the concept of Oceanic Anoxic Events.  Such events, whatever their exact nature and cause, were hypothesized to foster deposition of coeval carbon-rich sediments across environments ranging from deep oceans to shelf seas.  The original concept was primarily stratigraphic in nature, being based on the implicit assumption that the world ocean underwent a fundamental chemical and/or biological change during such events: enhanced productivity of organic-walled microfossils and bacteria and/or enhanced preservation of organic matter were both suggested as likely causes.  Among the plethora of black-shale horizons identified both on land and in the oceans, two major organic-rich horizons, one dated as early Aptian (Selli Event: OAE1a), the other at the Cenomanian-Turonian boundary (Bonarelli Event: OAE2), have proven to be of global distribution.  Both of these, for example, are recorded from submarine plateaus in the Pacific Super-Ocean, most recently the black shale of the Selli Event drilled on Shatsky Rise during ODP Leg 198. This extremely carbon-rich horizon (~35% TOC) contains biomarkers for cyanobacteria that could have utilized atmospheric elemental dinitrogen - as happens in some extreme upwelling environments today - if nitrate levels in the photic zone became vanishingly low because of utilization by plankton (Brassell, Figure 3-1).  This discovery points to upwelling and high productivity as a major forcing function behind the causality of Oceanic Anoxic Events.

Nitrogen-isotope data from Cenomanian/Turonian black shales from Italy and Morocco simi­larly are consistent with sedimentation below a water column that had undergone denitrification (Jenkyns and Tsikos), as is the case today in zones of vigorous upwelling, intense oxygen minima and high fluxes of planktonic carbon to the sea floor. Other events, particularly the Paquier Event (OAE1b) are more local, being confined - as far as we know at present - to the Atlantic-Tethyan domain.

Phil Meyers showed that low d15N values in black shales, values that falsely mimic land plant compositions, may reflect a combination of processes leading to elevated production and improved preservation of marine organic matter. Marine productivity is usually limited by availability of dissolved nitrate, but if a mid-water anoxic zone expands upward and enhances recycling of phosphorus into the photic zone, then nitrogen-fixing cyanobacteria can flourish. These organisms photosynthetically produce organic matter having a d15N value close to atmospheric nitrogen (0).  So, while the d15N values of most Mesozoic and Cenozoic marine sediments usually range between 4 and 8 ‰, Rau et al. (1987) reported d15N values of –2 to 3  in black shales from DSDP Sites 367, 530, and 603 (Figure 3-2).

From a study of isotopes and palynology of this Oceanic Anoxic Event from three sec­tions in the Central Atlantic and western Tethys, Erbacher and Herrle conclude: 1) that the aver­age duration of OAE1b was 45 ky; 2) a strong monsoonal circulation resulted in a dominance of the precessional signal (fertility); 3) fertility changes were superimposed on longer-term temperature cycles corresponding to the eccentricity signal; and 4) that OAE1b falls into an extremely warm and humid phase of an eccentricity cycle (Figure 3-3).  This event was probably a factor of 10 times shorter in duration than was OAE2. OAE3 (Coniacian-Santonian) again seems a more parochial affair (Wagner et al., Figure 3-4) with a record dominantly deriving from the Atlantic.  The question must be asked: is it actually useful to consider these organic-rich strata as being produced by an Oceanic Anoxic Event?  Is some minimum geographic extent of a black-shale unit required in order to qualify as the product of an OAE?

The advent of carbon-isotope stratigraphy in the nineteen eighties, with the recognition of a characteristic positive excursions related to excess global carbon burial, offered a proxy for the partitioning of the global carbon pool between oxidized and reduced reservoirs.  Recent carbon- isotope studies from England, Japan, Italy, Morocco and elsewhere now demonstrate that the both the Aptian and the Cenomanian/Turonian black shales are associated with such a positive carbon- isotope excursion in marine pelagic and shallow-water carbonate, marine organic matter and ter­restrial higher-plant material (Jahren, Hasegawa, Heimhofer et al.; Figures 3-5, 3-6, 3-7).  The Aptian event, paradoxically, is also associated with a pronounced negative carbon-isotope excursion, recently interpreted as due to dissociation of methane hydrates, a theme explored by Hope Jahren in her presentation. Because these characteristic carbon-isotope excursions, both positive and negative, can be found in deep-marine, shallow-marine and non-marine facies, they offer a novel means of correlation between sediments deposited in the oceans and on the continents. Palaeoclimatic data from conti­nental interiors may now be integrated with the wealth of data from deep-sea cores to produce a potentially global view of climate change during critical events in earth history.  The Aptian nega­tive isotope excursion is not unique in the Cretaceous: a similar phenomenon has been found in Atlantic and Tethyan sections predating the Paquier Event (Gröcke).  The question then has to asked: what is the exact relationship, if any, between OAEs and negative carbon-isotope excur­sions, when excess global carbon burial must produce a positive excursion? Perhaps both phe­nomena - OAEs and methane-dissociation events - are responding to increases in CO2-forced global temperature, the former being related to fundamental changes in the hydrological cycle, nutrient inputs, oceanic recycling, the latter to changes in the stability field of methane hydrate dependent on bottom-water temperatures.  CO2 could have been added to the atmosphere from volcanogenic sources as well as from oxidation of methane: and in one sense OAEs can be seen as the means by which the ocean-atmosphere returns to a pre-existing equilibrium. Massive seques­tration of organic carbon during the OAE would draw down CO2, return the atmosphere to pre-OAE conditions and produce global cooling.

In detail the exact relationship between the isotope curve and the total-organic-carbon stratig­raphy of any one section is complex.  The black shale or, more particularly, its most carbon-rich portions, is not fixed in exactly the same position with respect to carbon-isotope curve: in some localities the onset of the positive excursion coincides with the beginning of black-shale deposition, in others it does not.  This mismatch is seen, for example with the Cenomanian/Turonian in the Western Interior (Sageman and Meyers; Figure 3-8) where organic-carbon accumulation rates actually seem to have increased after the OAE - the OAE being defined by the duration of the carbon-iso­tope excursion.  In Italy, however, the carbon-isotope excursion begins abruptly at the base of the Bonarelli Level itself.  Hence, at these high levels of resolution, the "stratigraphic" concept of the Oceanic Anoxic Event breaks down.  But more importantly this is telling us that the most significant carbon sinks during the Cenomanian/Turonian OAE have yet to be identified, although there is some evidence that a (maybe the) major locus of organic-matter deposition was the proto-South Atlantic (Forster et al., Figure 3-9).

The Late Cenomanian oceanic anoxic event (OAE2) is the most extensive of the Mid-Creta­ceous OAEs. The duration of OAE2 was originally estimated based on biostratigraphic evidence and interpolation of geological timescale data points between 0.5 - 0.8 m.y. (Arthur et al., 1988) and 0.4 m.y. (Caron et al., 1999). Recently, orbital cyclicity has been used to estimate the duration of the event. These estimates range from 720 k.y. in Colorado (Meyers et al., 2001), approx. 400 k.y. (Kuhnt et al., 1997) in the Tarfaya Basin (Morocco) to 320 K.y. in western Canada (Prokoph et al., 2001).  The OAE2 is characterised by a large positive global carbon-isotope excursion in both carbonate and organic matter, caused by a major perturbation of the global carbon budget, probably due to the extensive burial of organic matter in black shales (Schlanger & Jenkyns 1976; Arthur & Schlanger 1979; Jenkyns 1980; Scholle & Arthur 1980; Herbin et al. 1986; Arthur & Schlanger 1987; Arthur et al. 1988; Weissert & Lini 1991; Jenkyns et al. 1994). This period of extensive carbon burial was coeval to a significant extinction event in the marine plankton, i.e. the extinction of the first clade of keeled planktonic foraminifers, the genus Rotalipora.

The OAE2 represents a major turn in earth climate history (Jenkyns et al. 1994; Norris & Wilson 1998). Decreased ocean-volume due to enhanced spreading rates and larger mid-ocean ridge volume had led to a eustatic sea level rise of 130-350 m since the early Aptian (Kominz 1984; Larson 1991a,b) and the worldwide formation of shallow, warm, epicontinental seas (Brass et al. 1982). Atmospheric CO2-partial pressure was 3-12 times higher than today due to volcanic outgassing (Larson 1991b; Berner 1991) and many terrestrial and marine paleoclimate-proxies suggest that the mid-Cretaceous was the warmest period in the last 200 m.y. (Frakes et al. 1992; Barron et al. 1995; Huber et al. 1995). The high surface temperatures resulted in enhanced evaporation within shallow, warm epicontinental seas and an intensification of the water-cycle and increased nutrient fluxes  (Föllmi et al. 1994). Recent evi­dence indicates that OAE2 was accompanied by a 40-80% reduction in CO2 levels (Kuypers et al., 1999). This was suggested to be due to a rapid increase in accumulation rates of organic mat­ter in the subtropical Atlantic Ocean and Tethyan marginal basins (Arthur et al. 1988; Kuhnt et al., 1990; Jenkyns et al. 1994; Kuypers et al. 1999). However, due to generally low sedimentation rates or even hiatuses in the late Cenomanian, a precise succession of events (carbon burial, reduction of pCO2, carbon isotope excursion, biotic extinctions and sea surface temperature changes) has never been established, leaving wide space for speculation about causal relation­ships.

 

Future Directions

Future research on OAEs must continue to characterize the environmental conditions that led to the deposition of organic-rich sediments.  Proxies that can provide direct information on nutrients in surface waters, atmospheric CO2 levels, and the original composition of biotic populations from microbes to  invertebrates, are desperately needed.  Multidisiplinary investigations must focus on events that perturbed the global ocean such as the OAEs in the early Aptian (OAE1) and the late Cenomanian (OAE2), as well as those that appear to be more regional in scale  such as OAEs 1b, 1c, and 1d.  There are a number of important questions that can best be addressed through ocean drilling:

·        What is the geographic and oceanographic distribution of these events?

·        What controls their spatial distribution and the rate of changes (chemical, physical, biological) during the event?

·        What preconditioning (tectonic, climatic, orbital) determined the time scales of the different OAEs and sustained them?

·        What are the triggering mechanisms and their manifestation, e.g. is there a role for methane?

·        What is the relationship between OAEs, ocean temperature changes and links to sea level?

·        What happened to the water column (physically, chemically, biologically) and the upper sedimentary column?

·        How did the organic matter (sources, preservation, productivity), nutrients and ocean structure change? How was that affected/stimulated by oxygen minima, euxinia, dysoxia?

·        What is the impact on the carbon cycle and its budgets, reservoirs and fluxes through the various OAEs?

·        What is the expression of these events on the continents (e.g. in lakes) versus shelf areas and the deep ocean?

 

Drilling Priorities

To address many of these questions in a rigorous fashion will require sections with a broader geographic distribution than those currently available. Dedicated drilling legs are required to obtain multiple core records of these critical intervals. Moreover, there must be a concerted effort to identify records of OAE in expanded, immature sections that will allow high-resolution studies at a millennial scale. Drilling priorities include the high latitudes (especially Arctic) transects from continent to the deep sea, and progressively "downstream" from Large Igneous Province eruptions.

 

 

Sea Level Record and Mechanisms for Global Eustatic Change

 

Sea Level Figures with Captions            Return to top of Report

 

Overview

One of the long-standing controversies about Cretaceous climate regards how short-term, global variations in sea level could have occurred during a "greenhouse" climate that is assumed to have been ice-free. The assumption of a warm, ice-free earth during the Cretaceous has been based on a variety of geochemical, sedimentologic, and paleontological evidence that oceanic and continental temperatures were much warmer than at present in the north and south polar regions. On the other hand, correlations between oxygen isotopic data, strontium concentrations, sedimentologic observations, and interpreted sea level variations have been proposed as evidence that polar ice-sheets did exist at various times during the Cretaceous. The "Cretaceous Sea level Record and Mechanisms for Global Eustatic Change" session was organized to evaluate evidence from both sides of this controversy and determine what approaches are needed to reconcile the divergent interpretations. The talks and posters presented in the session revealed tantalizing evidence for correlations between changes in sea level and geochemical shifts that are consistent with ice volume variation at several intervals during the Cretaceous. However, more evidence for global synchroneity of these records is needed before an ice-sheet forcing mechanism will be widely accepted.

 

The session presentations can be divided into the approaches that were used to examine the possibility of glacio-eustasy during the Cretaceous:

·        Development of new experimental tools for determining the temperature of Cretaceous water masses

·        Analysis of inorganic geochemical proxies that may have been influenced by ice-sheet growth and decay

·        Sedimentologic and biotic evidence for sea level variations at Milankovitch time scales

·        Climate modeling

 

Experimental Paleothermometers: Linear correlation between seawater temperature and a successively increasing number of cyclopentane rings in tetraether membrane lipids that are biosynthesized by a group of marine bacteria (crenarchaeota) has been demonstrated in field and laboratory studies. This "TEX86" proxy may serve as an alternative to established sea-surface temperature (SST) proxies (such as UK37 or d18O of carbonates) for sediments dating to the Albian, which is when the membrane lipids of marine crenarchaeota are known to have first appeared. Initial testing of this method on ancient sediments suggests that early diagenesis and sediment maturity do not influence the paleotemperature signal, but further testing is needed to determine the possibility of biasing paleoenvironmental factors. Assuming that biasing effects were negligible, application of the TEX86 proxy to Cenomanian-Turonian sediments at DSDP Site 367 reveals that tropical SSTs may have been up to 6°C warmer than at present (Figure 4-1).

Analysis of Mg/Ca ratios in marine carbonate is another method that is beginning to be used to estimate Cretaceous marine paleotemperatures. This approach was applied to sediments that span the Aptian/Albian boundary at ODP Hole 766A. Preliminary results suggest that the apparent oxygen isotope warming across this boundary interval may actually reflect a massive input of 16O into the global oceans as a result of a major deglaciation (Figure 4-2).

 

Inorganic Geochemical Proxies: The concept of long-term stability and equability of the Cretaceous greenhouse climate is giving way to recognition of much greater variability of the global climate on both short and long time scales. This improved understanding of Cretaceous climate comes largely as a result of increasingly detailed stable isotope records from well-preserved deep-sea sediments.

Two of the most complete and best-preserved long-term Cretaceous d18O records come from the subtropical North Atlantic and the southern South Atlantic (Figure 4-3). In the benthic foraminifer d18O curve from Blake Nose, six short-term, positive shifts of more than 0.3‰ are recorded during the Albian through Maastrichtian. It is unlikely that the late Albian, mid-Cenomanian, and mid-Campanian benthic d18O shifts were glacially forced since (1) they are not accompanied by positive shifts in the planktonic d18O record and (2) the maximum benthic d18O values are still below 1‰, which is considered by some authors (e.g., Barrera and Savin, 1999) as the ice/ice-free threshold based on benthic d18O records that span the late Eocene growth of the polar ice cap. On the other hand, coupled positive planktonic and benthic d18O shifts and cool deep-water paleotemperatures are recorded in the early Albian and early and late Maastrichtian at Sites 1050, suggesting the possibility of polar ice at these times.

Comparison of additional late Campanian-Maastrichtian d18O records from the North and South Atlantic and the Pacific (Figure 4-4) reveals correlative positive shifts in some, but not all, intervals that span the 70.5 Ma and 66.5 Ma cooling events. The 70.5 Ma event corresponds to an early Maastrichtian sea level fall recognized on the coastal margin of New Jersey (Miller et al., 1999). However, the New Jersey margin sections and other sea level curves do not show a significant sea level fall at 66.5 Ma. Both intervals clearly warrant further investigation.

New d18O data from well-preserved terebratulid and rhynchonellid brachiopods and belemnites from sections in southern England (Southerham, Eastbourne) exhibit the first high-resolution paleotemperature record spanning the early Cenomanian to early Turonian. The long-term record of brachiopod d18O values shows a continuous trend of climate warming from 14.4 °C in the middle Cenomanian to 20.3 °C in the lower Turonian (Figure 4-5). Superimposed on this long-term trend are periods of rapid cooling that are correlative to middle and late Cenomanian positive d13C events. The middle Cenomanian d13C increase is predated by a rapid d18O increase (-1.5 to -0.2‰) that corresponds to a sea level fall within the C. inerme Subzone. Maximum d18O values (0.5‰) are reached with the onset of transgression in the basal T. costatus Subzone and the occurrence of P. primus. A similar pattern is visible during the upper Cenomanian d13C positive excursion. d18O values of brachiopods and belemnites indicate rapid cooling during a sea level fall followed by subsequent warming after transgression and the brief occurrence of P. plenus. Within both Cenomanian events, the decrease of seafloor temperatures has a similar magnitude, and is 4-8°C if no changes in d18O of seawater are considered. The linkage of rapid d18O increases with sea level falls and with the southward spread of boreal taxa suggests that climate cooling could have been coupled to the build-up of ice-sheets and changes in ocean circulation, and could have initiated perturbations within the global carbon cycle.

Analyses of a number of d13C records from Cretaceous pelagic sediments reveal widespread, synchronous shifts that are attributed to changes in the relative burial fluxes of organic carbon and carbonate carbon resulting from variations in sea level. This proposed relationship is supported by comparison of Campanian carbon stable isotope and sedimentologic profiles from Tunisia, France, England, Germany and Kazakhstan, which all show remarkably similar patterns (Figures 4-6, 4-7). Positive d13C excursions ranging from +0.2 to +0.3‰ are recorded across the Santonian/Campanian boundary (~83.7 Ma) and in the mid-Campanian (~78.7 Ma), and a negative d13C excursion of -0.4‰ in the upper Campanian (~74.8 Ma) with durations of 600 - 750 kyr.  The long-term carbon isotope trend in the Campanian pelagic sections broadly follows first-order eustatic sea level with relatively stable high d13C values in the lower Campanian reflecting stable, high eustatic sea level and with decreasing d13C values in the upper Campanian reflecting falling eustatic sea levels.

 

Sedimentologic and Biotic Evidence for Cretaceous Eustasy: In order to demonstrate that sea level is truly eustatic it is necessary to identify synchronous sea level changes on a global scale using high-resolution bio-, chemo- and/or cyclostratigraphy. Although this is difficult to achieve particularly in nearshore, clastic facies, several examples of eustatic sea level change during the mid-Cretaceous are gaining acceptance based on increasingly detailed field and laboratory studies. For example, Gale et al. (2002) identified six mid- and late Cenomanian sea level cycles with frequencies of 400 kyr that can be correlated from the coastal plain of SE India to 11 individual sections in northwest Europe. Analysis of facies shifts and fluvial incision indicates that rapid falls of sea level took place at the sequence boundaries, with downcutting of 10-25 m. These are minimum values, depending on the quality and extent of outcrop. The major falls (mid-Cenomanian, C. inerme Zone, and late Cenomanian, M. geslinianum Zone) are coincident with positive d18O events of up to 2 to 2.5‰ in NW European chalk successions and correspond with the southerly migration of Boreal nektic and benthic taxa in NW Europe. Stratigraphic and sedimentologic observations from the Western Interior basin (such as identification of regional bioclastic accumulations that correlate westward to progradational wedges, some with incised valleys fills: Sageman, 1996), as well as biotic data (e.g., fluctuations in macrofaunal diversity and abundance, trace fossil content, and planktic:benthic foraminiferal ratios) indicate that the Cenomanian sea level events identified in India and NW Europe may also be expressed within the North American epicontinental stratigraphic record (Figures 4-8, 4-9, 4-10; Tibert et al., 2002). Although the duration of these mid- to late Cenomanian events may be consistent with a long eccentricity modulator (400 kyr), there has also been speculation that the rhythmic limestone-shale deposits of the Cenomanian-Turonian Bridge Creek Limestone in the Western Interior basin may reflect a high frequency eustatic signal (Elder et al., 1994; Sageman, 1998; Laurin and Sageman, 2001). Sea level changes of this magnitude and rate (tens of meters within 20 to 400 kyr intervals) are strongly suggestive of a glacio-eustatic control. 

The importance of accurate stratigraphy to correlating third-order sea level cycles is demonstrated by comparison of radiometrically interpolated and biostratigraphically correlated versions of the Haq et al. (1987) sea level curve with the sea level curve developed by Hancock (1990) for northwest Europe (Figure 4-11). Significant mismatch in the relative timing of the transgressive peaks and regressive troughs is caused by differences in the biozonal schemes, stage boundary definitions, and time scales that are used for each curve. Hancock (1993) noted that there is no simple right or wrong answer to how sea level curves should be plotted, but he emphasized that comparison of different sea level curves is only possible if their construction is based on identical stratigraphic criteria.

 

Climate Modelling: An isotope-capable version of the GENESIS atmospheric general circulation model (Mathieu et al., 2002) was used to examine the likely isotopic composition of an ice-sheet that formed during the Cretaceous and the size of the ice-sheet that would have been required to produce a significant shift in seawater isotopic composition. Preliminary results (Figures 4-12, 4-13) show that the latitudinal gradient in precipitation d18O is much less steep than the modern. The heavier-than-modern freshwater d18O values predicted for mid to high latitude North America are in agreement with those inferred from Cretaceous fossil tooth enamel studies (Fricke). The lower d18O gradient and 18O-enriched high latitude precipitation has at least two important ramifications for interpreting warm Cretaceous climate records: 1) If the mean isotopic composition of ice that formed at high latitudes was no less than -20‰, then an ice volume equivalent to 50% of the modern Antarctic ice-sheet would produce less than a 0.2‰ shift in the mean ocean dw value. This means that a substantial volume of ice could form or decay without being reliably detected in benthic d18O records. In the sequence of events reflected in the record during ice growth, eustatic sea level fall may therefore be the only "given" and is, indeed, generally accepted as having occurred throughout the Cretaceous; and 2) A lower latitudinal gradient in freshwater d18O could result in a lower gradient in upper ocean dw, relative to the modern. In that case, use of the latitudinal correction for dw based on modern GEOSECS data (Zachos et al., 1994) would consistently overestimate tropical upper ocean temperatures and underestimate high latitude temperatures. This seems to exacerbate the problem of Cretaceous polar ice growth.

 

Future Directions

            Large and rapid changes in Cretaceous sea level that have been recorded during times of global warmth pose a paradoxical problem to geologists and climatologists as they cannot be explained by any other known mechanism but glaciation (Pitman and Golovchenko, 1983). In the absence of direct geological evidence, the case for Cretaceous polar ice-sheets requires demonstration that proxy signals of sea level and climatic change are globally synchronous and consistent in their magnitude and direction of change. Thus far, few such records exist. Although the Exxon sea level curve has been promoted as representing a suite of eustatic cycles that can be globally correlated (Vail et al, 1977; Haq et al., 1987), some authors have argued that none of the Exxon cycles have been proven to be globally synchronous, the magnitude of the sea level changes have been considerably over estimated, and the use of the Exxon cycle chart should be abandoned (Miall, 1992; Rowley and Markwick, 1992). The recent surge of studies that postulate ice-sheet growth and decay as the cause for Cretaceous sea level variations and geochemical shifts (e.g., Stoll and Schrag, 1996; 2000; Miller et al., 1999; Gale et al., 2002) demonstrates the need to delineate which sea level changes were truly eustatic. 

            In order to resolve the Cretaceous ice-sheet debate, field and laboratory data that can be correlated at Milankovitch time scales must be obtained from a global array of sites and depositional settings. The following target intervals are identified as potentially yielding the greatest insight to the question of Cretaceous glacio-eustasy: (1) late Maastrichtian (~66.5 Ma); (2) early Maastrichtian (~70.5 Ma); (3) upper Campanian (~74.5 Ma); (4) Coniacian-Santonian (~89.0-83.5 Ma); (5) mid-Turonian (~92-91 Ma); (6) Cenomanian/Turonian boundary interval (~94-93 Ma), (7) mid-Cenomanian (~95.5 Ma); and (8) Aptian/Albian boundary interval (~114-112 Ma). Impermeable and low porosity clay-rich sediments from low and high latitudes should be sought to obtain the best preserved and most climatically informative oxygen isotope records across these intervals (e.g., Pearson et al., 2001). More detailed and higher resolution records from continental margin, carbonate platform, and transitional terrestrial-marine environments that have high-resolution (e.g., Milankovitch scale) age control will be essential to reconstructing a reliable Cretaceous eustatic curve.  Key questions include:

·        What were the magnitudes and rates of Cretaceous sea level changes?

·        Do Cretaceous sea level fluctuations demonstrate a Milankovitch frequency? If so, how did Milankovitch cycles affect Cretaceous sea level?

·        Which sea level changes can be proven to be globally synchronous?

·        Which, if any, Cretaceous sea level changes were glacially forced?

 

In addition to the many questions related to ice-sheet growth and sea level change, there are Cretaceous sea level change issues that have important relevance to current global warming and environmental problems (such as coral bleaching events). We need to better understand the timing, extent and causes of carbonate platform drowning. What is the mechanistic relationship, if any, between sea level rise and the OAEs? In future drilling and field studies, progress in sea level studies will require that we:

·        Identify localities that have minimal regional tectonic influences.

·        Locate terrestrial sections that record incisement during marine incursions in order to provide a quantitative estimate of sea level regression.

·        Use every environmental proxy available in stratigraphically complete, well-dated sedimentary sequences.

·        Accurately correlate between epicontinental and deep-sea records using orbitally-tuned sections, radiometrically-dated horizons and unique isotope events.

 

Drilling Priorities

1)      Principle target ages that could constrain the timing, rate, duration, and magnitude of climatic and/or sea level events and potentially provide evidence for glacio-eustasy

·           Maastrichtian: The proposed 66.5 and 70.5 Ma glacio-eustatic events can be tested by increasing the number of high-resolution, well-preserved records from deep-sea and continental margin sequences. Important sites would include:

·           Late Campanian (~74.5 Ma): Can the negative d13C excursion identified in pelagic carbonate sequences across Europe and western Asia be identified globally, and does it correlate with a positive oxygen isotope shift and sedimentologic evidence for a rapid sea level fall?

·           Coniacian-Santonian (89.0-83.5 Ma): Can this interval, which contains one of the longest relatively continuous records of orbitally influenced sedimentation in North America (as well as the comparatively poorly studies OAE3 event), be used as a test case to better understand orbital forcing of sedimentation and organic carbon burial processes and their effect on climate?

·           Mid-Turonian (~91 Ma): Can the major sea level fall identified across the U.S. Western Interior be identified globally at the same time? Could this event have been glacially forced at a time when Earth experienced some of the warmest global temperatures of the past 140 m.y.?

·           Cenomanian-Turonian boundary interval (~93.5 Ma): how rapidly did sea level change across this interval and how did that influence OAE2?

·           Mid-Cenomanian (~95.5 Ma): Did a rapid cooling in deep waters and at high latitudes occur at precisely the same time as the sea level fall identified in SE India and European sections? Can this sea level fall be identified in carbonate platform and continental margin sequences globally?

·           Aptian-Albian boundary interval (~120 Ma): Relatively positive high latitude temperature estimates for this time suggest that the polar regions may have been cool enough for the presence of a continental ice-sheet in the south polar region.

                       

2)      High priority drilling locations

·           Passive continental margin:

o        Petroleum industry borehole logs and cores: These are considered a major untapped resource that could significantly improve understanding of Cretaceous global sea level change.

o        Southeast India: potential to correlate nearshore clastic sequences with deepwater water clays at Milankovitch frequencies to better constrain the timing and magnitude of mid-Cretaceous sea level changes in that could be compared with other high-resolution records (e.g., U.S. Western Interior)

o        Brazil margin

o        J-Anomaly Ridge

o        Northwest Australia

·           Low latitudes

o        Demerara Rise: Provides critical insight to tropical climate change from an expanded Cenomanian through Turonian hemipelagic deepwater sequence; mid-Cretaceous foraminiferal preservation is known to be excellent based on DSDP Site 144A drill cores

o        Manihiki Plateau

o        Hess Rise

·           Southern, high latitude targets: could provide critical information on fluctuations in polar climates coincident with sea level rise/fall events (you need to tie this into sea level change)

o        Agulhas and Crozet Plateaus: Lamont-Doherty piston core records reveal the presence of well-preserved mid-Cretaceous foraminifera.

o        Naturaliste Plateau: Presence of well-preserved Cenomanian foraminifera documented at DSDP Site 258, but that record is incomplete because of poor drilling recovery and presence of unconformities

o        Weddell Sea

o        Mozambique/S. Madagascar Ridges

o        Falkland Plateau

·           Arctic: Any climatic records from the Arctic are highly desirable as they could provide an indication of the coolest temperatures on Earth available from the geologic record.

o        Arctic/Lomonosov

o        Hudsons Bay

o   Bering Sea

 

 

Atmospheric and Ocean Circulation in a Greenhouse World

 

Circulation Figures with Captions            Return to top of Report

 

Overview

Since the original efforts of Eric Barron and co-workers in the early 1980s, considerable progress has been made towards understanding the Cretaceous greenhouse world. This progress was forged through collaborations between the data-gatherers and the climate modelers. In this spirit, the working session, Atmosphere and Ocean Circulation in a Greenhouse World, brought together similarly disparate specialists to report on the current state-of-affairs in Cretaceous cli­mate science. The session served as a forum to report and discuss many novel and exciting ideas, and to reassert the need for continued, and closer, collaboration between climate modelers and geologists. Contributions to the Atmosphere and Ocean Circulation session could be forcibly divided into three categories, each of which is individually summarized below, with the following objectives:

·        To understand general circulation during the Cretaceous

·        To document and understand climate change through the Cretaceous

·        To develop critical data sets as boundary conditions and validation of numerical models of the Cretaceous.

 

One of the most important conclusions reached in the session is that there is no longer a sin­gle paradigm for understanding the Cretaceous general circulation. New paradigms depart signifi­cantly from the classic view of the Cretaceous as a warm, equable world forced by moderately high (4-6 x present-day levels) atmospheric carbon dioxide levels and a reversed thermohaline cir­culation. Rather, the following views were expressed:

 

·        In a Cretaceous greenhouse world, the westerly winds developed only seasonally. In the absence of persistent westerlies, the subtropical ocean gyres would have weakened leading to an ocean circulation dominated by eddies. As a result, the pycnocline would have been more diffuse than today, contributing to enhanced thermohaline circulation and global oceanic heat transport (Figure 5-1) (Hay).

·        In order to match the warmest tropical paleotemperature estimates, general circulation models of the Cretaceous indicate that atmospheric pCO2 must have been much higher than previously thought (~12 x present-day levels) (Figure 5-2) (Bice et al.).

·        High atmospheric pCO2 levels are not required to achieve a very warm Cretaceous climate. With moderate pCO2 levels (~3 x present-day levels), the Hadley coupled ocean atmosphere model predicts a hot Cretaceous world dominated by latent heat. The differ­ence between the Hadley model and other climate models that require higher pCO2 is probably in the climate sensitivity to clouds (Figure 5-3) (Valdes and Markwick).

·        Warm Cretaceous oceans can be explained by the sinking of warm, saline high-latitude waters. With moderate pCO2 levels (~3 x present-day levels), the NCAR Climate System Model predicts deep-ocean temperatures of 9-11 °C, and surface temperatures that are 3-4 and 6-14 °C warmer than modern at low and high latitudes, respectively. Ocean heat transports in the model are diminished in the Northern Hemisphere and enhanced in the Southern Hemisphere (Figure 5-4) (Otto-Bliesner et al.).

 

In contrast to the older paradigm of low latitude bottom water formation, it is notable that all the numerical models presented in which thermohaline overturning occurred showed that the warm Cretaceous deep oceans can be explained by the sinking of warm, saline high-latitude waters.

These views of the Cretaceous general circulation are a sign not only of the progress that has been made in the last 20 years, but also a representation of the scientific debates that will be played out in the next decade. As an example of the relevance of Cretaceous climate science, many of the topics discussed in the working session mirror discussions that are being held regarding future global climate change, including the sensitivity of the climate to pCO2, the presence or absence of a "tropical thermostat," the role of clouds and water vapor in climate change, and the response of ocean thermohaline circulation to polar warmth and an increased hydrologic cycle.

Another critical issue highlighted in this session was the very large differences in the response of the general circulation models to Cretaceous boundary conditions. For example, in comparison to the NCAR models, the Hadley Centre model indicates a much stronger CO2 sensi­tivity via clouds and hydrologic cycle strength. The same spectrum of climate models used in Cretaceous is being used to predict future climates, but it is only through comparison against the Cretaceous data record that we can begin to quantitatively address the question of whether the models’ sensitivity to increased greenhouse gas concentrations is too large or too small. If the low subpolar salinities predicted by the Hadley model can be verified as consistent with the existence of abundant and diverse Cretaceous planktonic foraminifera at these latitudes, then there is good reason to suspect that less sensitive models used to predict anthropogenic change may be substan­tially under-estimating future polar temperatures.

Another sign of the maturity of Cretaceous climate science is awareness that the Cretaceous climate displayed considerable variability over its 79 million years. In this working session (and others), climate variability was documented and analyzed. This variability includes changes in the geochemical state of the oceans, long-term climate warming and cooling, and millennial-scale changes in the hydrological cycle. Cretaceous marine sediments from the Tethys record funda­mental changes in the global carbon reservoir. Carbon burial occurred as inorganic carbon in pelagic and shallow water carbonates during the early Cretaceous, organic carbon in deep ocean and margin basins during the middle Cretaceous, and inorganic and organic carbon on shelves during the Late Cretaceous (Jansa et al.). Possible causes of Cretaceous climate variability discussed in this session include:

·        Large, rapid shifts in atmospheric pCO2. General circulation models indicate that large shifts in pCO2 are required to explain tropical sea-surface temperature variations in the mid-Cretaceous leading into the Cretaceous Thermal Maximum. These pCO2 large shifts fall within the range of atmospheric CO2 estimates that have been calculated through proxy methods (Bice et al.).

·        Precessional forcing. Results from a general circulation model demonstrate that the hydrological cycle in western North America is sensitive to precessional forcing. The formation of bedding couplets is controlled by changes in the rate of mechanical erosion, which is a function of surface runoff  (Figure 5-5) (Floegel et al.).

·        Paleogeographic changes. Results from a coupled ocean-atmosphere model indi­cate that the opening of the Atlantic Equatorial Gateway could have caused a large-scale reorganization of the tropical climate, and regional warming. This mechanism was con­sidered as a cause of the Cretaceous Thermal Maximum (Figure 5-6) (Poulsen et al., 2003).

 

As demonstrated by the findings summarized above, numerical models of the Cretaceous climate can provide insights into the working of a greenhouse world, as well as validation of the sophisticated models used to forecast future climate change. However, Cretaceous simulations are only as good as the boundary conditions incorporated into the models. Likewise, validation of the models necessitates accurate and detailed descriptions of critical aspects of the Cretaceous environment. Progress has been made in both of these areas, and include:

·        The production of high-resolution paleotopographic and paleobathymetric eleva­tion models for the Late Maastrichtian (70 Ma), early Campanian (80 Ma), C/T bound­ary (90 Ma), Albian (110-100 Ma), early Aptian (120 Ma), and Valanginian (130-140 Ma) (Figure 5-7) (Scotese).

·        The construction of detailed paleobathymetric maps with accurate description of gateway openings and block movements (Figure 5-8) (Lawver and Gahagan).

·        The development of detailed global vegetation maps, and an analysis of areas of agreement and disagreement between different reconstructions (Figure 5-9) (Upchurch et al.).

·        The reconstruction of Cretaceous climate using statistical relationships between leaf form and climate. Much of our knowledge of terrestrial climate stems from these statistical models, however the choice of regression model can introduce a strong climate bias. Differences between regression models can cause climate interpretations that vary by 7°C in mean annual temperature and 600 mm in mean annual precipitation (Figure 5-10) (Scherer et al.).

·        The reconstruction and variability of detailed current systems, such as the middle Cretaceous contour current system along the continental rise of the deep southeastern Gulf of Mexico (Figure 5-11) (Buffler).

 

The need for detailed data sets to use as boundary conditions and to validate the climate models will only increase as the model resolution and sophistication increase. In addition, targeting specific time intervals of interest could facilitate model intercomparison and validation. Such an endeavor would require support from the entire Cretaceous scientific community.

 

Future Directions

The study of climate variability in the Cretaceous requires continuous time-series of environmental change. As more continuous, high-resolution (millennial scale) archives are developed, the picture of Cretaceous climate variability will expand. Obtaining these records and identifying the causes of climate variability in a greenhouse world, particularly those that can cause "surprises" such as rapid pCO2 fluctuations or tropical climate shifts, should be a major focus of the Creta­ceous scientific community.

 The working session on Cretaceous atmosphere and ocean circulation demon­strated that significant progress has been made in defining and understanding the complexities of Cretaceous climate. Old paradigms have been replaced by a variety of new paradigms (some speculative) that will be the focus of the community for the near future. Many of the remaining critical questions in Cretaceous climate science are shared by the future global change community, including the roles of clouds, water vapor, tropical climate, and CO2 in driving global climate. The Cretaceous community is uniquely positioned to contribute significantly to these questions. To facilitate this endeavor, we must encourage and support more cross-disciplinary collaborations between climate scientists and those who gather Cretaceous climate proxy data.

 

 

Environmental and Biotic Consequences of Large Igneous Provinces

 

Consequences of LIPs Figures with Captions            Return to top of Report

 

Overview

Large Igneous Provinces (LIPs) were constructed during voluminous magmatic events that took place over geologically brief (<3 m.y.) time intervals (e.g., Duncan and Richards, 1991; Tarduno et al., 1991; Coffin and Eldholm, 1994).  These events are thought to be associated with massive thermal anomalies in the mantle known as "superplumes" (Larson, 1991).  The volume of crust produced by LIPs in the mid-Cretaceous was almost three times greater than in prior and subsequent time periods (Larson, 1991).  In particular three prominent LIPs were formed during this interval.  The Ontong Java Plateau (OJP) and Manihiki Plateau in the Pacific formed ~123 Ma in the late Barremian, the Kerguelen Plateau in the Indian Ocean was erupted in the late Aptian and early Albian, and the Caribbean Plateau is thought to have formed near the Galapagos hotspot between 93 and 95 Ma (Duncan and Hargraves, 1984).

Increased rates of volcanism associated with oceanic plateau formation and sea floor spreading in mid-Cretaceous time probably caused a variety of biological and geochemical responses.  A current popular model for the sporadic occurrence of oceanic anoxic events (OAEs) in the Cretaceous ties hydrothermally-induced changes in ocean chemistry to increased surface productivity, followed by mid-to-deep water oxygen depletion and accumulation of organic-rich sediments (e.g., Vogt, 1989; Leckie et al., 2002). In addition, CO2 outgassing during volcanism may have increased global temperatures and altered deep water circulation patterns leading to increased anoxia in warm deep waters (e.g., Arthur et al., 1985).  However, small but possibly significant mismatches between radiometrically dated oceanic basalts and stratigraphically dated geological responses make it difficult to establish cause and effect relationships with certainty (Figure 6-1, Larson et al.).

Metal anomalies that arise from hydrothermal activity during ridge-crest and mid-plate volcanism can be advected for significant distances by plumes (e.g., Baker, 1994), especially where the water column is reducing.  Megaplume activity can enrich Fe, Mn, and trace metals (e.g., Cr, V, Ni, Zn, Cu, Ba) in proximal sediments by several orders of magnitude (Figure 6-2; Duncan and Rubin, 1997). This signature in sedimentary sections has great potential for precise stratigraphical correlation between hydrothermal activity and its potential environmental responses including OAEs and plankton turnover.  Preliminary metal data from the Cismon section, for example, appear to record Ontong Java Plateau (OJP) volcanism in strata within and directly below the Selli Level (Figure 6-3, Turgeon et al.; Duncan and Huard, 1997) providing an enticing causal scenario for OAE1a.  However, a far more comprehensive set of drill sites is required to test this relationship, and connections between LIP eruptions and other OAEs.  In addition, the sensitivity of phytoplankton to bio-limiting and toxic trace metals and the difference between the hydrothermal inputs from sea floor spreading centers and ocean plateaus is not completely understood. Precise paleotemperature estimates are still needed for the Barremian-early Albian interval to assess the potential effect of this huge volcanic episode on paleoclimate.

The relationship between LIP formation and OAEs derived from radiometric estimates is less straight forward.  Radiometrically dated basalts from the OJP and Manihiki Plateau average 123 Ma, while the Selli black shale (OAE1a) and associated isotopic ratio anomalies occurred 2-3 m.y. later.  Basalts from the Kerguelen Plateau suggest major volcanic activity, much of which was subaerial, beginning at about 118-119 Ma, which possibly continued at decreased rates and contributed to OAE1b and elevated paleotemperatures in the Albian. Basalts from the Caribbean Plateau, which were previously determined to have radiometric ages of about 88-91 Ma (Sinton and Duncan, 1997), have been redated and with one exception now have radiometric ages of about 92-95 Ma (Duncan, unpulished data). Thus, the case is considerably stronger, but not yet certain, that Caribbean Plateau volcanism contributed to OAE2 and associated isotopic anomalies near the Cenomanian/Turonian boundary at 93.5 Ma. These new age 40Ar-39Ar whole rock age determinations are based on incremental heating experiments that, with one exception, produce Ar-recoil patterns from which only total fusion ages can be extracted. These ages are more precise than previous estimates, but still produce the same estimated duration of volcanic activity of about 3 m.y. Additional improvements in radiometric dating will rely on finding samples from which feldspar can be separated.

Ocean drilling can make a major contribution to investigating the linkage between LIP volcanism and environmental change.  High-resolution studies have and will continue to reveal the time scale and nature of biostratigraphic, lithologic and chemical changes at OAEs. An array of drilling sites designed to recover continuous sections for targeted OAEs, will document "near-field" and "far-field" effects, trace element abundance patterns, and Cretaceous ocean circulation. Advances in analytical methods (ICP-MS) open the way for detection of a wide range of potentially diagnostic elements from large numbers of samples.  Finally, other tracers with short residence times are required to trace hydrothermal activity regionally and globally.  Os isotope ratios, specifically 187Os/188Os, are limited to analysis of sediments deposited in oxic conditions, but hold significant potential to meet this goal (Ravizza et al., 2001). For example, based on analyses of metalliferous sediments from Cyprus and Oman, there is an excursion close to the Cenomanian/Turonian boundary that may be associated with LIP emplacement in the Caribbean.   Os isotopes have significant potential to further our understanding of the linkage between LIP activity and OAEs (Figure 6-4, Ravizza et al.).

 

Future Directions

A number of key questions can only be addressed through ocean drilling. 

·        What was the effect of the world-wide, mid-Cretaceous volcanic pulse on the deposition of Corg and the timing of OAEs?  We need to determine whether the timing and duration of LIPs is correlative with OAE events via improved radiometric dating of LIPs; improved dating of OAEs (GPTS, Os-dating of black shales); sites proximal to an ocean plateau that records both volcanic history and OAE events (e.g., Nauru Basin and OJP).

 

·        Which OAEs are LIP-related and which have other causes?  We need high-resolution, multiple-proxy studies of "regional" OAEs, for which no LIP has been identified.

 

·        What was the effect of mid-Cretaceous volcanism on paleotemperature and pCO2? Needed: updated calculations of ocean heating by massive lava flows in appropriate Creta­ceous ocean conditions; high-resolution GCM of Cretaceous ocean with LIP inserted to model altered flow and circulation downstream from LIP effluent; better estimates of degassing and hydrothermal trace element "fingerprints"; understanding of gas hydrate distribution and stability in early and mid-Cretaceous oceans; better information about primary trace metal contents of LIPs and alteration effects; which metals are bio-limiting (or toxic) and which phytoplankton are important in OAEs.  Was the volcanic pulse a direct cause of "greenhouse" climate conditions?  Or is methane dissociation a more likely trigger? 

 

·        Do microplankton and microbenthos respond to the physical, chemical and biological oceanographical changes associated with OAEs?  What are the causes of apparent extinction and evolution in these time intervals?

 

·        What are the different effects of predominantly submarine LIPs vs. predominantly subaerial LIPs?  Needed: high-resolution, multiple-proxy studies of K/T (Deccan) or Valanginian (Parana) vs. early Aptian (OJP) or C/T (Caribbean) events.

 

Drilling Priorities

      Drilling priorities for OAE1a in the Pacific include Magellan Plateau, Nauru Basin, and seafloor sufficiently young to be above the CCD at OJP time (i.e., M1-M3 age). In the Atlantic and Indian Oceans, the Weddell Sea and Maud Rise are high priorities.  For OAE2, future drilling in the Pacific on Magellan Rise, Manihiki Plateau, Hess Rise, and Cenomanian-Turonian atolls is needed.

 


DRILLING TARGET SUMMARY

 

LOCATION               PROPOSAL #            PROPONENTS       

PACIFIC RISES

 

Manihiki Plateau                                     Roger Larson and Elisabetta Erba

Magellan Rise                                                   Roger Larson and Elisabetta Erba

Hess Rise                                                         Roger Larson and Elisabetta Erba

 

HIGH LATITUDE SOUTH

 

Weddell Sea                             503 (full)     Woody Wise, W. Jokat, et al.      

Naturaliste Plateau                                     Darren Gröcke

Agulhas/Crochet Plateaus                                Brian Huber

Mozambique/S. Madagascar Ridges              Dick Norris and Karen Bice

Falkland Plateau                                     Karen Bice, Woody Wise

 

HIGH LATITUDE NORTH

 

Arctic/Lomonosov                   533 (full)     Jan Backman

Arctic-Atlantic Gateway            588 (pre)     F. Gradstein, S. Ren, et al.

Hudsons Bay                            617 (pre)     Tim White

Bering Sea                                                        Tim Bralower

 

CONTINENTAL MARGINS

 

Carolina Transect                       616 (pre)     Tim Bralower, S. Culver, et al.

J-Anomaly Ridge               562 (full)     Dick Norris, Karen Bice, et al.

Cape Verde Basin                                        Tom Wagner

Brazil Margin                                                    Lisa Pratt, Simon Brassell, Karen Bice

Northwest Australia                                               Paul Bown, Leon Clarke

NE Japan                                 608 (pre)     Takashi Hasagawa

 

OTHER CRETACEOUS OBJECTIVES

 

Scott Plateau                            513 (full)     B. Opdyke, H. Stagg, G. C. H. Chaproniere

Hikurangi LIP                           542 (pre)     N. Mortimer, R. Wood, et al.

Chicxulub Impact Crater            548 (full)     J. Morgan, R. Buffler, et al.

Caribbean LIP                          561 (full)     Bob Duncan

S. Rockall-Hatton Plume            596 (pre)     Tim Morrissey, P. Shannon, et al.

Somali Basin                             606 (pre)     Hiroshi Nishi, Hisatake Okada, Brian Huber

Ontong Java Plateau             623 (pre)     C. Neal, M. Coffin, et al.

 

 

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Appendix 1

 

Workshop Participants

Thierry Adatte

University of Neuchâtel

Michael A. Arthur

Penn State University

Enriqueta Barrera

National Science Foundation

Britta Beckmann

University of Bremen

Karen L. Bice

Woods Hole Oceanographic Institution

Paul R. Bown

University College London

Timothy J. Bralower

University of North Carolina-Chapel Hill

Simon C. Brassell

Indiana University

Richard T. Buffler

University of Texas

Pat R. Castillo

Scripps Institution of Oceanography

Leon J. Clarke

University of Wales, Bangor

Linda M. de Romero

University of North Carolina-Chapel Hill

Walter Dean

USGS, Denver

My Le Ducharme

Smithsonian Institution

Robert A. Duncan

Oregon State University

Maya B. Elrick

University of New Mexico

Elisabetta Erba

University of Milan

Jochen Erbacher

BGR

David B. Finkelstein

Indiana University

Alfred G. Fischer

University of Southern California

Cynthia G. Fisher

West Chester University of Pennsylvania

Sascha Floegel

GEOMAR

Karl B. Föllmi

University of Neuchâtel

Astrid Forster

Netherlands Institute for Sea Research

Henry Fricke

Colorado College

Andrew S. Gale

University of Greenwich

Luis A. Gonzalez

University of Iowa

Darren Gröcke

Royal Holloway College

Jake M. Hancock

Imperial College of Science, Technology and Medicine

Takashi Hasegawa

Kanazawa University

Noralynn Hassold

University of Michigan

William W. Hay

GEOMAR

Ulrich Heimhofer

ETH-Zurich

Achim Hermann

Penn State University

Peter M. Hofmann

University of Cologne

Ann Holbourn

Christian Albrechts University

Brian T. Huber

Smithsonian Institution

Hope Jahren

Johns Hopkins University

Luba F. Jansa

Dalhousie University

Ian Jarvis

Kingston University

Hugh C. Jenkyns

Oxford University

Claudia C. Johnson

Indiana University

Kirk Johnson

Denver Museum of Nature and Science

Erle G. Kauffman

Indiana University

Gerta Keller

Princeton University

Wolfgang Kuhnt

Christian Albrechts University

Roger L. Larson

University of Rhode Island

Jiri Laurin

Academy of Sciences of the Czech Republic

Lawrence A. Lawver

University of Texas

R. Mark Leckie

University of Massachusetts

Jackie A. Lees

University College London

Elana Leithold

North Carolina State University

Greg A. Ludvigson

University of Iowa

Kenneth G. MacLeod

University of Missouri

Adam McConnell

University of Massachusetts

Cheryl L. Metz

Texas A&M University

Philip A. Meyers

University of Michigan

Stephen R. Meyers

Northwestern University

Isabel P. Montanez

University of California-Davis

Dragana D. Nebrigic

University of Texas at Dallas

Richard D. Norris

Woods Hole Oceanographic Institution

David Osleger

University of California-Davis

Bette L. Otto-Bliesner

National Center for Atmospheric Research

Desiree Polyak

University of Massachusetts

Christopher Poulsen

University of Southern California

Lisa M. Pratt

Indiana University

Isabella Premoli Silva

University of Milan

Greg Ravizza

Woods Hole Oceanographic Institution

Shelley Rios

National Science Foundation

Bradley Sageman

Northwestern University

Sarah Santee

University of California-Davis

Christopher R. Scotese

PALEOMAP Project

Paul J. Sikora

University of Utah

Laura J. Snow

Oregon State University

Erica M. Sterzinar

University of Massachusetts

John A. Tarduno

University of Rochester

Steven C. Turgeon

ICBM - Universität Oldenburg

Garland R. Upchurch

Southwest Texas State University

Paul J. Valdes

University of Reading

Silke Voigt

University of Cologne

Hu Xiumian

Chengdu University of Technology

Thomas Wagner

University of Bremen

David K. Watkins

University of Nebraska

Timothy S. White

Penn State University

Peter Wilf

Penn State University

Paul A.Wilson

University of Southampton

Sherwood W. Wise

Florida State University

 

 

Appendix 2

Download workshop program (pdf).

 

Return to top of Report

 

 

Figures with captions - Cretaceous Climate Record as Revealed by Stable Isotopes

Figure 1-1 (Norris et al.) Compilation of paleotemperature estimates from oxygen stable isotope ratios for clay-hosted planktonic foraminifera (red symbols), chalk-hosted planktonic foraminifera (blue symbols), and benthic foraminifera (black symbols).

 

Figure 1-2 (Bice et al.)  Estimated paleotemperatures for DSDP Site 511 calculated assuming that ambient surface waters were as depleted as the lightest water in the GEOSECS dataset poleward of 60 degrees latitude (-0.5 per mil SMOW) and adjusted by -1.0 per mil to correct for ice-free world; dw of bottom waters was assumed to be -1.0 per mil SMOW.

 

Figure 1-3 (MacLeod and Huber) Paleogeographic map of the mid-Maastrichtian (Ziegler et al., 1997) showing the approximate location of selected sites for which Maastrichtian ocean temperatures have been estimated.  Estimated paleotemperature from unpublished data and compilations of Barrera and Savin (1999) and Frank and Arthur, (1999).

 

Figure 1-4 (Jenkyns and Tsikos) Chemostratigraphic correlations between the Black Band (S. Ferriby, England) and the Cenomanian/Turonian of Olini (Columbia) and Pueblo (Colorado, U.S.) sections.

 

Figure 1-5 (Elrick and Molina) Proposed carbon isotopic correlations between the lacustrine carbonates of the Cedar Mountain Formation and carbon isotope profiles presented by Bralower et al. (1999, Jour. Foram. Res. 29:4:418-437).  Uppermost strata of the Cedar Mountain Formation contain a 98.4 Ma volcanic ash bed straddling the Albian-Cenomanian boundary (Cifelli et al., 1997, Proc. Natl. Acad. Sci. USA 94:11163-11167). Note the systematic d13C offset between the Price River (proximal foreland) and Dinosaur National Monument (distal foreland) sections.

 

Return to Stable Isotopes text

 

Figure with captions - Biotic Records of Global Change during the Cretaceous

Figure 2-1 (Lees) Nannofossil palaeobiogeographic data can be used to indicate broad-scale ocean-climate. Four Southern Hemisphere Late Cretaceous nannofossil palaeobiogeographic zones (PBZs) can be determined using semiquantitative data - Subantarctic, Austral, Temperate, Tropical. These are broadly equivalent to marine-climatic belts. Latitude-related movements in the water-mass fronts bounding nannofossil PBZs can be used to determine ocean-climate-change trends. Such trends correlate well with published d18O SST data. The Campanian nannoplankton diversity maximum appears to be the result of cooling (but in a warm, greenhouse world). Understanding the biogeographic distribution and ecological niche of each Late Cretaceous nannofossil taxon, and the effects of climate upon these, is essential for greater (wider) biostratigraphic effectiveness. Knowledge of the potential ecological strategy of each Late Cretaceous nannofossil taxon could help to elucidate climate-related features of a water-mass, e.g. potentially r-selected (meso-/eutrophic) taxa indicating nutrient cycling, turbulence, upwelling and seasonality, and putative K-selected (oligotrophic) taxa suggesting water-column stratification and relative stagnation.

 

Figure 2-2 (Premoli Silva) Summary of planktic foraminiferal diversity trends during the Early Cretaceous.

 

Figure 2-3 (Premoli Silva) Planktic foraminiferal abundance and diversity through the lower Aptian Selli Event (OAE1a) in Italy.

 

Figure 2-4 (Johnson) Paleobiogeographic distribution of scleractinian corals. The dispersion pattern for colonial corals infers that the geographic extent of the Cretaceous tropics was greater than that of our present-day interglacial period. Base map of Scotese and Golonka (1992).

 

Figure 2-5 (Wilf et al.) Terminal Cretaceous paleotemperatures estimated from oxygen isotope data from tests of benthic (filled symbols) and planktic (open symbols) foraminifera at (A) middle- and (B) high-latitude drilling sites, with (C) the most complete data from (A) and (B) plotted against temperatures derived from North Dakota leaves (this study). Large arrowheads indicate the Bass River size and abundance acme (A) (Olsson et al., 2001) and Antarctic appearance datum (B) (Huber and Watkins, 1992) for Pseudotextularia elegans, a thermophilic foraminifer. Paleotemperatures were calculated using the equation of Erez and Luz (1983), assuming an ice-free world with an average d18O value for ocean water of -1.2 ‰, Peedee belemnite standard (Shackleton and Kennett, 1975). Benthic data are based on combined d18O values for Gavelinella beccariiformis and Nuttallides trumpeyi, which generally plot within 0.2‰ of each other. None of the data has been corrected for variations in seawater salinity or vital effects, and normal marine salinity is assumed for all sites. The Bass River borehole is in the New Jersey coastal plain, 40°N paleolatitude, 100 m paleodepth, data from Olsson et al. (2001); Deep Sea Drilling Project Site 525A is in the South Atlantic, 35°S, 1000 m (Li and Keller, 1998); Ocean Drilling Program (ODP) Site 1050C is in the western North Atlantic, 30°N, 1500 m; and ODP Site 690C is in the Weddell Sea, 65°S, 1500 m (Barrera and Savin, 1999). All data for Site 1050C and some data for Site 690C are new. K = Cretaceous; P = Paleogene; C29r, C30n = magnetic polarity Chrons 29 reversed and 30 normal, respectively. Limitations on graphic presentation cause floral data from < 1 m above and foraminiferal data from just below the K-P to appear within the gray line representing the K-P.

 

Figure 2-6 (Tarduno) A glendonite from the Early Cretaceous of the high Arctic.

 

Figure 2-7 (Fisher) Contour map of planktic foraminiferal (Hedbergella delrioensis) porosity data from localities across the Western Interior Sea during the latest Cenomanian Neocardioceras Biozone time.

 

Figure 2-8 (Fisher) Profile of latest Cenomanian planktic foraminiferal (Hedbergella delrioensis) porosity data from the southern part of the Western Interior Sea.

 

Figure 2-9 (Erba) Integrated bio-, magneto- and chemo-stratigraphy of the late Valanginian "Weissert event" (Bartolini & Erba, in prep.). Time scale after Channell et al. (1995);  d13C curve after Weissert et al. (1998);  Igneous events after Renne et al. (2001).

 

Figure 2-10 (Leckie et al.) - Summary of the major geochemical, tectonic, sea level, and plankton evolutionary events associated with the mid-Cretaceous Oceanic Anoxic Events. Note the concentration of evolutionary turnover events (speciation plus extinction) with the OAEs. Also note that OAE1a, 1b, and 2 are temporally associated with increased submarine volcanic activity as indicated by the lower 87Sr/86Sr ratios (Bralower et al., 1997), and all three are linked to increased burial of marine organic matter (e.g., Arthur et al., 1987; Erbacher et al., 1996; Larson and Erba, 1999). We hypothesize that submarine volcanism and hydrothermal activity at the spreading centers helped to fuel the elevated levels of marine productivity during the OAEs by way of iron fertilization of the water column. In addition to submarine volcanism, the strontium isotope record is also influenced by continental weathering and runoff (e.g., Jones and Jenkyns, 2001), and the rise in 87Sr/86Sr ratios during the Albian may in large measure record increased weathering rates with rising sea level and global warming, despite the faster spreading rates that sustained high global sea level through much of the Late Cretaceous. The high productivity associated with OAE1d may have been facilitated by an ocean already preconditioned by dissolved iron (from Leckie et al., 2002).

 

Figure 2-11 (Erba) Mid-Cretaceous integrated stratigraphy, nannofossil evolutionary events and evidence of cooling episodes interrupting the greenhouse conditions. The main igneous events related to the formation of the Ontong Java - Manihiki and Kerguelen LIPs closely correlate with OAEs, isotopic excursions and biotic changes. Timescale: Gradstein et al. (1995). Planktonic foraminiferal zones: Premoli Silva & Sliter (1999). Nannofossil zones and events: Bralower et al. (1997), Walsworth-Bell & Erba (in prep.), Erba (1986, 1992, unpublished). Oxygen and carbon isotopic curves: Menegatti et al. (1998), Weissert et al. (1998), Jenkyns et al. (1994), Herrle (2001), Wilson & Norris (2001). Igneous events: Larson & Erba (1999), Duncan (2002).

 

Figure 2-12 (Holbourn and Kuhnt) Benthic foraminiferal biofacies for Cretaceous oceanic anoxic events 1a-1d, 2 and 3.

 

Figure 2-13 (Holbourn and Kuhnt) Our data do not support a simple model of mass extinctions caused by global anoxia, followed by prolific radiations during the recovery period at the end of OAEs. We suggest an alternative model of accelerated faunal turnover within reduced or isolated populations during and following periods of anoxia. This new model implies that the extent, depth and intensity of oxygen minima within ocean basins varied considerably with time during OAEs. In the case of OAE2, the most significant faunal turnover was in deep sea assemblages, whereas faunal turnovers in shelf and bathyal assemblages mainly reflect sea level change and taphonomic bias.

 

Figure 2-14 (Meyers and Sageman) The rate of first appearance, last appearance, and turnover of bivalves (FA-LA) is compared to geochemical proxy fluxes (titanium, carbonate, molybdenum) from the Bridge Creek Limestone Member. The accumulation rate data is from the # 1 Portland core (Meyers et al., 2001). Evolutionary rates were calculated using the time scale of Meyers et al. (2001) and taxa range data compiled by Harries and Little (1999). Note the following:  1. Apparent evolutionary rates of molluscan fauna of the Western Interior Seaway represent a balance between faunal migration, local environmental conditions, and extra-basinal forcing. 2. Migration of Tethyan fauna into the seaway is most prominent at the base of the Bridge Creek Limestone (S. gracile biozone), with rates of bivalve first appearance approaching 30 spp./1000 years. 3. An elevated rate of bivalve last appearance occurs in the upper S. gracile biozone, and is correlative with enhanced detrital flux into the seaway.  Species loss may have been forced by changes in substrate firmness and/or clogging of the feeding apparatus as suggested by Elder (1989). 4. The major turnover of molluscan species prior to the C/T boundary, which reflects some extinction but mainly very low origination rates, is not correlative with evidence of the largest changes in redox state or detrital flux, as recorded in the geochemical proxy data. This may indicate that the turnover mechanism was extra-basinal.

 

Return to Biotic Records text

 

Figures with captions – Oceanic Anoxic Events: Causes and Consequences

Figure 3-1 (Brassell) Elemental and molecular characteristics of OAE 1a from Shatsky Rise, depicting: 50cm organic-rich interval corresponding to OAE 1a at Hole 1207B, results from Rock-Eval pyrolysis of organic-rich intervals in the West Pacific, and illustrative distributions of hydrocarbon and ketone biomarkers labelled according to their biological origins.

 

Figure 3-2 (Meyers) Compilation of d15N:d13Corg values for various samples.

 

Figure 3-3 (Erbacher and Herrle) Cyclicity and orbital control of OAE 1b in France.

 

Figure 3-4 (Wagner et al.) Temporal relationship of continental supply, development of deep-water anoxia and organic carbon burial.

 

Figure 3-5 (Jahren) Carbon release from methane hydrate (Gt) versus time.

 

Figure 3-6 (Hasegawa) Based on a comparison of carbon isotopes from terrestrial organic carbon, marine carbonate carbon and marine organic carbon, relationships between the long-term climatic optimum during the Middle Cenomanian-Early Turonian and isotope signals are proposed: A greenhouse-induced warm and humid climate gradually prevailed over northeastern Asia. Under these conditions, a strengthened canopy and humidity effects drew the d13C value of plants in a negative direction. A gradual increase in pCO2 drove an intensified greenhouse effect that led to the climatic optimum. It caused a long-term negative excursion in marine organic carbon d13C that is comparable to that for terrestrial organic carbon.

 

Figure 3-7 (Heimhofer et al.) Correlation of Aptian shallow-water successions from the Algarve and Lusitanian Basins, Portugal. Stratigraphy of the Algarve Basin is based on chemostratigraphy ( d13C  of terrestrial organic matter) in combination with palynological data. The Lusitanian succession is dated with palynomorphs and benthic foraminifera. D2 and D3 correspond to major sedimentary discontinuities, LSE represents a near-shore equivalent of the "Livello Selli" horizon. Colors refer to different depositional environments. Major events in the sedimentary evolution of the two basins are marked with an arrow.

 

Figure 3-8 (Sageman and Meyers) Geochemical fluxes (organic carbon, carbonate, molybdenum), and percent lamination for the Bridge Creek Limestone Member (#1 Portland core). Accumulation rate data is from Meyers et al., 2001. Percent lamination was calculated by applying a 2 meter moving window to high-resolution ichnologic data (oxygen-related ichnocoenoses from Savrda, 1998), and determining the relative frequency of laminated intervals (# laminated samples/total # samples) within each 2 meter window.

 

Figure 3-9 (Forster et al.) Compilation of isotopic data (from left to right: bulk organic carbon, compound specific, and bulk carbonate), a quantification of the decrease in the carbon isotopic fractionation factor of marine phytoplankton (ep) and organic mater mass accumulation rates covering the OAE 2 at different sites under investigation (paleogeographic map gives location by small numbers) in comparison with published data.

 

Return to Oceanic Anoxic Events text

 

Figures with captions - Sea Level Record and Mechanisms for Global Eustatic Change

Figure 4-1 (Schouten et al.) Estimation of the mean annual sea surface temperatures for today's equatorial oceans and from Cenomanian-Turonian sediments at DSDP Site 367 based on analysis of membrane lipids from marine crenarchaeota, which are nannoplankton that have thrived in present and Cretaceous oceans. Further tests of this "TEX86" proxy should demonstrate its reliability as a new organic paleothermometer.

 

Figure 4-2 (Clarke) Preliminary benthonic foraminiferal Mg/Ca data are used to investigate the cause of a large negative shift in oxygen-isotope ratios (d18O) that occurs across the Aptian–Albian boundary in ODP Hole 766A (cf. Clarke and Jenkyns, 1999). Because d18O values reflect both the temperature of calcification and the oxygen-isotope composition of contemporaneous seawater, it is necessary to utilize an independent paleotemperature proxy, i.e. foraminiferal Mg/Ca ratios, in order to deconvolute the ice-volume and temperature components of the d18O record. The recorded Aptian–Albian d18O shift is of a comparable magnitude (~1.5‰) to the change of 1.2‰ in benthic d18O values at the Eocene–Oligocene boundary that relates to the onset of major Antarctic glaciation during the Cenozoic (cf. Zachos et al. 2001). Consequently, it is possible that the high d18O values during the mid–late Aptian can be explained in terms of an ice-volume effect that resulted in seawater being depleted in 16O, rather than solely being due to cool paleotemperatures. Statistical analyses (t-Test and F-test) of these initial data indicate that mean Mg/Ca ratios are significantly different (0.05 confidence level) below and above the d18O shift, and are indicative of a cooling across the Aptian–Albian transition. As such, the Mg/Ca data strongly suggest that the recorded d18O change reflects variations in the isotopic composition of seawater, due to the input of 16O from a shrinking cryosphere, rather than an increase in paleotemperatures. Currently, no correction is made for long-term changes in the Mg/Ca composition of the mid-Cretaceous oceans. Such an interpretation of a major mid-Cretaceous deglaciation event will help to reconcile the controversial dropstone and glendonite evidence for a cool/sub-freezing late Aptian climate during the assumed peak greenhouse climate conditions of the mid-Cretaceous.

 

Figure 4-3 (Huber et al.) Paleotemperature estimates based on d18O analyses of planktic and benthic foraminifer species from the subtropical North Atlantic (Blake Plateau ODP Sites 1049 and1050) and sub-Antarctic DSDP Site 511 and ODP Site 690 (modified after Huber et al., 1995, 2002). Temperatures are estimated using the Erez and Luz (1983) paleotemperature equation and assuming that the isotopic composition of Cretaceous seawater was –1.0‰SMOW. Planktonic data are adjusted using the Zachos et al. (1994) correction for paleolatitude. Note that the coolest deepwater temperatures in the Blake Plateau record occurred during the late Albian and early and late Maastrichtian. Brief benthic cooling events are shown at ~100 and 95.5 Ma, but correlative cooling is not observed in the planktonic record from Blake Plateau or in benthic and planktonic records from southern high latitudes. Higher resolution records and more accurate correlation of the across these "cooling events" to test whether they can be identified globally.

 

Figure 4-4 (Huber et al.) Late Campanian-Maastrichtian d18O records from Atlantic, Pacific, and Southern Ocean deep-sea drilling sites. Diamonds = benthic foraminifera; triangles = deeper dwelling planktonic foraminifera; circles = near surface planktonic foraminifera. Note that the positive (cooling) shifts in planktonic and benthic d18O at ~66.5 Ma and ~70.5 Ma are not apparent in several of the other d18O curves. Such inconsistencies are an impediment to establishing links to global climatic forcing mechanisms.

 

Figure 4-5 (Voigt and Gale) d13C and d18O values of Cenomanian articulate brachiopods and belemnites from sections in southern England. Note the long-term warming trend and the coincidence of temperature decreases with sea level falls in the earliest Middle and Late Cenomanian. Abbreviations: L. Tur.-  Lower Turonian, T. cost. - Turrilites costatus, A. rhotomag. - Acanthoceras rhotomagense, A. juk.-br. - Acantoceras jukesbrownei, M. geslin. - Metoicoceras geslineanum, W. dev. - Watinoceras devonense, M. nodos. - Mammites nodosoides, SB - sequence boundary.

 

Figure 4-6 (Jarvis et al.) Schematic illustration of major processes affecting the carbon isotopic composition of Campanian seawater and their relationship to sea level rise.  Thick lines and red arrows indicate the dominant processes controlling the d13C composition of the oceans and the atmosphere, and recorded in the marine carbonate record; thinner lines and yellow arrows are subsidiary processes.  Carbon isotope excursions are caused principally by changes in the partitioning of carbon between the organic (Corg) and carbonate (Ccarb) sinks, driven by eustatic sea level change.  Positive isotope excursions are linked to sea level rise and higher Corg burial fluxes; declining  d13C following transgression is controlled principally by increased Ccarb burial at constant or decreasing Corg burial rates. SW = seawater, CO2 = atmospheric carbon dioxide.

 

Figure 4-7 (Jarvis et al.) Sea level change versus carbon isotope stratigraphy.  The carbon isotope curve is a five-point moving average of data from the Trunch borehole, eastern England (data from Jenkyns et al., 1994).  The d13C curve (thick grey line) is plotted against the time scale of Gradstein et al. (1995), calibrated using the base Campanian (83.5 Ma) and base Maastrichtian (71.3 Ma) and assuming a constant sedimentation rate at Trunch.  Isotope events are indicated by colored bands.  The relative positions of the NW European macrofossil and Tethyan planktonic foraminifera biostratigraphies are based on a carbon isotope correlation with El Kef, Tunisia (Jarvis et al., in press).  The transgressive and regressive events (green and red polygonal boxes, respectively) recognized in Germany (Niebuhr, 1995; Niebuhr et al., 2000) are shown for comparison.  Peaks and troughs on the regional sea level curves have been placed relative to the appropriate biostratigraphy. The 'eustatic' curve (Haq et al., 1987) has been re-calibrated by placing the base of TST3.4 at the bottom of the Santonian - Campanian Boundary Event, the base of TST4.1 at the base of the mid-Campanian Event,  and the base of TST4.4 at the top of the Upper Campanian Event, and scaling the remainder of the curve accordingly. HST = high-stand systems tract; LST = low-stand systems tract; TST = transgressive systems tract.

 

Figure 4-8 (Leckie et al.) West to east transect of clastic-dominated stratigraphic sections from southern Utah, northeastern Arizona, and southwestern Colorado (stipple pattern: coastal plain and shallow marine sandstone; brick pattern: limestone and/or calcarenite-rich intervals; no pattern: marine non-calcareous and calcareous shale and mudstone). These sections represent the western side of the Cretaceous Western Interior Sea and record the third-order transgressive-regressive Greenhorn Cyclothem. Peak transgression occurred during the early Turonian and a major regression at the end of the middle Turonian caps the Greenhorn Cycle. Fourth-order carbonate cycles (Leithold, 1994) and intermediate stratigraphic cycles (Gardner, 1995) illustrate the occurrence of higher frequency sea level cycles some of which may represent 400 kyr long-eccentricity cycles (from Tibert et al., 2002). 

 

Figure 4-9 (Sageman and Meyers) Diagrammatic W-E cross section showing regional stratigraphic relations within the Greenhorn marine cycle:  stacking patterns of marginal marine strata on the western margin (faded patterns are inferred) are correlated to the distal offshore stratigraphic section at Rock Canyon, CO, based on biostratigraphic and lithostratigraphic data.  An interpreted relative sea level curve is shown at right (Approximate scale shows oscillations on the order of tens of meters).  Sea level fall events are based on correlation of prograding shoreface deposits on the western margin to regionally tracable skeletal carbonate accumulations and changes in biofacies in the central and eastern parts of the basin. Deepening events are based on retrograding shoreface intervals correlated basinward to intervals of enhanced TOC content and laminated shale deposition (wt. % TOC compiled from SEPM Guidebook No 4 and unpublished data).  Using the Obradovich (1993) time scale to constrain the duration of the Cenomanian interval that contains up to six possible sea level fall events (2.53 Myr) yields an average duration of 0.42 myr.  Although this timing is consistent with a long eccentricity modulator, it is difficult to confirm that these events are periodic.  However, they appear to be correlative with six Cenomanian sea level fall events identified by Gale et al. (2002). [Figure modified from Sageman, 1991].

 

Figure 4-10  (Forster et al.) Interpretation of middle Turonian third- and fourth-order sea level fluctuations and watermass interaction in the central Western Interior Seaway based on analysis of small-scale cycles in the Carlile Shale from the Amoco Rebecca Bounds Core (Kansas). The biomarker and d18O data indicate a strong but fluctuating freshwater influence.

 

Figure 4-11 (Hancock) Comparison of radiometrically interpolated and biostratigraphically correlated versions of the Haq et al. (1987) sea level curve with the Hancock (1990) sea level curves for northwest Europe the Campanian-Maastrichtian. Differences in the timing of the transgressive peaks and regressive troughs is caused by differences in the biozonal schemes, stage boundary definitions, and time scales that are used for each curve.

 

Figure 4-12 (Bice et al.) Preliminary mid-Cretaceous experiments have been performed with an atmospheric general circulation model that includes water isotopes in the hydrologic cycle. These indicate that warm climate high latitude freshwater would have been much less depleted in 18O than in the modern. Winter (July) precipitation over Antarctica in the mid-Cretaceous experiments is -10 to -30‰ (SMOW), compared to the modern -20 to -60‰.

 

Figure 4-13 (Bice et al.) This graph allows estimation of the shift in mean ocean d18O (vertical axis) given growth or decay of an ice-sheet of a given average composition (horizontal axis) and volume (diagonal lines). A mid-Cretaceous ice-sheet 50% the volume of the modern Antarctic ice with an average composition of -20 per mil or heavier could produce a shift in mean ocean d 18O of no more than 0.2‰. If mid-Cretaceous ice was so much less depleted than modern ice, the model suggests that a substantial volume could have existed without producing a shift larger than the interspecies isotopic offsets among many benthic foraminifera.

 

Return to Sea Level Record text

 

Figures with captions - Atmospheric and Ocean Circulation in a Greenhouse World

Figure 5-1 (Hay) A) A classic view of Cretaceous atmospheric and oceanic circulation, based on analogy with the present ocean but showing here the reversal of the thermohaline circulation that has been proposed by several authors. B) A new view of a possible Cretaceous atmospheric and ocean circulation, showing the effect of unstable westerly winds producing eddies which replace the general gyral circulation of today.

 

Figure 5-2 (Bice et al.) The colored curves show January sea surface temperature profiles predicted by the GENESIS model using various CO2 concentrations (1120-7500 ppm) and heat transport factors (Q=2-20). Solar luminosity was set to 99% of the modern for all runs except the 1120 ppm case, which used 99.2%. Symbols indicate upper ocean temperatures calculated from d18O of well-preserved planktonic foraminifera. Local water d18O is assumed to be -1.0 per mil (SMOW) with an adjustment for latitudinal variations in surface water (Zachos et al., 1994). The model shows that, in order to match the warmest tropical temperature estimates, 4500 ppm or more CO2 is required. If the lightest Late Turonian foram data at DSDP Site 511 indicate tropical-like summer (January) temperatures (Huber et al., 1995), then the model requires 6500 ppm CO2 or higher. However, the meaning of the very light isotopic event at Site 511 is as yet undetermined (Bice et al., this meeting).

 

Figure 5-3 (Valdes and Markwick) Zonal average Maastrichtian sea-surface temperature simulated with the Hadley coupled ocean atmosphere model. With similar CO2 concentrations, the Hadley coupled ocean atmosphere model generates much warmer Cretaceous temperature than the NCAR CSM.

 

Figure 5-4 (Otto-Bliesner et al.) Vertical sections of simulated ocean temperature and salinity at 30W longitude for present day and Cretaceous 1680 ppm CO2 coupled model experiments.

 

Figure 5-5 (Floegel et al.) GCM modeling of one complete precessional cycle, with emphasis on Western North America during the late Cretaceous (Cenomanian/Turonian boundary).

 

Figure 5-6 (Poulsen et al.) Mean annual upper ocean temperature and salinity difference resulting from the rifting of the Equatorial Atlantic Gateway during the mid-Cretaceous. Black shading represents the Cretaceous continents; gray shading marks the grid cells that were depressed in the opening of the gateway.

 

Figure 5-7 (Scotese) Cretaceous paleogeographic reconstructions for 65 Ma (K/T boundary), 80 Ma (early Campanian, 2 views), and 120 Ma (early Albian).

 

Figure 5-8 (Lawver) Detailed tectonic reconstruction of the Albian (105 Ma).

 

Figure 5-9 (Upchurch et al.) Geologic data and climate model predictions of latest Cretaceous vegetation.

 

Figure 5-10 (Scherer et al.) Mean annual temperature estimates for the Jose Creek leaf megaflora using different regression functions.

 

Figure 5-11 (Buffler) Mid Cretaceous deposition and erosion in the deep eastern Gulf of Mexico.

 

Return to Atmosphere and Ocean Circulation text      

 

Figures with captions – Consequences of Large Igneous Provinces

 

Figure 6-1 (Larson et al.) Timing comparison of the mid-Cretaceous igneous events proposed as causes for the two most prominent geological responses. Ontong Java and Manihiki Plateau formation proposed as cause for OAE 1a (Selli Event) and Caribbean Plateau formation proposed as cause for OAE 2 (Bonarelli Event).

 

Figure 6-2 (Duncan) Cartoon depicting a hydrothermal “event” plume produced by eruption of large volume (~1000 km3) lava flow during construction of an ocean plateau. High concentrations of certain metals (relative to trace concentrations in sea water) are carried to the ocean surface in the thermally buoyant plume. Many of these metals are normally bio-limiting, so their sudden availability could spur brief periods of high productivity. The metals are removed from the surface at differing rates and fractionated (near field and far field patterns), but ultimately transported to the sea floor on particles.

 

Figure 6-3 (Turgeon et al.) Potential geochemical paleoproductivity proxies within the Bonarelli horizon of the Gubbio Core, taken from central Italy.  Dashed vertical lines represent "Average shale" composition of Wedepohl (1971, 1991).  Darker shaded area represent times of increased P/Al ratios.

 

Figure 6-4 (Ravizza et al.) High temporal resolution records of seawater Osmium (Os) isotope variation have the potential to better constrain the timing of LIP emplacement relative to important stratigraphic horizons, such as OAEs and episodes of faunal change. Two major OAEs occur near the initiation of major negative excursions in the marine Sr isotope record. The long marine residence time of Sr and the similar Sr isotope signatures of LIP and MORB volcanism preclude the possiblity of using Sr data to test the hypothesis that LIP emplacement played a causative role in these Cretaceous OAEs. The marine residence time of Os is much shorter than that of Sr allowing this system to respond more quickly to rapid perturbations in oceanic inputs. Moreover, the Os isotope signature associated with LIP emplacement may be enhanced relative to Sr because the alleged source region of LIPs is the core-mantle boundary, a domain in the deep Earth that is very enriched in siderophile elements like Os. Although there are only very few data constraining the Cretaceous seawater Os isotope record, low temporal resolution preliminary data from a sediment sequences in Oman (Ravizza, unpublished) and in Cyprus (Ravizza et al. 2001) suggest that an excursion toward more mantle-like 187Os/188Os ratios may occur close to the C-T OAE.

 

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References

 

Arthur, M.A., and Schlanger, S.O., 1979. Cretaceous "Oceanic Anoxic Events" as causal factors in development of reef-reservoired giant oil fields. Amer. Assoc. Petrol. Geol. Bull., 63, 870-885.

Arthur, M.A., Dean, W.E., and Schlanger, S.O., 1985. Variations in global carbon cycling during the Cretaceous related to climate, volcanism, and changes in atmospheric CO2 . In Sundquist, E.T., and Broecker, W.S. (Eds), The Carbon Cycle and Atmospheric CO2: Natural Variations Archean to Present. Geophys. Monogr., Am. Geophyics. Union, 32, 504-529.

Arthur, M.A., Schlanger, S.O., and Jenkyns, H.C., 1987. The Cenomanian-Turonian Oceanic Anoxic Event II, paleoceanographic controls on organic matter production and preservation. In Brooks, J., and Fleet, A. (Eds), Marine Petroleum Source Rocks, Geol. Soc. London Spec. Publ. 24, pp. 399-418.

Arthur, M.A., Brumsack H.-J., Jenkyns, H.C., and S.O. Schlanger, 1990, Stratigraphy, geochemistry, and paleoceanography of organic carbon-rich Cretaceous sequences, in Cretaceous Resources, Events, and Rhythms, edited by R.N. Ginsburg and B. Beaudoin, B., Kluwer Acad. Publ, pp. 75-119.

Baker, E.T., Feely, R A; Mottl, M J, Sansone, F. T., Wheat, C. G., Resing, J. A., Lupton, J. E., Hydrothermal plumes along the East Pacific Rise, 8 degrees 40' to 11 degrees 50'N; plume distribution and relationship to the apparent magmatic budget, Earth and Planetary Science Letters, vol.128, no.1-2, pp.1-17, 1994.

Barrera, E., and Savin, S.M., 1999. Evolution of late Campanian Maastrichtian marine climates and oceans. In Barrera, E., and Johnson, C.C. (Eds), Evolution of the Cretaceous Ocean-Climate System. Geol. Soc. Am., Spec. Paper, 332, 245-282.

Barron, E.J., 1983. A warm, equable Cretaceous: The nature of the problem. Earth Science Review,19, 305-338.

Barron, E. J., Arthur, M. A., and Kauffman, E. G., 1985, Cretaceous rhythmic bedding sequences: A plausible link between orbital variations and climate, Earth Planet. Sci. Lett., 72, 327-340.

Berner, R. A., 1990, Global biogeochemical cycles of carbon and sulfur and atmospheric O over Phanerozoic time, Chemical Geology, 84, 159.

Bice, K. L., and Norris, R. D., 2003, Possible atmospheric CO2 extremes of the warm mid-Cretaceous (late Albian-Turonian), Paleoceanography, in press.

Bice, K. L., Huber, B. T., and Norris, R. D., Extreme polar warmth during the Cretaceous greenhouse?: Paradox of the late Turonian d18O record at DSDP 511, Paleoceanography, in review.

Bralower, T. J., and Thierstein, H. R., 1984, Low productivity and slow deep-water circulation in mid-Cretaceous oceans, Geology, 12, 614-618.

Bralower, T. J., Arthur, M. A., Leckie, R. M., Sliter, W. V., Allard, D.J., and Schlanger, S. O., 1994. Timing and paleoceanography of oceanic dysoxia/anoxia in the Late Barremian to Early Aptian. Palaios, 9, 335-369.

Bralower, T. J., Fullagar, P. D., Paull, C. K., Dwyer, G. S., and Leckie, R. M., 1997. Mid-Cretaceous strontium-isotope stratigraphy of deep-sea sections. Geological Society of America Bulletin, 109, 1421-1442.

Bralower, T.J., CoBabe, E., Clement, B., Sliter, W.V., Osburne, C., and Longoria, J., 1999. The record of global change in mid-Cretaceous, Barremian-Albian sections from the Sierra Madre, northeasterm Mexico. In Huber, B.T., Bralower, T.J., and Leckie, R.M. (Eds), A memorial volume to William V. Sliter. J. Foraminiferal Res., 29, 418-437.

Brass, G.W., Southam, J.P., and W.H. Peterson, Warm saline bottom water in the ancient ocean, Nature, 269, 620-623, 1982.

Caron, M., Robaszynski, F., Amedro, F., Baudin, F., Deconinck, J.-F., Hochuli, P., Salis-Perch Nielsen, K., and N. Tribovillard, 1999, Estimation de la durée de l'événement anoxique global au passage Cénomanien/Turonien. Approche cyclostratigraphique dans la formation Bahloul en Tunisie centrale, Bull. Soc. géol. France, 170, 145-160.

Channell, J.E.T., Cecca, F., and Erba, E., 1995, Correlations of Hauterivian and Barremian, Early Cretaceous stage boundaries to polarity chrons. Earth and Planetary Science Letters, 134, 125-140.

Cifelli et al., 1997, Proc Natl Acad. Sci., 94, 11163-11167.

Clarke, L.J., and Jenkyns, H.C., 1999. New oxygen isotope evidence for long-term Cretaceous climatic change in the Southern Hemisphere, Geology, 27, 699-702.

Coffin, M.F., and Eldholm, O., 1994, Large igneous provinces: Crustal structure, dimensions, and external consequences. Rev. Geophys., 32, 1-36.

DeConto, R. M., Brady, E. C., Bergengren, J., and Hay, W. W., 2000, Late Cretaceous climate, vegetation, and ocean interactions, in Huber, B. T., MacLeod, K. G., and Wing, S. L., eds., Warm Climates in Earth History, Cambridge, pp. 275-296.

Duncan, R.A., 2002, A time frame for construction of the Kerguelen Plateau and Broken Ridge. J. Petrol., 43, 1109-1119.

Duncan, R.A. and Hargraves, R.B., 1984. Plate tectonic evolution of the Caribbean region in the mantle reference frame. Geol. Soc. Amer. Mem. 162, pp. 81-93.

Duncan, R.A. and Huard, J., 1997, Trace metal anomalies and global anoxia: The OJP-Selli hydrothermal plume connection. EOS, Trans. Amer. Geophys. Union, 78, F774.

Duncan, R.A., and Richards, M.A., 1991. Hotspots, mantle plumes, flood basalts, and true polar wander. Rev. Geophys., 29, 31-50.

Elder, W. P.,1989, Molluscan extinction patterns across the Cenomanian-Turonian stage boundary in the Western Interior of the United States, Paleobiology, 15, 299-320.

Elder, W. P., 1991, Molluscan paleoecology and sedimentation patterns of the Cenomanian-Turonian extinction interval in the southern Colorado Plateau region, Geological Society of America Special Paper 260, pp. 113-137.

Elder, W. P., Gustafson, E.R., and Sageman, B.B., 1994, Correlation of basinal carbonate cycles to nearshore parasequences in the Late Cretaceous Greenhorn Seaway, Western Interior, U.S.A., GSA Bulletin, 106, 892-902.

Erba, E., 1986, I Nannofossili calcarei nell'Aptiano-Albiano (Cretacico inferiore): biostratigrafia, paleoceanografia e diagenesi degli Scisti a Fucoidi del Pozzo Piobbico (Marche). PhD Thesis Univ. Milano, 313 pp., 26 tav., 48 fig., Milano.

Erba, E., 1992, Calcareous nannofossil distribution in pelagic rhythmic sediments (Aptian-Albian Piobbico core, central Italy), Riv. Ital. Paleont. Strat., 97, 455-484.

Erba, E., 1994, Nannofossils and superplumes: The early Aptian "nannoconid crisis," Paleoceanography, 9, 483-501.

Erbacher, J., Thurow, J., and Littke, R.,1996. Evolution patterns of radiolaria and organic matter variations: A new approach to identify sea-level changes in mid-Cretaceous pelagic environments, Geology, 24, 499-502.

Erez, J., and B. Luz, 1983, Experimental paleotemperature equation for planktonic foraminifera, Geochim. Cosmochim. Acta, 47, 1025-1031.

Fassell, M.L., and T.J. Bralower, 1999, Warm, equable mid-Cretaceous: Stable isotope evidence, in Evolution of the Cretaceous Ocean-Climate System, edited by E. Barrera and C.C. Johnson, Geol. Soc. Amer. Spec. Paper 332, pp. 121-142.

Fischer, A.G., and M.A. Arthur, 1977, Secular variations in the pelagic realm, in Deepwater Carbonate Environments, edited by H.E. Cook and P. Enos, Soc. Econ. Paleontol. Mineral. Spec. Publ. 25, pp. 19-50.

Föllmi, K.B., Weissert, H., Bisping, M., and H. Funk, 1994, Phosphogenesis, carbon-isotope stratigraphy, and carbonate platform evolution along the Lower Cretaceous northern Tethyan margin, Amer. Assoc. Petrol. Geol. Bull., 106, 729-746.

Frakes, L.A., Francis, J.E., and J.I. Syktus, 1992, Climate Modes of the Phanerozoic, Cambridge University Press, 274 pp.

Frank, T.D., and Arthur, M.A., 1999. Tectonic forcings of Maastrichtian ocean-climate evolution. Paleoceanography, 14, 103-117.

Gale, A. S., and five others, 2002, Global correlation of Cenomanian (Upper Cretaceous) sequences Evidence for Milankovitch control on sea level, Geology, 30, 291-294.

Gardner, M.H., 1995, Tectonic and eustatic controls on the stratal architecture of mid-Cretaceous stratigraphic sequences, central Western Interior Foreland Basin of North America, in,  Dorobek, S.L., and Ross, G.M., eds., Stratigraphic Evolution of Foreland Basins, SEPM Special Publication, 52, pp. 243-281.

Gradstein, F.M., Agterberg, F.P., Ogg, J.G., Hardenbol, J., Van Veen, P., Thierry, J., Huang, Z., 1995, A Triassic, Jurassic and Cretaceous time scale, SEPM Special Publication, 54, 95-126.

Haq, B.U., Hardenbol, J. and Vail, P.R., 1987, Chronology of fluctuating sea levels since the Triassic (250 million years to Present), Science, 235, 1156-1167.

Hancock, J. M., 1990, Sea-level changes in the British region during the Late Cretaceous, Proceedings of the Geologists' Association, 100, 565-594.

Hancock, J.M., 1993, Transatlantic correlations in the Campanian-Maastrichtian stages by eustatic changes of sea-level, in Hailwood, E. A. and Kidd, R. B., (eds.), High Resolution Stratigraphy, Geological Society Special Publication, No. 70, The Geological Society, London, pp. 241-256.

Harries, P.J., and Little, C.T.S., 1999, The early Toarcian (Early Jurassic) and the Cenomanian-Turonian (Late Cretaceous) mass extinctions; similarities and contrasts, Palaeogeography, Palaeoclimatology, Palaeoecology, 154, 39-66.

Herbin, J. P., Montadert, L., Mueller, C., Gomez, R., Thurow, J., and Wiedmann, J., 1986, Organic-rich sedimentation at the Cenomanian-Turonian boundary in oceanic and coastal basins in the North Atlantic and Tethys, in North Atlantic palaeoceanography, edited by Summerhayes, C. P., and Shackleton, N. J., Geological Society Special Publications, London, 21, pp. 389-422.

Herrle, J.O., 2001, Paleoceanographic and paleoclimatic implications on mid-Cretaceous black shale formation in the Vocontian basin and the Atlantic: Evidence from calcareous nannofossils and stable isotopes, PhD. Thesis Univ, Tubingen, 114 pp.

Huber, B.T., and Watkins, D.K., 1992, Biogeography of Campanian-Maastrichtian calcareous plankton in the region of the southern ocean: Paleogeographic and paleoclimatic implications, in The Antarctic paleoenvironment: a Perspective on Global Change, Antarctic research Series, 56, pp. 31-60.

Huber, B.T., Hodell, D.A., and C.P. Hamilton, 1995, Middle-Late Cretaceous climate of the southern high latitudes: Stable isotopic evidence for minimal equator-to-pole thermal gradients, Geol. Soc. Amer. Bull., 107, 1164-1191.

Huber, B.T., Leckie, R.M., Norris, R.D., Bralower, T.J., and E. CoBabe, 1999, Foraminiferal assemblage and stable isotopic change across the Cenomanian-Turonian boundary in the subtropical North Atlantic, Jour. Foram. Res., 29, 392-417.

Huber, B. T., Norris, R. D., and MacLeod, K. G., 2002, Deep sea paleotemperature record of extreme warmth during the Cretaceous, Geology, 30, 123-126.

Jenkyns, H.C., 1980, Cretaceous anoxic events: From continents to oceans. J. Geol. Soc. London, 137, 171-188.

Jenkyns, H.C., Gale, A.S., and Corfield, R.M., 1994, Carbon- and oxygen-isotope stratigraphy of the English Chalk and Italian Scaglia and its paleoclimatic significance. Geol. Mag., 131, 1-34.

Jones, C.E., and H.C. Jenkyns, 2001, Seawater strontium isotopes, Oceanic Anoxic Events, and seafloor hydrothermal activity in the Jurassic and Cretaceous, Amer. Jour. Science, 301, 112-149.

Kerr, A.C., 1998, Oceanic plateau formation: A cause of mass extinction and black shale deposition around the Cenomanian-Turonian boundary, Jour. Geol. Soc. London, 155, 619-626.

Kominz, M.A., 1984, Oceanic ridge volumes and sea-level change: An error analysis, in Interregional Unconformities and Hydrocarbon Accumulation, edited by J.S. Schlee, Amer. Assoc. Petrol. Geol. Mem. 36, pp. 109-127.

Kuhnt et al., 1990.

Kuhnt, W., Nederbragt, A.J., and Leine, L., 1997, Cyclicity of Cenomanian-Turonian organic-carbon-rich sediments in the Tarfaya Atlantic Coastal Basin, Morocco), Cretaceous Research, 18, 587-601.

Kuypers, M.M.M., Pancost, R.D., and J.S. Sinninghe Damsté, 1999, A large and abrupt fall in atmospheric CO2 concentration during Cretaceous times, Nature, 399, 342-345.

Larson, R.L., 1991. Latest pulse of the Earth: Evidence for a mid Cretaceous super plume, Geology, 19, 547-550.

Larson, R. L., 1991, Geological consequences of superplumes, Geology, 19, 963-966.

Larson, R. L., and E. Erba, 1999, Onset of the mid-Cretaceous greenhouse in the Barremian-Aptian: Igneous events and the biological, sedimentary, and geochemical responses, Paleoceanography, 14, 663-678.

Laurin, J., and Sageman, B.B., 2001, Tectono-sedimentary evolution of the western margin of the Colorado Plateau during the latest Cenomanian and Early Turonian, in Erskine, M.C., Faulds, J.E., Bartley, J.M., and Rowley, P. (eds.), Symposium Volume: Geologic Transition between the Great Basin and the Colorado Plateau (Cedar City, Sept. 2001), Utah Geological Association Pub. 30, 57-74.

Leckie, R.M., Bralower, T.J., and Cashman, R., 2002, Oceanic anoxic events and plankton evolution: Biotic response to tectonic forcing during the mid-Cretaceous. Paleoceanography, 17, 10.1029/2001PA000623.

Leithold, E.L., 1994, Stratigraphical architecture at the muddy margin of the Cretaceous Western Interior Seaway, southern Utah, Sedimentology, 41, 521-542.

Li, L. and Keller, G., 1998, Maastrichtian climate, productivity and faunal turnovers in planktic foraminifera in South Atlantic DSDP sites 525A and 21, Marine Micropaleontology, 33, 55-86.

Menegatti, A.P., Weissert, H., Brown, R.S., Tyson, R.V., Farrimond, P., Strasser, A., and Caron, M., 1998, High-resolution d13C-stratigraphy through the early Aptian "Livello Selli" of the Alpine Tethys, Paleoceanography, 13, 530-545.

Meyers, S. R., Sageman, B. B., and Hinnov, L. A., 2001, Integrated quantitative stratigraphy of the Cenomanian-Turonian Bridge Creek Limestone Member using evolutive harmonic analysis and stratigraphic modeling, Journal of Sedimentary Research, 71, 628-644.

Miall, A.D., 1992, The Exxon global cycle chart: An event for every occasion? Geology, 20, 787-790.

Miller, K. G., Barrera, E., Olsson, R. K., Sugarman, P. J., and Savin, S. M., 1999, Does ice drive early Maastrichtian eustasy?, Geology, 27, 783-786.

Niebuhr, B., 1995. Fazies-Differenzierungen und ihre Steuerungsfaktoren in der höheren Oberkreide von S-Niedersachen / Sachsen-Anhalt (N- Deutschland). Ber. Geowiss. Abh. Reihe A Band 174, 1-131.

Niebuhr, B., Wood, C.J., Ernst, G., 2000. Isolierte Oberkreide – vorkommen zwischen Wiehengebirge und Harz, in Hiss, M., Schönfeld, J., Thiermann, A. (Eds.), Stratigraphie von Deutschland III. Die Kreide der Bundesrepublik Deutschland. Courier Forschunginstitut Senckenberg, 226, Frankfurt am Main, pp. 101-109.

Norris, R.D., and P.A. Wilson, 1998, Low-latitude sea-surface temperatures for the mid-Cretaceous and the evolution of planktic foraminifera, Geol., 26, 823-826.

Olsson, R. K., Wright, J. D., and Miller, K. G., 2001, Paleobioeography of Pseudotextularia elegans during the latest Maastrichtian global warming event, Journal of Foraminiferal Research, 31, 275-282.

Pearson, P.N., Ditchfield, P.W., Singano, J., Harcourt-Brown, K.G., Nicholas, C.J., Olsson, R.K., Shackleton, N.J., and Hall, M.A., 2001, Warm tropical sea surface temperatures in the Late Cretaceous and Eocene epochs, Nature, 413, 481-487.

Pitman, I.W.C. and Golovchenko, X., 1983, The effect of sea-level change on the shelf edge and slope of passive margins, in Stanley, D. J. and Moore, G. T. (eds.), The Shelfbreak: Critical interface on continental margins, Society of Economic Paleontologists and Mineralogists Special Publication 33, Tulsa, Oklahoma, pp. 41-58.

Poulsen, C.J., Gendaszek, A.S., and Jacob, R.L., 2003, Did the rifting of the Atlantic Ocean cause the Cretaceous thermal maximum?, Geology, in press.

Premoli Silva, I., and Sliter, W.V., 1999, Cretaceous Paleoceanography: Evidence from planktonic foraminiferal evolution, in Barrera, E., and Johnson, C.C., eds., The Evolution of the Cretaceous Ocean-Climate System, Geol. Soc. Am., Spec. Paper, 332, 301-328.

Prokoph, A., Villeneuve, M., Agterberg, F. P., and Rachold, V., 2001, Geochronology and calibration of global Milankovitch cyclicity at the Cenomanian-Turonian boundary, Geology, 29, 523-526.

Rau, G. H., Arthur, M. A., and Dean, W. E., 1987, 15N/14N variations in Cretaceous Atlantic sedimentary sequences: Implication for past changes in marine nitrogen biogeochemistry, Earth and Planetary Science Letters, 82, 269-279.

Ravizza, G., Blusztajn, J., and Prichard, H. M., 2001. Re-Os systematics and platinum-group element distribution in metalliferous sediments from the Troodos Ophiolite, Earth and Planetary Science Letters, 188, 369-381.

Renne, P.R., Glen, J.M., Milner, S.C., and Duncan, A.R., 2001, Age of Etendeka flood volcanism and associated intrusions in southwestern Africa. Geology, 24, 659-662.

Rowley, D. B. and Markwick, P. J., 1992, Haq et al. eustatic sea level curve: Implications for sequestered water volumes, Journal of Geology, 100, 703-715.

Rubin, K., 1977, Degassing of metals and metalloids from erupting seamount and mid-ocean ridge volcanoes: Observations and predictions. Geochim. Cosmochim. Acta, 61, 3525-3542.

Sageman, B.B., 1996, Lowstand tempestites: Depositional model for Cretaceous skeletal limestones, Western Interior, U.S., Geology, 24, 888-892.

Sageman, B. B., 1998, Analysis of mechanisms of relative sea level change in the Western Interior basin based on study of fine-grained basinal facies, American Association of Petroleum Geologists, Annual Meeting Expanded Abstracts - American Association of Petroleum Geologists, v.1998.

Sageman, B B, Rich, J., Arthur, M.A. Birchfield, G.E., Dean, W.E., 1997, Evidence for Milankovitch periodicities in Cenomanian-Turonian lithologic and geochemical cycles, Western Interior U.S.A., Journal of Sedimentary Research, 67, 286-302.

Savrda, C.E., 1998, Ichnology of the Bridge Creek Limestone: Evidence for spatial and temporal variations in paleo-oxygenation in the Western Interior Seaway, in W.E. Dean and M.A. Arthur, eds., Stratigraphy and Paleoenvironments of the Cretaceous Western Interior Seaway, U.S.A., Society Economic Paleontologists Minerologists, Concepts in Sedimentology and Paleontology 6, 127-136.

Schlanger, S.O., and Jenkyns, H.C., 1976. Cretaceous oceanic anoxic events: Causes and consequences. Geol. Mijnbouw, 55, 179-184.

Scholle, P.A., and Arthur, M.A., 1980, Carbon isotope fluctuations in Cretaceous pelagic limestones: Potential stratigraphic and petroleum exploration tool. AAPG Bull., 64, 67-87.

Shackleton, N.J., and J.P. Kennett, 1975, Paleotemperature history of the Cenozoic and the initiation of Antarctic glaciation: Oxygen and carbon isotope analysis in DSDP Sites 277, 279, and 280, in Initial Reports of the Deep Sea Drilling Project, edited by J.P. Kennett, R.E., Houtz, et al., Washington, U.S. Govt. Printing Office, 29, pp. 743-755.

Sinton, C.W. and Duncan, R.A., 1997, Potential links between ocean plateau volcanism and global ocean anoxia at the Cenomanian-Turonian boundary. Econ. Geol., 92, 836-842.

Stoll, H.M., and Schrag, D.P., 1996, Evidence for glacial control of rapid sea level changes in the Early Cretaceous. Science, 272, 1771-1774.

Stoll, H. M. and Schrag, D. P., 2000, High-resolution stable isotope records from the Upper Cretaceous rocks of Italy and Spain: Glacial episodes in a greenhouse planet?, Geological Society of America Bulletin, 112, 308-319.

Tarduno, J.A., Sliter, W.V., Kroenke, L., Leckie, R.M., Mayer, H., Mahoney, J.J., Musgrave, R., Storey, M., and Winterer, E.L., 1991, Rapid formation of Ontong Java Plateau by Aptian mantle volcanism. Science, 254, 399-403.

Tarduno, J., Brinkman, D. B., Renne, P. R., Cottrell, R. D., Scher, H., and Castillo, P., 1998, Evidence for extreme climatic warmth from Late Cretaceous Arctic vertebrates, Science, 282, 2241-2244.

Tibert, N.E., Leckie, R.M., Eaton, J.G., Kirkland, J.I., Colin, J.-P., Leithold, E.L., and McCormic, M.E., 2002, Recognition of relative sea level change in Upper Cretaceous coal-bearing strata: A paleoecological approach using agglutinated foraminifera and ostracodes to detect key stratigraphic surfaces, in, Olson, H.C., and Leckie, R.M., eds., Micropaleontologic Proxies of Sea Level Change and Stratigraphic Discontinuites, SEPM Special Publication 75, in press.

Vail, P.R., Mitchum, R.M.Jr., and Thomson, S.I., 1977, Seismic stratigraphic and global changes of sea level, part 4: Global cycles of relative changes of sea level, in Payton, C. E. (eds.), Seismic Stratigraphy-Applications to Hydrocarbon Exploration, American Association of Petroleum Geologists Memoir, Tulsa, OK, 26, 83-97.

Vogt, P.R., 1989, Volcanogenic upwelling of anoxic nutrient-rich water: A possible factor in carbonate-bank/reef demise and benthic faunal extinctions, Geol. Soc. Amer. Bull., 101, 1225-1245.

Weissert, H., and Lini, A., 1991, Ice age interlude during the time of Cretaceous greenhouse climate?, in Müller, D.W., McKenzie, J.A., and Weissert, H., eds., Controversies in Modern Geology, London, Academic Press, pp. 173-191.

Weissert, H., Lini, A., Föllmi, K.B., and Kuhn, O., 1998, Correlation of Early Cretaceous carbon isotope stratigraphy and platform drowning events: A possible link?, Palaeogeography, Palaeoclimatology, Palaeoecology, 137, 189-203.

Wilson, P. A. and Norris, R. D., 2001, Warm tropical ocean surface and global anoxia during the mid-Cretaceous period, Nature, 412, 425-429.

Wilson, P. A., Norris, R. D., and Cooper, M. J., 2002, Testing the mid-Cretaceous greenhouse hypothesis using "glassy" foraminiferal calcite from the core of the Turonian tropics on Demerara Rise, Geology, 30, 607-610.

Zachos, J.C., Stott, L.D., and Lohmann, K.C., 1994, Evolution of early Cenozoic marine temperatures, Paleoceanography, 9, 353-387.

Zachos, J., Pagani, M. Sloan, L., Thomas, E., and Billups, K., 2001, Trends, Rhythms, and Aberrations in Global Climate 65 Ma to Present , Science, 292, 686-693.

Ziegler et al., 1997

 

 

 

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