collaborative research; the dynamics of ...silab/biocomplex/proposal_short.pdfthe strategy will...

B-1

COLLABORATIVE RESEARCH; THE DYNAMICS OF CARBON RELEASE AND SEQUESTRATION: CASE STUDIES OF TWO EARLY EOCENE HYPERTHERMALS

Intellectual Merit: The ocean is the largest sink for anthropogenic CO2 and has absorbed nearly 130 PgC of the 380 PgC emitted to the atmosphere since the onset of the Industrial Revolution. If emissions continue to rise unabated for the next three centuries, an additional 4000 PgC or more will be input to the atmosphere and ocean. Published model simulations of the ocean/atmosphere response to the eventual complete utilization of fossil fuels indicate that atmospheric CO2 will rise to levels that Earth likely hasn’t experienced for at least 40 million years, and the surface ocean may undergo acidification to the extent that corals and other calcifying organisms will be unable to precipitate their skeletons.

Confidence in and refinement of these model simulations will benefit from application to, and comparison with, analogous events in Earth history. Approximately 55 million years ago (Mya), Earth experienced a similar episode of rapid and extreme transient warming, the Paleocene-Eocene Thermal Maximum (PETM), likely the product of massive carbon release. Intense study of the PETM over the last five years has led to a far clearer understanding of the consequences of this event on climate, biota, and biogeochemical cycles. One of the more prominent advances is the documentation of evidence for widespread ocean acidification and buffering, consistent with carbon cycle theory. A related advance was the discovery of second warming and ocean acidification event at ~53 Mya. This event, known as ELMO, was less extreme than the PETM in every sense, from the carbon cycle perturbation to the magnitude of warming. Advances have been accelerated by the recovery of spectacular new marine and terrestrial records of the two events, by new proxies for environmental reconstruction, and by techniques to resolve time to within a few thousand years.

The ancient global warming events, termed hyperthermals, provide a unique opportunity to gain insight into the long-term impacts of rapidly rising CO2 levels on modern climate, ocean carbonate chemistry, and biotas. They also provide an opportunity to identify potential non-linear feedbacks, and test climate and biogeochemical model sensitivity. To this end, an interdisciplinary group of scientists with expertise in carbon cycle dynamics, sediment geochemistry, paleoceanography and paleobiology has been assembled, and will embark on a 4-year project to address critical questions regarding two hyperthermals, and their implications for understanding of the carbon cycle including: 1) what were the mass, rate, and origin of carbon released during the hyperthermals? 2) what were the rates of sequestration and recovery and what biogeochemical feedbacks came into play? and 3) how did associated extreme changes in ocean carbonate chemistry affect planktonic calcifiers? The strategy will involve integration of the observational database with numerical models. The observational database group will be responsible for providing the essential data for constraining and testing the carbon cycle models. This includes records of biogenic carbonate production, accumulation and preservation in 3-dimensions through the PETM and ELMO. This effort will require substantial refinement of age models. With a highly resolved and multifaceted data set for input, three modeling approaches will be used, each involving specific opportunities and compromises in terms of the time scales and scope of processes that can be modeled. Earth system models (GENIE and CCSM) will provide boundary conditions for the process-oriented models. Process model simulations will be designed to investigate problems identified during data/model validation of the Earth system models and to develop hypotheses to be tested with model simulations. Broader Impacts: This highly interdisciplinary project will provide important insight into the short-term and long-term fate of anthropogenic CO2 on the global carbon cycle, climate, and biota. Such information is essential to providing scientific leaders and policy makers with a better sense of the consequences of unabated anthropogenic CO2 emissions for global climate, ocean carbon chemistry and marine food chains. Moreover, the project places significant emphasis on a number of closely integrated research and educational activities that will lead to the development and circulation of educational materials related to abrupt climate change and training in how to integrate them in curricula. In addition, we will take advantage of highly successful existing programs to provide opportunities for undergraduates from under-represented groups to participate in cutting-edge, relevant, carbon-cycle research.

0628719

TABLE OF CONTENTSFor font size and page formatting specifications, see GPG section II.C.

Total No. of Page No.*Pages (Optional)*

Cover Sheet for Proposal to the National Science Foundation

Project Summary (not to exceed 1 page)

Table of Contents

Project Description (Including Results from Prior

NSF Support) (not to exceed 15 pages) (Exceed only if allowed by aspecific program announcement/solicitation or if approved inadvance by the appropriate NSF Assistant Director or designee)

References Cited

Biographical Sketches (Not to exceed 2 pages each)

Budget (Plus up to 3 pages of budget justification)

Current and Pending Support

Facilities, Equipment and Other Resources

Special Information/Supplementary Documentation

Appendix (List below. )

(Include only if allowed by a specific program announcement/solicitation or if approved in advance by the appropriate NSFAssistant Director or designee)

Appendix Items:

*Proposers may select any numbering mechanism for the proposal. The entire proposal however, must be paginated.Complete both columns only if the proposal is numbered consecutively.

1

1

15

8

4

12

2

2

0

0628719





Table of Contents



References Cited








Appendix Items:


1

0

4

7

4

1

0

0628486





Table of Contents



References Cited








Appendix Items:


1

0

2

6

1

1

0

0628394





Table of Contents



References Cited








Appendix Items:


1

0

2

7

1

1

0

0628302





Table of Contents



References Cited








Appendix Items:


1

0

2

10

1

1

0

0628336





Table of Contents



References Cited








Appendix Items:


1

0

2

6

1

1

0

0628366





Table of Contents



References Cited








Appendix Items:


1

0

2

7

1

2

0

0628358





Table of Contents



References Cited








Appendix Items:


1

0

2

6

1

1

0

0628387

C-1

RESULTS FROM PRIOR NSF SUPPORT

J.C. Zachos, T.J. Bralower, L.R. Kump - EAR-0120727: Consequences of greenhouse warming forbiocomplexity and biogeochemical cycles: A multidisciplinary case study across the Paleocene-Eoceneboundary : 10/01-9/06; $2.5 million (w/ 7 other investigators). Supported 12 graduate and 15undergraduates, and 55 publications (http://es.ucsc.edu/~silab/biocomplex/researchnews_pubs.htm; Last 2:Kelly et al. 2005, Paleoceanography; Bowen et al., in press, EOS)G. Bowen – No prior NSF supportK.A. Farley - EAR-9909448: Assessing the pace of a rapid climatic event: the late Paleocene thermalmaximum: 12/99-11/01; $88,192. Supported 1 graduate student, 1publication Farley & Eltgroth, (2003).M. Pagani – OCE-0095734: Collaborative Research: Reconstruction of Paleogene alkenone-basedεp records. 8/02-8/05; $155,129 to Yale U., 1 publication (Pagani et al., 2005), others in progress.H. Stoll OCE-0424474 (SGER). Improving the utility of paleoproxies from coccolith chemistry: calibrationand analytical advances. 5/04-4/06; $50,000. Supported 6 undergraduates (3 summer, 3 academic yearRA), 2 publications in review, others in prep.A. Winguth – No prior NSF supportR. Zeebe – OCE-05-25647: Deciphering climate archives: Establishing the inorganic basis of an isotopefractionation phenomenon in biogenic CaCO3: 08/05-07/08; $242,962 (PI: Zeebe).Supports 1 graduate and 2 undergraduates, work/publications in progress.

MOTIVATIONThe capacity of the ocean to absorb anthropogenic CO2 is controlled largely by its ability to buffer the

pH and carbonate ion concentration [CO32-] through several mechanisms or feedbacks, each of which

operates on different time scales (Ridgwell and Zeebe, 2005). On time scales of thousands of years, themost important feedback involves the dissolution of carbonate sediments on the seafloor, which can restorepH and [CO3

2-], and thus allow the ocean to absorb additional carbon (Archer et al., 1997). The majority ofcarbonate sediment, however, resides on the deep sea floor. As a consequence, the process of bufferingthrough carbonate dissolution is paced partly by the rate at which ocean overturn can deliver acidifiedwater to the deep sea. Because the rate of overturn, roughly 103 y, is comparatively slow relative to the rateof emissions, CO2 is rapidly accumulating in the atmosphere. In theory, with several mixing cycles, thebulk of the anthropogenic carbon will slowly propagate into the deep sea, and trigger widespreaddissolution of carbonate, thereby sequestering CO2 at a predictable rate. As the system drifts further frompresent conditions, however, the rate of sequestration could deviate from predictions. For one, the rate ofoceanic overturn should slow as high-latitude surface waters become warmer and fresher, which wouldreduce absorption. Also, the chemical erosion of seafloor carbonate is limited by the rate of resupply offresh carbonate sediment via bioturbation (Archer and Maier-Reimer, 1994). Should the organismsresponsible for bioturbation disappear, say for a lack of oxygen or warmer temperatures, then the resupplyof carbonate for weathering should cease as well. On even shorter time scales, the export production ofcarbon, which is controlled by factors such as production and flux of calcareous algae, could change withacidification and climate change. Each of these potential surprises increases the degree of uncertainty inforecasts of ocean carbon absorption and sequestration.

To evaluate our theoretical understanding of the complex processes that govern the carbon cycle, and totest the sensitivity of coupled climate/biogeochemical models to extreme forcing, researchers areincreasingly turning to Earth’s past to study periods of rapid greenhouse warming. Of particular interest is atransient global warming event characterized by a carbon cycle perturbation at the Paleocene-Eoceneboundary 55 Mya referred to as the Paleocene-Eocene Thermal Maximum (PETM). As evidenced by aprominent carbon isotope excursions (CIE) and global deep-sea dissolution horizon (Fig. 1), the PETM wasaccompanied by the release of ~4000 PgC over a period significantly shorter than the residence time ofcarbon in the ocean (<10 ky; Zachos et al., 2005). Interestingly, this carbon release, which left an indelibleimprint in the sedimentary and fossil record, may not have been as large as the potential input of carbonfrom fossil-fuel burning.

0628719

C-2

Figure 1. The clay horizon and CaCO3content in deep sea cores recoveredfrom Walvis Ridge during ODP Leg208 (Zachos et al., 2004)

The last five years have seen a surge in our understanding of the dynamics of the PETM event includingfar more precise constraints of the range of climatic, biotic and biogeochemical responses on both short andlong time-scales. Significant discoveries have been made by an international team funded through NSF-Biocomplexity who have taken advantage of the recovery of spectacular new marine and terrestrial recordsof the event (e.g., Zachos et al., 2003; 2005; Bowen et al., 2004, in press; Wing et al., 2005; seehttp://es.ucsc.edu/~silab/biocomplex/index.htm for more information) as well as the development ofpowerful new geochemical proxies (Zachos et al., submitted). In addition, we now recognize that thePETM was not unique: a second event, referred to as ELMO (Lourens et al., 2005), occurred some twomillion years later and exhibits many of the same features of the PETM. While the pace of discovery hasbeen rapid, the exact cause(s) of these events is still a matter of debate and we have been unable to fullyquantify the processes responsible for evaluation of the long-term carbon cycle recovery rates and modes ofsequestration, and to test models of how biogeochemical feedbacks work to buffer the ocean and sequestercarbon. In particular, uncertainties in chronology prevent us from fully interpreting the rates of carbonaddition during the onset of the events, and especially, removal during the recovery. Thus, ourunderstanding of the dynamics of these events and potential implications for present and future carboncycle perturbation is less than complete.

Here we propose a 4-year investigation focused on the dynamics of ocean carbon uptake andsequestration during two early Eocene hyperthermals, with a particular emphasis on the PETM. Thisinvestigation brings together an international team of experts in ocean and carbon cycle modeling, marineand sedimentary geochemistry, and paleoceanography, to jointly address, through data/model comparison,several key questions regarding the nature of the carbon cycle perturbations during these events; 1) Whatwere the mass, rate, and origin of carbon released during the events? 2) What were the rates ofsequestration and recovery and what biogeochemical feedbacks came into play? and 3) How did associatedextreme changes in ocean carbonate chemistry affect planktonic calcifiers?

EARLY EOCENE HYPERTHERMALSThe PETM (55 Mya), first documented 15 years ago, (Kennett and Stott, 1991), still represents the

most prominent rapid global warming event in Earth history linked to extreme greenhouse forcing.Evidence for a massive release of carbon includes a >3.0‰ negative carbon isotope excursion as recordedin marine and terrestrial fossils (e.g. Kelly et al., 1996; Koch et al., 1992) temporally coupled with aworldwide seafloor carbonate dissolution horizon (e.g., Bralower et al., 1997; Lu et al., 1998; Schmitz etal., 1996; Thomas et al., 1999; Thomas and Shackleton, 1996). The climatic impacts of this greenhouseforcing were significant. Sea-surface temperatures (SST) increasedby 5 °C in the tropics (Tripati and Elderfield, 2004; Zachos et al.,2003), by 6 to 9°C in the Arctic and sub-Antarctic, respectively(Kennett and Stott, 1991; Pagani et al., in press; Thomas et al.,1999), and by 4-6°C throughout the deep sea. Global humidity orprecipitation patterns changed as well (Pagani et al., in press;Robert and Kennett, 1994; Wing et al., 2005), as did deep-seacirculation patterns (Nunes and Norris, 2006; Thomas et al., 2003).

In recent years, significant progress has been made in detailingthe impacts of the PETM on ocean climate and biogeochemistry, inlarge part, because of the success of a series of Ocean Drillingexpeditions designed specifically to recover the boundary in depthtransects. These depth transects, spanning as much as 2 km,provided insight into depth dependent changes in ocean chemistry(Bralower et al., 2002; Lyle et al., 2002; Erbacher et al., 2004;Zachos et al., 2004). The PETM sections exhibited dissolutionpatterns consistent with models of ocean acidification, for example,shoaling of the lysocline and calcite compensation depth (CCD), byas much as 2 km in some regions (Fig. 1; Zachos et al., 2005).

0628719

C-3

These expeditions also confirmed the existence of a second hyperthermal, ELMO (Zachos et al., 2004),roughly 2 m.y. post-PETM (Lourens et al., 2005); Westerhold et al., 2005). This event exhibits many of thesame characteristics of the PETM including a transient warming and negative carbon isotope excursion,and dissolution horizons (Fig. 2). The magnitude of each, however, appears to be half that of the PETM.The CIE, which was first documented in multiple deep-sea cores by Cramer et al. (2003), also appears to bepresent in terrestrial records demonstrating that it was not a purely marine phenomenon (see onlinematerial; Lourens et al., 2005).

Figure 2. ODP Site 1262 high-resolution magneticsusceptibility (MS (a*)) and Fe concentration data fromcore logs and XRF scanner (Lourens et al., 2005;Westerhold et al., submitted), and bulk carbon isotopedata (McCarren et al., in prep.). Filter shows prominentcycles which reflect the 100 and 400 kyr eccentricitycycles. Precession cycles are numbered. Similar recordsexist for each site in the Leg 208 depth transect.

Finally, the high-resolution, strati-graphically complete composite sectionsrecovered during Leg 208 have proven to behighly suitable for astronomical tuning, andthus are being used to develop the first high-

resolution age models for the entire upper Paleocene and lower Eocene (Fig.2; Lourens et al., 2005;Westerhold et al., 2005). These tuned chronologies can be transferred to other sequences using high-resolution carbon isotope stratigraphy (e.g., Cramer et al., 2003), an achievement that will also allow us toframe these extreme perturbations within the context of the long- and short-term “background variability”in the time preceding and following the events.

CARBON FLUXES AND OCEAN ACIDIFICATIONIn theory, the extent of ocean acidification should scale with the mass of carbon, thus providing an

independent means of estimating the mass of carbon added to the ocean. Dickens and others (1995) positedthe release of 1200 PgC from decomposition of methane hydrates. The thermal decomposition ofsedimentary organics by a mantle plume penetrating the crust has been implicated as well (Svenson et al.,2004), as have the desiccation and oxidation of sedimentary organics in terrestrial soils (Kurtz et al., 2003)or shallow epicontinental seas (9000 PgC; Higgins & Schrag, 2004), and the introduction of extraterrestrialcarbon from a comet.

The first attempt to quantitatively estimate the mass of carbon released at the PETM via a model/datacomparison was accomplished using the Walker and Kasting (Walker and Kasting, 1992) carbon cycle boxmodel (Dickens et al., 1997; Dickens et al., 1995). Assuming a methane hydrate source for carbon (δ13C = -60‰), CIE equivalent excursions (∆δ13C = -2.5 to -3.0‰) and lysocline shoalings (followed byoverdeepenings) were simulated with a flux of 1200-2000 PgC over 10 ky, with a return to steady stateδ13C in ~120 ky. More recent investigations using coupled ocean models of intermediate complexity,funded under the 2001 NSF-Biocomplexity project, are providing new insight as to how other factors suchas ocean circulation, productivity, and dissolved oxygen influence carbonate deposition in 3-dimensions ona variety of spatial scales (Ridgwell et al., 2005; Panchuk et al., in prep.). For example, initial experimentssuggest that locally dysoxic bottom waters can amplify shifts in the lysocline and carbonate preservation.Such effects, if not recognized, would lead to inaccurate estimates of the global carbonate dissolutionfluxes as well as circulation patterns. These findings demonstrate the necessity of using dynamical modelsas a means of interpreting the sediment records of the hyperthermals.

0628719

C-4

RESEARCH OBJECTIVESThe early Eocene hyperthermals represent natural carbon cycle experiments involving rapid input of

carbon to the atmosphere/ocean on scales comparable to the modern anthropogenic forcing. The success ofrecent ODP expeditions in recovering spectacular quality and complete sections of these events in depthtransects coupled with recent advances in the development of coupled earth system models provide newopportunities to address the critical questions framed below. This effort, however, will require a highlyfocused, systematic reevaluation of how ocean carbon chemistry changed during such events, specificallyregarding the magnitude of the CIEs and variations in carbonate accumulation rates on a global scale. Itwill also require a carefully coordinated series of modeling experiments and integration of observationaldata. Consequently the objectives of this project, framed as critical questions, are as follows:

1) What was the mass and rate of carbon released during the hyperthermals and was this releaseinstantaneous or pulsed?

Detailed carbon isotope records exist for many marine and terrestrial PETM sections, and provide a keyconstraint for quantifying the mass and rate of carbon release to the ocean/atmosphere. However, twosignificant questions remain. First, the amplitude of the CIEs in pelagic, marine sections typically rangesfrom 2 to 4‰, while the CIE in terrestrial sections ranges from 5 to 6‰, so the true amplitude of carbonrelease remains uncertain. Second, coccolith and bulk carbonate isotope records show steps in the negativeisotope excursion which are not observed in planktonic foraminiferal (single specimen) records, so it isunclear whether carbon was released in a single instantaneous event or in multiple pulses that would reflectperiodic forcing or positive feedbacks. Resolution of both questions rests on identifying potentialbiological or vital effects on isotope fractionation which may bias components of marine or terrestrialrecords, and on assessing the degree to which variable dissolution of marine foraminifera and coccolithsmay alter the preserved isotopic record. For example, changing CO2 and humidity may amplify the CIE interrestrial records (e.g., Bowen et al., 2004) while ocean acidification and lower [CO3

2-] of surface waterscould diminish the marine CIE through a carbonate ion effect (e.g. Spero et al., 1997). An alternativehypothesis, that marine carbonate records were truncated by dissolution and sediment reworking, isconsistent with depth transects where minimum CIE values recorded in bulk carbonate increases with depth(Kelly et al., 1996; Zachos et al., 2005). A combination of dissolution and reworking could alsopotentially introduce steps in the marine carbon isotopic record, as could variable vital effects in coccolithisotopic fractionation.

To empirically address these issues, we need to identify and constrain potential artifacts associated withmicrofossil shell production and deposition. To start, accumulation rates must be more tightly constrained.Dissolution horizons should be associated with sharp spikes in the accumulation of extraterrestrial He(3HeET), and be more pronounced in deeper sites. Also, the lack of transitional δ13C values in singleplanktonic shells might be an artifact of sampling biases, which could be resolved by analyzing rare taxathat might have displaced common taxa during the transitions (Kelly et al., 1998). A second solution is tomeasure the δ13C of organic compounds. Recent investigations show the presence of n-alkanes derivedfrom terrestrial plant leaf waxes in marine PETM sections (Hasegawa et al., submitted; Pagani et al., inpress). The δ13C n-alk will allow for a direct measure of the δ13Cterr relative to the marine carbonate record.Another strategy involves targeting near-shore marine sections that are relatively expanded (Giusberti et al.,submitted; Zachos et al., submitted). And finally, interpretation of both marine and terrestrial archives ofδ13CDIC requires application of models that can evaluate the parameters that influence carbon isotopefractionation (e.g., Bowen et al., 2004). For this purpose, box models provide a fast and effective means ofsimulating the whole-ocean, time dependent C- isotope evolution over long time scales. However,circulation models that simulate the effects of deep-water aging and carbonate dissolution on sedimentationare clearly required to interpret the spatial variations recorded in bulk and benthic foraminiferal δ13Crecords.2) How do the magnitude and rate of carbon release during hyperthermals affect the scale of thechanges in the lysocline and CaCO3 accumulation rates?

0628719

C-5

This question can be addressed by distinguishing between the acidification phase when carbon wasbeing introduced and CCD/lysocline were rapidly shoaling, and the recovery phase, when carbon was beingbuffered and the same surfaces were deepening.

a) Acidification phase; carbonate undersaturation and chemical erosion. As discussed above, allPETM and ELMO sections are characterized by carbonate dissolution horizons. While dissolution is morepronounced at deeper sites, as expected (Fig. 1), spatially, there are significant differences in carbonatedeposition patterns that are difficult to reconcile with simple models of ocean acidification. For example,in the Southern Ocean PETM intervals at Sites 689 and 680, the carbonate content drops, but only to 75 and85% respectively, implying the local CCD did not shoal as much as elsewhere (Schellenberg et al., in prep).To the north, in the equatorial Atlantic, Caribbean, and North Atlantic, some sites show distinct clay layerswith little to no carbonate (Bralower et al., 1997), while others show less carbonate dissolution. Onehypothesis suggests that these spatial variations reflect the release and entry path of carbon into the deepsea. Alternatively, these trends may reflect the influence of circulation on local productivity,inorganic/organic carbon fluxes, and bottom water redox conditions (Ridgwell et al., 2005). These factorsmust be delineated to infer the full magnitude of carbonate dissolution.

b) Recovery phase: mass /rate of carbonate deposited (chalk layer). During recovery, deep-sea[CO3

2-] transitions (in ~20-40 ky) from an extreme undersaturated state to what appears to be asupersaturated state as characterized by pure white, rapidly-deposited coccolith-rich chalks (Farley andEltgroth, 2003; Kelly et al., 2005). The white chalk appears to be a common feature of most pelagic PETMsections. This response is not unexpected as carbon cycle models that utilize a sediment/rock weatheringfeedback exhibit this type of behavior. The oversaturation results directly from the loading of dissolvedions from accelerated dissolution of carbonates and silicates and, hence, reflects an important negativefeedback. As CO2 is extracted from the system during weathering and replaced with carbonate ion, [CO3

2-]rises forcing the carbonate saturation horizon to great depths, thus allowing the ocean to purge the excessions. As a consequence, carbonate sediment accumulation rates should rise. The issue we wish to resolve iswhere, and to what extent?

The magnitude of carbonate accumulation and carbon sequestration during the recovery intervalremains highly uncertain because contrasting age models imply significantly different rates. Application ofan orbital age model (Röhl et al., 2000) to the white chalk at Site 690, yields a duration of 100 ky, andcreates an inflection in the C-isotope curves, which if real would imply a relative decrease in the burial ofreduced carbon. In contrast, the 3HeET model (Farley and Eltgroth, 2003) implies a much faster carbonateaccumulation rate and shorter duration (20 ky) for the recovery interval. In addition, the 3HeET age modelimplies that the removal of carbon from the ocean-atmosphere system during this phase was nearly as rapidas its addition to the ocean-atmosphere system, <20 ky. From a purely theoretical point of view, we mightanticipate a rapid increase in carbonate accumulation rates during the period of supersaturation as thelysocline descends to the seafloor. Yet, increased carbonate/organic carbon burial ratios would haveworked against the rapid rise in δ13C implied by the 3HeET age model, unless increased carbonate ballastingalso elevated organic carbon burial fluxes (although the organic/inorganic burial ratio would also have toincrease). These apparent paradoxes require further investigation.

Here, astronomical stratigraphy and 3HeET will be used to improve the estimates of carbonateaccumulation on a global scale for the PETM and ELMO. Moreover, dissolution indexes, such asforaminiferal fragmentation and % coarse fraction will be used to constrain the position of the lysoclinerelative to the CCD. Because the differences in carbonate accumulation patterns almost certainly reflect onthe influence of circulation on local productivity, inorganic/organic carbon fluxes, and bottom water redoxconditions (Ridgwell et al., 2005), ocean models are required to assess these affects under a variety ofscenarios. Multiple simulations (sensitivity tests) will be required to gauge the potential effects of eachvariable using models that can simulate in 3-D each of critical controls on carbon fluxes and burial.

3) How did lower/higher pH and other environmental changes affect production and/or calcificationof coccolithophorids and foraminifera, and their relative contributions to fluxes?

0628719

C-6

In theory, the more rapid the rate of CO2 input to the atmosphere, the more extreme the changes insurface ocean pH and carbonate saturation state. In the modern ocean, planktonic calcifiers and corals arepotentially threatened by future increases in CO2 (e.g., Ridgwell and Zeebe, 2005). With the PETM andELMO, the major groups of planktonic calcifiers, coccolithophorids and foraminifera, did not experiencemajor extinction implying that surface ocean pH did not reach extinction levels. This would be consistentwith the relatively long period (>10 ky) over which the several thousand Pg of carbon were released. Still,significant changes in the relative abundances of coccoliths and planktonic foraminifera have beendocumented (Bralower, 2002; Kelly, 2002; Kelly et al., 1996). Some of the changes can be attributed towarming, increased stratification, and lower fertility. Did lower/higher pH have any noticeable impacts onthe calcification rates of coccolithophorids and foraminifera?

To address this, a systematic quantitative assessment of coccolithophorids and foraminiferalassemblages, size, morphology, calcification rates, and growth rates is required. Such an assessment willhelp elucidate the degree to which changes in carbonate accumulation rates reflect shifts in the productionby calcifying organisms vs. changes in the dissolution or preservation of carbonate. Trace metal indicatorsof growth rates and ocean chemistry, and isotope ratios will be measured on individual species at the levelof shells and chambers. Models of biogenic calcification will be required to interpret these data. Ultimately,these data will lead to improvements in the way our numerical models calculate changes in rates ofcalcification in the surface ocean resulting from ocean acidification events.

4) Was the mass of carbon released during the PETM substantially greater than during ELMO? Didfeedbacks play a role in amplifying the fluxes?

Given the findings from Objectives 2 and 3, can we quantify the mass and rate of carbon input to theocean during the hyperthermals? Computations based solely on the CIE magnitude cannot provide aunique solution. An independent constraint is required. The degree of the model-simulated oceanacidification required to match reconstructed CCD shifts in the Atlantic and Pacific allows an independentestimate of total carbon input. The simulations will provide a temporal analysis of CCD variations,carbonate accumulation rates, δ13C variations in surface and deep waters, and climate change, which, whenconstrained by observation, will permit assessment of magnitude, rate, and origin of the carbon released.Can the carbon flux from any one source (reservoir) account for the full mass of carbon added to theocean/atmosphere? If not, what are the potential feedbacks that might supply additional carbon? Solution ofthe above questions is critical if we are to precisely compare the scale of the hyperthermals to the modernpredicament.

5) How did feedback processes restore ocean carbonate chemistry and atmospheric CO2?Although the focus of past research has been on the onset and magnitude of the CIE, it is equally

important to understand the time scale and mechanisms of recovery of the biosphere to massive carbonaddition if we are to gauge the long-term implications of fossil fuel burning. Are there feedbacks thataccelerate or damp this response?

Model sensitivity tests are required to simulate the time scale of C-cycle recovery from rapid injectionsof CO2. One component of this recovery is weathering of carbonate (short-term) and silicate (long-term)rocks on land. Using a suite of numerical models, we will investigate the sensitivity of CO2 consumptionrates during weathering to temperature, freshwater fluxes, and soil development. Another important factoris the extent to which marine productivity and organic carbon burial are promoted or inhibited by changesin riverine nutrient delivery, climate, and ocean circulation associated with the hyperthermals. If the 3HeET

age model is correct, an organic carbon burial event rivaling the carbon release itself must have occurred.What drove this response of the marine biota to the PETM and did a similar response occur during ELMO?

RESEARCH STRATEGYResearch Team

We have assembled an interdisciplinary research team with extensive experience in the core areas ofthis project. The project team is organized into two groups; a theoretical group (L. Kump (group leader),

0628719

C-7

Figure 3. Site 1209 on the Shatsky rise. The 3He data suggest nearlya 20-fold change in sedimentation rate through the PETM.

co-PIs G. Bowen, A. Winguth, and R. Zeebe, and international collaborators, A. Ridgwell and D. Beerling),and an observational group (J. Zachos (group leader), T. Bralower, K. Farley C. Kelly, M. Pagani, and H.Stoll, and international collaborators U. Röhl, H. Brinkhuis, S. Gibbs, T. Tyrrell, I. Raffi, S. Galeotti, & P.Ziveri). We will continue to collaborate with investigators of the 2001 biocomplexity project (J. Dickens, P.Koch, E. Thomas, L. Sloan, P. Delaney, S. Schellenberg, C. Hollis, J. Kiehl), as well as several participantsof ODP Legs 198, 207, and 208 (K. Kaiho, R. Norris, D. Kroon, L. Lourens, M. Petrizzo, M. Nicolo. S.Monechi).

Observational Database: Field and Lab Work

Sampling NetworkTo constrain and test the model experiments, it will be necessary to improve the temporal resolution

and spatial coverage of reconstructions of ocean carbon chemistry and flux changes during thehyperthermals. This includes reconstruction of δ13CDIC, biogenic carbonate production, fluxes, dissolutionand burial. To this end, we will construct high-resolution records for each site in then N. Pacific and S.Atlantic ODP depth transects (Legs 198, 207, and 208), plus a dozen or more pelagic and hemipelagic sitesso that each major ocean sector, the North Atlantic (e.g. Sites 401, 549, 929), Tethys (e.g. Piave, Italy,Zumaya, Spain), central Pacific (Sites 1220, 1221), Southern Ocean (Sites 690,738, Dee & Mead Stream),and Indian Ocean (e.g., Sites 213, 762), is well represented for both events at multiple depths. Based onour preliminary survey, it appears ELMO is present at many of the same sites where the PETM has beendocumented (e.g.; Charisi & Schmitz, 1998; Speijer & Schmitz, 1998; Galeotti et al., 2000; Zachos et al.,2003; Crouch et al., 2001; Schmitz et al., 2001; Hancock et al., 2002; Egger et al., 2002; Cramer et al.,2003; Zachos, Kroon, Blum et al., 2003; Hancock et al., 2003; Crouch et al., 2003; McCarren et al., 2005;in prep., Hollis et al., 2005; Lourens et al., 2005; Nicolo et al., 2005; Nunes & Norris, 2006; Gusberti et al.,submitted; Westerhold et al, 2005; in prep., Galeotti et al., in press; Kaiho et al., in press), so spatialcoverage should be as good, if not better.

Astronomical / Extraterrestrial 3He Age ControlHighly precise time scales are fundamental to both the observational and modeling component of this

project. New sections combined with recent improvements in techniques offer great potential to resolvechronology for PETM and ELMO sections.Thus, substantial effort will go into refiningage models and computing the carbonateaccumulation rates between and across thetwo hyperthermals. With the exception of theclay layers, orbital stratigraphy coupled withchemostratigraphy will be used to establishbaseline accumulation rates prior to and afterthe events. Ba concentration data, obtainedfrom XRF scanning, offer the potential toresolve cycles where other elemental data arenon-cyclic. The Leg 208 orbitally tuned time-series, which is being developed using a combination of thehigh-resolution (~1-3 cm) core logging, XRF core scanner and isotope data from all 5 sites, spans the entireinterval from C24N to C25N and includes both the PETM and ELMO (Fig. 2), and will thus serve as theprimary section to which all others are correlated above and below the clay layers.

In the clay or condensed layers, we propose to expand on earlier work to establish the pace of thePETM and ELMO using extraterrestrial 3He as a constant flux proxy. 3He in most deep-sea sediments isoverwhelmingly derived from ~10 nm diameter interplanetary dust particles (IDPs). Because terrestrial andextraterrestrial helium have very different 3He/4He ratios, isotopic measurements can be used to establishthe concentration of extraterrestrial 3He (3HeET) in a sample. For a given 3HeET flux (F, in atoms/area/time),3HeET is related to the sediment mass accumulation rate (α) by dilution: 3He=F/α. This relationship can be

0628719

C-8

Figure 4. The %CaCO3 and %CF (>63 µm/g) fraction ofthe Leg 208 Sites. IV represents the base of the white,coccolith chalk layer within which both measures areidentical at all sites, regardless of depth (unpublished).

inverted to calculate mass accumulation rates from 3HeET measurements, provided F can be determined, forexample by measuring the amount of 3HeET accumulated over an orbitally-tuned time interval. Temporalvariability of the apparent 3He flux to Earth over intervals comparable to the PETM is fairly small.Uncertainties in the apparent flux can be reduced by calibration using a sedimentary section located closein space and time to the section of interest. Similarly, comparisons among multiple sites provide anempirical test of the resulting age models, because sedimentary phenomena affecting the apparent flux areunlikely to be identical in timing and magnitude at geographically separated localities. The 3He methodprovides instantaneous sedimentation mass accumulation rate estimates for every analyzed sample, whichcan be converted into linear sedimentation rates, and by integration, used to establish an age model. Thismethod successfully resolved fine scale changes in accumulation rate at ODP Sites 690 and 1051 (Farleyand Eltgroth, 2003). The method will be applied to each site in the depth transects, plus a half-dozen sitesin the North Atlantic and Indian Ocean. Preliminary data for Site 1209 from the Leg 198 transect shows a20-fold increase in concentrations (similar to clay) suggesting a substantial loss of carbonate (Fig. 3).

Global Carbon Isotope ExcursionsDetailed, carbonate based carbon isotope records exist for almost every PETM boundary section

studied to date. This includes bulk, planktonic and benthic records. In the Leg 198/208 depth transects theserecords are currently being extended upward to include ELMO (Fig. 2). We will generate similar recordsfor ELMO at a half-dozen additional sites where the PETM is present. The resolution will be on the orderof 1-2 ky for the bulk carbon isotope records, and at lower resolution for planktonic and benthicforaminifera (2-4 ky). Since there are discrepancies between coccolith-dominated bulk and planktonicforaminiferal stable isotope records from some sites during the PETM, we will also generate stable isotoperecords in restricted size fractions dominated by single coccolith genera, eliminating artifacts of changingspecies assemblages and in conjunction with cellular models elucidating the contribution of vital effects instable isotope records (e.g., Stoll, 2005). Coccolith fraction stable isotope records will be produced incombination with trace element records from coccoliths which verify the primary rather than diageneticnature of the coccolith calcite and reveal unique geochemical signatures in certain species during isotopeplateaus which cannot be artifacts of mixing of pre-PETM and PETM material.

Understanding the full extent of the negative CIE during the PETM (and ELMO) is critical to modelingexperiments (see above). Theoretically, a relatively larger terrestrial PETM CIE, measured from δ13Cvalues of terrestrial leaf wax n-alkanes in the Arctic region, could be potentially explained by a floral shiftfrom gymnosperms to angiosperms. However, similar floral shifts must have synchronously occurred atother localities to account for terrestrial 13C-excursions, derived from soil carbonates, of the samemagnitude. Rather than explaining a similarobservation by different processes, it is possible thatthe CIE expressed by higher plant n-alkanes reflectsthe fu l l δ 13C change of atmospheric CO2 inequilibrium with the surface ocean during the PETM.This scenario implies that foraminiferal and coccolithδ13C values do not accurately represent the full CIEof ocean DIC due to effects related to dissolution andchanges in pH. If this hypothesis is validated by theextensive compound-specific isotope analysisproposed in this study, evidence for a ~ –5 to -6‰CIE would require a substantial increase in the massof carbon released. To test this, we intend to measurethe carbon isotope ratios of n-alkanes extracted fromthe near-shore PETM boundary sections. High-resolution planktonic foraminifer carbon isotope

0628719

C-9

records already exist for two shallow marine sections from the New Jersey margin (Zachos et al., in press),and two from outer shelf, upper slope sections from the California margin (John et al., 2005). TheCalifornia sections are currently being processed and preliminary results indicate abundant terrestriallyderived n-alkanes are present. We will also sample hemipelagic sections along the Tethyan margin (e.g.,Piave, Italy; Giusberti et al., submitted), and in New Zealand (Mead and Dee Stream; Nicolo et al., 2005),and several pelagic cores), to isolate n-alkanes. Moreover, similar coupled n-alkane δ13C and carbonateδ13C records for ELMO when carbon flux was smaller and marine carbonate dissolution less severe, shouldprovide additional insight into the nature of the offset.

Biogenic Carbonate Accumulation High-resolution %CaCO3 records already exist for most of the pelagic and hemipelagic PETM sections

in our global sampling network. Moreover, all the depth transect cores have also been scanned by XRF, andthus have high-resolution Ca concentration records (U. Röhl, pers. comm.), which can be easilytransformed through regression to %CaCO3. Thus, most of our analytical effort will focus on older DSDPand ODP cores and land-based outcrops. The archive halves of cores that have not been scanned will beshipped to Bremen University for scanning. For the few cores that are unsuitable for scanning, discretesamples will be collected for conventional coulometric analysis. For most land-based marine PETM andsome ELMO sections, CaCO3 records already exist, so the number of sections to resample will be minimal.

The relative contribution of foraminifera vs. coccolithophorids to the carbonate flux shifts significantlythrough the PETM (Fig. 4). To ascertain the global extent of this important ecological shift, standardsieving and settling techniques will be used to partition and compute the accumulation of various biogeniccomponents (forams vs. coccoliths). Samples from the depth transects have already been wet sieved at >38µm and dry sieved in larger size fractions (>63, >150 µm). Settling techniques will be used to separatenannofossils (Stoll, 2005; Stoll and Ziveri, 2002).

Dissolution CCD/Lysocline:In sites examined to date, the foraminiferal preservation in the white chalk/ooze layer is excellent, with

little to no fragmentation (Kelly et al., 2005; in prep.). In the Leg 208 depth transect, %CF (& %CaCO3) inthis layer is essentially identical at all depths (Fig. 4), an observation that suggests the entire water columnwas highly oversaturated. To determine the scale of this unusual phenomenon, we will construct proxypreservation records for both the PETM and ELMO in each ocean sector (as above). We will target sitesthat provide the broadest depth coverage possible. Proxies to be measured include the %CF,planktonic/benthic and fragmentation indexes, and microscale carbonate overgrowth. In the Leg 198 and208 sites, we will investigate proxies sensitive to carbonate ion content such as depth-dependent variationsin Zn/Ca in benthic foraminifera and Mg/Ca in planktonic foraminifera (Fehrenbacher and Martin, 2006).

Nannofossil preservation in PETM and ELMO samples will be evaluated by establishing thedissolution susceptibility of key nannofossil and foraminiferal species. This will be performed in threedifferent ways: (1) To establish the solution susceptibility of ancient plankton taxa, samples will be reactedwith seawater that is undersaturated with respect to CaCO3, as done by Hill (1975) with traps. We willconduct similar experiments, but in the laboratory using seawater solutions of controlled pH. (2) We arecompiling a global dataset of PETM nannofossil and foraminiferal assemblage data and will usemultivariate techniques (Detrended Correspondence Analysis (DCA)) to determine ecological groupings oftaxa (Gibbs, Bralower, et al., in prep.). This same data set can be mined to determine the relative amount ofdissolution of individual samples as well as the solution susceptibility of different taxa. And (3) We willquantify % etched or overgrown taxa for nannofossil and foraminiferal specimens and use quantitativemetrics to determine the extent of alteration using a scanning electron microscope.

For planktonics, shell diameter/mass of specimens is also a useful gauge of their preservation (Bijma etal., 2002; Broecker, 2002). Average mass (and wall thickness) of globally distributed mixed-layerplanktonic species Acarinina soldadoesnsis, and thermocline dweller Subbotina patagonica will bemeasured. In addition, we will measure the weight of Morozovella velascoensis and the “excursion taxa” of

0628719

C-10

Morozovella (M. allisonensis) and Acarinina (A. sibaiyensis) that are restricted to tropical and temperatelocations e.g., (Kelly et al., 1998). Preliminary work shows a substantial increase in the mean mass offoraminiferal shells in the white, chalk layer. The fragmentation of foraminiferal assemblages will also bedetermined (e.g., (Kelly, 2002); Colosimo et al., 2005).

Once the relative solution susceptibility of calcareous nannofossil taxa is known, we will calibrateassemblage data with grain size analysis of the <38µm fraction. Grain size analysis offers an advantage fordetermining assemblage and preservational changes because it is fast and relatively inexpensive andprovide us with the means to observe changes at unusually high resolution (mm to cm) with a minimum ofeffort. We are currently using a Malvern Mastersizer and Coulter Counter particle analyzer for this purpose.

Productivity of coccolithophore carbonate producersTo ascertain the extent to which changes in productivity of coccolithophorid algae contributed to shifts

in the carbon cycle and carbonate accumulation during the PETM and ELMO, we will use trace elementratios in coccoliths representative of primary trace-metal incorporation during calcification. The ratio ofSr/Ca in particular has been shown to vary with nutrient-stimulated growth rates in culture (Rickaby et al.,2002; Stoll et al., in review-a), sediment trap, and surface sediment transects (Stoll and Ziveri, 2004).Where dissolution is minor, coccolith Sr/Ca ratios covary with other indicators of coccolithophoridproduction including alkenone and carbonate accumulation rates (Rickaby et al., in review). Thisrelationship likely arises due to variable polysaccharide extrusion in response to nutrient availability, whichbinds Sr preferentially to Ca and affects the near cell ratio of Sr/Ca available for uptake into the coccolithcalcification vesicle (Langer et al., 2006).

Coccolith Sr/Ca and other elemental ratios can be measured using separated near-monogeneric sizefractions (e.g., Stoll and Bains, 2003), as well as a new ion probe analysis of individually pickedpopulations of monogeneric coccoliths (Stoll et al., in review-b). This latter technique is especiallyadvantageous for studying lower Eocene sections where coccoliths are not abundant due to dissolution,when monogeneric coccolith fractions cannot be satisfactorily separated from sediments, and in shelfsections where high lithogenic input may hamper ICP analysis of coccolith size fractions. The ion probetechnique also provides a clearer picture of how ecologically distinct coccolith genera responded to theevents. The ion probe technique reproduced to within 1% the Sr/Ca ratios of monospecific culturedHelicosphaera carteri samples which had also been measured by inductively coupled plasma atomicemission spectroscopy. Analyses of replicate populations of Toweius coccoliths, from the same samplepicked and analyzed several months apart, yield Sr/Ca ratios which differ by 1%.

Figure 5. Models and model co-ordination used to study the carbon cycle duringthe early Paleogene hyperthermal events. A) Three modeling approaches will beused, each involving specific opportunities and compromises in terms of the timescales and scope of processes that can be modeled. B) Modeling experiments (grayarrows) will be coordinated to assess each motivating question. Earth systemmodels (GENIE and CCSM) will provide boundary conditions for the process-oriented models. Process model simulations will be designed to investigateproblems identified during data/model validation of the Earth system models andto develop hypotheses to be tested with model simulations

Numerical ModelingOur modeling efforts to date have begun to constrain the

magnitude and duration of carbon release required to generate theobserved PETM isotopic and sedimentary response (see below), but

a number of outstanding questions remain and new issues of CIE magnitude, duration, and truncation havearisen (described above) that we must address. Thus, we propose simulations with well-tested communitymodels of various degrees of complexity to predict the oceanic and sedimentary response to a range ofcarbon addition scenarios (including the first quantitative analysis of the ELMO event). In addition we willassess which of the scenarios (e.g., clathrate or thermogenic methane vs. fossil carbon – CO2 input, fast vs.

0628719

C-11

slow input) generate the proper isotopic, climatic, and CCD responses (both regional and global) for theonset, magnitude, and recovery from these events. Transient simulations will be carried out with theintermediate complexity Earth system model GENIE. This modeling will be supported by higher-resolutiontime-slice simulations using the comprehensive climate model CCSM-3. CCSM-3 will provide improvedsimulations of ocean biogeochemistry for the initiation and termination of the PETM and ELMO events,and necessary boundary conditions to GENIE. In this work we benefit greatly from the international teamof experts whose primary task is model validation for modern-day and future prediction. In addition, boxmodels of carbon cycle processes will be used to conduct long (multimillion-year) simulations, andprocess-specific models will be used to address particular components of the global response. Thesemodeling efforts will be coordinated: GENIE and CCSM-3 will provide climate and ocean transport ratesto the box models, and the process-oriented and box models will guide improvements to theparameterizations of the GCMs (Fig. 5).

All spatially resolved models will use late Paleocene - early Eocene paleogeography and physiographyderived from GIS layers assembled by C. R. Scotese (www.scotese.com) and the techniques of Markwickand Valdes (2004). To assess the sensitivity to these boundary conditions, the paleogeography andpaleobathymetry produced by the Paleogeographic Atlas Project of the University of Chicago (presentlyused in GENIE modeling as well as in the work of Bice and Marotzke, 2001, 2002) will also be employed.

Process-oriented models

Long-term simulations of the carbon cycle spanning the PETM and ELMO will be conducted withglobal atmosphere-ocean-sediment carbon cycle models, building upon the initial results for the PETM ofDickens (1997). The ocean component resolves the different ocean basins, high and low-latitudes, andsurface/intermediate/deep waters (Walker and Kasting, 1992; Dickens, 1997; Sigman et al., 1998; Zeebeand Archer, 2005); water fluxes are derived from the Earth system models. Coupling to sediment models(Keir, 1982; Sundquist, 1986; Sigman et al., 1998) and inclusion of carbonate and silicate weatheringfeedbacks will allow quantitative analyses of carbon fluxes on time scales from thousands to millions ofyears. Model tracers include nutrients such as PO4, stable carbon isotopes (δ13C), and total CO2 and totalalkalinity from which atmospheric CO2 is calculated. These simulations will provide the baseline reservoirproperties for initiating GENIE and CCSM-3 simulations.

A depth-explicit soil organic carbon and CO2 model including stable isotopes (Bowen and Beerling,2004) will be used to explore soil carbon processes and carbon isotope ratios to be compared to paleosolrecords, at vertical resolutions that cannot be achieved with the coupled Earth Systems models. Steady-state and dynamic vertical soil organic carbon decay and soil gas CO2 profiles can be simulated fromderived soil physical property and organic carbon input and decay parameters. Additional constraints forthe model simulations will be given by n-alkane carbon isotope data made available by this project.Updates to the model will include development of schemes for interfacing the soils model with GENIE andCCSM-3 for grid-level simulation of PETM and ELMO soils.

.Earth system model of intermediate complexity: The GENIE model

Intermediate complexity models present an unprecedented opportunity to perform time continuoussimulations of geologic events like the PETM and ELMO (or both simultaneously); previous modeling hasbeen largely restricted to snapshots using GCMs or 0-D box model simulations. GENIE(www.genie.ac.uk) consists of interconnected modules treating atmosphere, ocean, sediments, ice sheets,land surface and vegetation, soils, sea ice, and ocean biogeochemistry. The model uses a highly efficientfrictional geostrophic 3-D representation of the ocean, a 2-D energy and moisture balance atmosphere (afterWeaver et al., 2001; coarse-resolution 3-D treatments are possible), and a dynamic and thermodynamic sea-ice model (Annan et al., 2005; Edwards and Marsh, 2005). A sediment component of GENIE is currentlyunder construction by A. Ridgwell (see letter of support) and based in part on the work of Archer et al.(2002). This component calculates sediment accumulation rates (carbonate, non-carbonate, and organiccarbon), sediment compositions (e.g., %CaCO3 and %Corg), and isotopic compositions. As such, it allows

0628719

C-12

Figure 6 Model generated carbonate content along a “Walvis Ridge”transect after addition of 2000-6000 Gt C to the ocean. Panel on right isfrom Zachos et al. (2005). (courtesy Andy Ridgwell).

2000 Gt C 4000 Gt C 6000 Gt C

for an assessment of the extent to which the magnitude of the marine CIE has been truncated by erosion, ashypothesized above based on the higher-plant alkane δ13C record. Kump and his graduate student, KarlaPanchuk, together with Ridgwell, have been modifying GENIE for application to the PETM event. Thefirst simulations of the PETM event are encouraging (Fig. 6). We are able to reproduce the Walvis Ridgecarbonate record with a 6000 Pg C addition over 15ky, including the more rapid recovery of carbonatesedimentation at shallower depths. We propose here to evaluate the degree of the model-simulated oceanacidification required to match reconstructed CCD shifts in both Atlantic and Pacific sectors. Constrainedby new estimates of carbonate accumulation rates and δ13C chronologies, the modeling will permitassessment of magnitude, rate, and origin of the carbon release. Also, with δ13C tracers, we can simulatebottom water gradients as captured in benthic foraminifera (Nunes & Norris, 2006), while including theeffects of dissolution on sedimentary profiles.

Presently GENIE does notallow weathering responses toclimate change, a critical partof the response to large carbonadditions. Increased fluxes ofkaolinite from the continentsduring the PETM (Gibson etal., 2000; Robert and Kennett,1994), together with an Osisotope excursion (Ravizza etal., 2001) have been argued toreflect intensified silicateweathering, and thus may signalincreased consumption of CO2

through chemical weathering(cf. Thiry, 2000). Thus we need to develop a weathering module for GENIE. The model will use a set ofpredictive functions to estimate clay mineral abundances in soils based on climate, vegetation type, bedrockmineralogy, and physiography, derived through multiple regression analysis of digital spatial data sets formodern soils (FAO, 2003) in the context of global climatological datasets (New et al., 2000), biomedistributions (http://edcsns17.cr.usgs.gov/glcc/ globe_int.html), and physiography (USGS, 1996) inunglaciated, non-agricultural regions. Early Paleogene soil mineralogy will be predicted using these samevariables, which are explicitly specified or calculated in GENIE. A paleogeologic map for the Eocene(following Bluth and Kump, 1991) will be constructed as a senior-thesis project in the first year of funding.Weathering rates will be determined using empirical rate laws derived from the data on river loads frommodern-day, monolithologic watersheds (e.g., Bluth and Kump, 1994; Gibbs et al., 1999). The effect ofrelief and soil cover will be parameterized by analogy with modern drainages (e.g., Milliman and Syvitski,1992; Summerfield and Hulton, 1994; Hooke, 2000). Validation will include comparison of chemicalerosion rates calculated for the major rivers of the world compared to observation for the modern; fairagreement has been achieved in the past (Gibbs and Kump, 1994; Ludwig et al., 1999).

Moreover, the organic carbon weathering and deposition components of GENIE have not beenimplemented. As described above, the organic carbon cycle seems to be an important part of the recoveryfrom the PETM, one that has been neglected to date. We will work with Ridgwell to activate this part of themodel.

As described above, one explanation for the smaller amplitude CIE in the marine vs. terrestrial recordsis the dependence of the δ13C of marine carbonate on carbonate ion concentration. To evaluate thishypothesis, the carbonate ion effect will be incorporated into the carbon cycle models and the resultscompared with those generated without the effect.

0628719

C-13

Presently, GENIE does not resolve continental shelves and thus cannot fully represent the response tothe PETM/ELMO perturbations. We will evaluate the sensitivity of CCD response to this partitioning byattaching low-, mid-, and high-latitude shelf “boxes” to the box model and to GENIE, with specifiedpartitioning based on paleogeographic reconstructions of latitudinally dependent flooded shelf areas for theearly Paleogene and estimated rates of carbonate deposition based on adjacent open-ocean waterchemistries (after Opdyke and Wilkinson, 1993) from GENIE.

Time-slice experiments for onset and recovery of the PETM and ELMO with the Community ClimateSystem Model (CCSM)

The CCSM-3 (see letter of collaboration) is a coupled climate model for simulating Earth’s climatesystem (http://www.ccsm.ucar.edu/models/ccsm3.0/). Time-slice simulations with the CCSM3 for the onsetand recovery of the CIE near the PETM and ELMO will be guided by previous simulations with olderversions of the CCSM (e.g. (Huber et al., 2002; Huber and Caballero, 2003; Huber and Sloan, 2001;Shellito et al., 2003)) and coordinated with CCSM Paleoclimate Working Group. We are planning to carryour simulations of various greenhouse gas levels (i.e. 1xCO2, 2xCO2, and 8xCO2) to explore interactionsof the climate and the carbon cycle, in particular how the carbon cycle responds to changes in the climatestate. The output of these simulations will be used for model-data validation and input for the offline three-dimensional carbon cycle modeling studies as well as for the process-oriented models and GENIE (surfacewind velocities and shear stresses). Moreover, the role of geography will be investigated by comparisonwith a modern reference simulation.

Output from CCSM-3 will be used as input for offline carbon cycle models in order to investigateeffects of different ocean circulation patterns on water column processes, fluxes at the sediment/waterinterface, and sedimentary composition. The offline carbon cycle model has been developed at theUniversity of Chicago and includes the prediction of water mass tracers based on the HAMOCC model(Maier-Reimer, 1993; Archer and Maier-Reimer, 1994; Archer et al., 2000) with prognostic macro- andmicronutrients (P, Si, Fe), oxygen, carbon tracers (δ13C), and a model ("Muds”) for oxic and anoxicdiagenesis of shallow and deep-sea sediments based on an efficient solver for steady-state pore water andsolid phase diffusion/reaction/advection equations (Archer et al., 2002). The sediment model used in theproposed project is similar to the one in GENIE and will be updated in collaboration with D. Archer. Thedependence of carbon export rates on micronutrients (Fe) and mineral ballast (Armstrong et al., 2002) havebeen tested with the HAMOCC model and compared with carbon tracers and sediment traps (Howard et al.,in press). We will improve a simplified sulfur cycle currently developed at the MPI Hamburg (E. Maier-Reimer) by adopting the code developed for GENIE. The off-line coupling of the carbon cycle model withPOP_TM is under development and tested with ideal age tracers in collaboration with the NCAROceanography Section (OS) (S. Yeager, W. Large) and Climate Change Research Section (CCR) (J. Kiehl).

We will carry out experiments with both GENIE and CCSM-3 to study the sensitivity of the latePaleocene/early Eocene thermohaline circulation and carbon cycle to changes in the hydrological cycle,following the work of Bice and Marotzke (2001) that demonstrated a high degree of sensitivity of the oceancirculation to the amounts and location of freshwater discharge to the ocean. Possible switches in thethermohaline circulation related to changes in atmospheric moisture transport could lead to sufficientwarming to destabilize seafloor gas hydrates over most of the world ocean to a water depth of at least 1900m. We will determine changes in clathrate stability following the lead of Bice and Marotzke (2002) andcalculate methane fluxes accordingly, but explicitly determining the delay in response resulting from therequirement for the warming to penetrate through the sedimentary pore waters to the clathrates.Furthermore, we will perform simulations similar to those of Heinze (2004) to address how significantecological changes at the PETM (see Kelly, 2002, and Kelly et al., 2005, and references therein) likelyaltered POC fluxes into the abyssal layers and thus influenced the CCD. Sensitivity of the CCD to mineralballasting of POC (Armstrong et al., 2002; Klaas and Archer, 2002; Howard et al., in press) will be alsoexplored. Finally, we will continue our research on the effect that bioturbation on the capacity of seafloordissolution to damp the lysocline response to CO2 (Ridgwell et al., 2005).

0628719

C-14

SIGNIFICANCEThe ocean is the largest sink for anthropogenic CO2 and has absorbed nearly 130 PgC of the 380 PgC

emitted to the atmosphere since the onset of the industrial revolution (Sabine et al., 2004; Feeley et al.,2004). If emissions continue to rise unabated for the next three centuries, an additional 4000 PgC or morewill be added to the atmosphere and ocean. Because the emission rate is relatively short compared to themixing time of the ocean, most of anthropogenic carbon will accumulate in surface waters, therebylowering the seawater pH and [CO3] concentration to levels that might impact the ability of corals andcoccolithophorids to calcify (Riebesell et al., 2000; Caldeira & Wickett, 2003; Orr et al., 2005), while alsoslowing the rate of uptake by the ocean. Only vertical mixing and dissolution of seafloor carbonate willbuffer these changes. Because pCO2 will rapidly rise to levels not seen on Earth in over 40 million years(Pagani et al., 2005), there is some uncertainty as to how fast the ocean will sequester this carbon. Forexample, as the climate rapidly warms, and the ocean pH decreases, it is not entirely clear that rates ofsequestration will follow modeled scenarios. Worse yet, there is still insufficient understanding of howpotential positive feedbacks may work to amplify the rise in CO2.

Approximately 55 million years ago, the Earth experienced a similar episode of rapid and extremetransient warming, the Paleocene-Eocene Thermal Maximum that was also the product of massive carbonrelease. Intense study of this event over the last five years has lead to several major findings regarding theconsequences of this event on climate, biota, and biogeochemical cycles. One of the more prominentadvances is the documentation of evidence for widespread ocean acidification and buffering, consistentwith carbon cycle theory. A related advance was the discovery of second ocean acidification event at ~53million years ago. This warming event, referred to as ELMO, was less extreme in every sense, from theperturbation in the carbon cycle to the magnitude of warming. These hyperthermals provide a uniqueopportunity to gain insight into the long-term impacts of rapidly rising CO2 levels on climate, oceancarbonate chemistry, and biota. They also provide an opportunity to identify potential non-linear feedbacks,and test model sensitivity.

MANAGEMENT PLANOur management structure follows a model used in a previous NSF-Biocomplexity project

(http://es.ucsc.edu/~silab/biocomplex/index.htm). To start we will hold two workshops. The first workshopwill be convened within 6 months of the project start date to review the long and short-term goals andobjectives, develop experimental design, coordinate integration of data with models, and then organize firstand second year work plans. The second workshop ~ 20-24 months later will be designed to assessprogress, identify additional observational needs and model experiments, and to organize publications.

The leaders of the two groups, theoretical and data (L. Kump & J. Zachos), will be responsible fororganizing the activities of each team and disseminating information within and between groups. As forspecific contributions, Kump will head the theoretical group coordinating the myriad of model experiments,and responsible for directing the GENIE collaboration between his graduate student, Andrew Ridgwell atUBC, and the UK GENIE group. Winguth and a graduate student will be responsible for the sensitivityexperiments with CCSM-3 and the off-line carbon cycle model. Zeebe and his graduate student willdevelop/run simplified atmosphere-ocean-sediment carbon cycle models, provide comparison to futurescenarios, and collaborate on laboratory dissolution experiments with PSU. Bowen and his group willdevelop and apply process-oriented models to study carbon cycle feedbacks involving the coupling ofterrestrial and marine systems through soil and weathering processes. The observational group will beheaded by Zachos who along with a graduate student will coordinate field sampling and be responsible forthe stable isotope studies, and the integration of cycle stratigraphy with chemostratigraphy. Kelly and agraduate student will be responsible for quantifying foraminiferal assemblages and preservation indexes,and collecting specimens for isotope analyses. Farley and a graduate student will be responsible fordeveloping 3He age models and will collaborate with Bralower, Zachos, and Röhl in mass accumulationrate estimates. Pagani and graduate student will undertake the isotope analyses of n-alkanes. Bralower andStoll and their students will coordinate research activities focused on coccolithophore preservation andproductivity using a variety of microscopic and geochemical methods.

0628719

C-15

BROADER IMPACTSThe proposed research has significant potential to educate the next generation of earth scientists,

general education college and K-12 students about the fate of anthropogenic CO2, a topic of significantsocietal concern. In addition, the research will contribute to the training and education of 6 undergraduateand 9 graduate students at all of the PI institutions combined. We propose to take advantage of therelevance of the proposed research to generate several additional educational activities:ß PIs Bralower, Kump, Stoll and Zachos will lead a workshop for educators on curriculum design

involving abrupt ancient global warming. The workshop will include modules and exercises that will bedeveloped jointly by these PIs and their undergraduates and graduate students engaged in the proposedresearch and include data-rich, inquiry-based laboratory/discussion sections aimed at general educationand upper division elective courses. The three-day course at PSU will follow the model of On theCutting Edge workshops and we will work with leaders of that highly successful program to design aneffective program (see attached letter from Heather Macdonald). The Science Education ResourceCenter (SERC) will help advertise the workshop. Media and modules developed will be made availableto faculty at other institutions by inclusion on the SERC web site.

ß Summer undergraduate interns and all graduate students will be expected to develop and give apresentation on the climate system to a high school science class.

ß Penn State University has recently formed a partnership with Fort Valley State University (FVSU) inGeorgia and developed a 3+2 dual degree program (see attached letter). The first FVSU students will bearriving at PSU in Fall 2006. The proposed program will include two FVSU student interns as part ofthe well-established PSU Summer Research Opportunity Program for minority science majors. Bralowerand Kump have been active in a range of summer programs including the Summer Experience in Earthand Mineral Sciences for high school minority students interested in science. Stoll will continue to beinvolved in the Williams College Summer Science Program that promotes the participation of under-represented groups in research. She has hosted four students from this program in her lab since 2001.

ß The University of Wisconsin and Penn State, together with other Worldwide Universities Networkpartners, are developing an international summer workshop for graduate students and early careerscientists (Summer Institute for Earth Systems / Transatlantic or SIES/TA). The first SIES/TA isscheduled for Summer, 2007 and will be focused on Arctic climate change (modern and ancient). Wepropose that the Summer, 2009 workshop be focused on Deep-Time Carbon Cycling: Modeling andData Analysis, to be taught by the PIs, postdocs, and students supported by this proposal.

ß UCSC has several proven programs in place that will benefit from, and contribute to, the broaderimpacts for education that are articulated in this proposal. First, UCSC is a participant in the NSFAGEP Program UCSC is building cohorts of graduate students in the fields of science, technology,engineering and math (STEM) with the goals of mentoring these students towards successfulprofessorial positions. UCSC-AGEP would welcome the participation of UCSC graduate students in thisproposal to the AGEP cohort. Second, UCSC is proud to be a participant in the UCLEADS program,which encourages and mentors under-represented minority junior and senior undergraduate students inthe STEM fields to go to graduate school in the UC system. Zachos will mentor several UCLEADSstudents on this project (see attached letter).

ß Our website will be a vehicle to share knowledge and progress in our investigation of carbon cycledynamics. This website will include updates about research activities, publications, presentations, andopportunities for new student involvement, as well as links to appropriate resources, education modules,and FAQs. In addition, Zachos and Winguth will propose a topical session for the 2007 AAAS meetingin San Francisco on the “The Early Eocene Hyperthermals: Lessons for the Future”.

Through group collaboration and activities including workshops, participating undergraduate and graduatestudents will experience involvement in a multidisciplinary, international research project. For example, thebi- annual workshop described will bring all project participants together and provide students withexcellent opportunities to interact with an international group of scientists who can be mentors and rolemodels.

0628719

D-1

Citation List Annan, J.D., Hargreaves, J.C., Edwards, N.R. and Marsh, R., 2005. Parameter estimation in an

intermediate complexity earth system model using an ensemble Kalman filter. Ocean Modelling 8: 135-154.

Archer, D., A. Winguth, D. Lea, and N. Mahowald, 2000. What causes the glacial/interglacial pCO2 cycles?, Reviews of Geophysics, 38, 159-189.

Archer, D., and Maier-Reimer, E., 1994, Effect of Deep-Sea Sedimentary Calcite Preservation On Atmospheric Co2 Concentration: Nature, v. 367, p. 260-263.

Archer, D., H. Kheshgi and E. Maier-Reimer. Dynamics of fossil fuel CO2 neutralization by marine CaCO3. Global Biogeochem. Cycles, 12:259–276, 1998.

Archer, D., Kheshgi, H., and Maier-Reimer, E., 1997, Multiple timescale for neutralization of fossil fuel CO2: Geophysical Research Letters, v. 24, p. 205-408.

Archer, D.E., Morford, J.L., and Emerson, S.R., 2002. A model of suboxic sedimentary diagenesis suitable for automatic tuning and dridded global domains. Global Biogeochemical Cycles 16:

Armstrong, R.A., C. Lee, J.I. Hedges, S. Honjo, and S.G. Wakeham, 2002. A new, mechanistic model for organic carbon fluxes in the ocean: based on the quantitative association of POC with ballast minerals, Deep-Sea Res. II, 49, 219-236.

Ben-Yaakov, S. and M .B. Goldhaber, 1973. The influence of sea water composition on the apparent constants of the carbonate system. Deep-Sea Res., 20, 87-99.

Bice, K. L., and J. Marotzke, 2001. Numerical evidence against reversed thermohaline circulation in the warm Paleocene/Eocene ocean, J. Geophys. Res., 106, 11,529– 11,542, 2001.

Bice, K.L., and Marotzke, J., 2002. Could changing ocean circulation have destabilized methane hydrate at the Paleocene/Eocene boundary. Paleoceanography 17 10.1029/2001PA000678.

Bijma, J., Honisch, B., and Zeebe, R.E., 2002, Impact of the ocean carbonate chemistry on living foraminiferal shell weight: Comment on "Carbonate ion concentration in glacial-age deep waters of the Caribbean Sea" by W. S. Broecker and E. Clark - art. no. 1064: Geochemistry Geophysics Geosystems, v. 3, p. 1064.

Bluth, G.J.S. and Kump, L.R., 1991. Phanerozoic paleogeology. Amer. J. Sci. 291: 284-308. Bluth, G.J.S. and Kump, L.R., 1994. Lithologic and climatologic controls of river chemistry.

Geochimica et Cosmochimica Acta, 58:2341-2359. Bowen, G.J. and Beerling, D.J., 2004. An integrated model for soil organic carbon and CO2: implications

for paleosol carbonate pCO2 paleobarometry. Global Biogeochemical Cycles, 18, GB1026, doi:10.1029/2003GB002117.

Bowen, G.J., Beerling, D.J., Koch, P.L., Zachos, J.C., and Quattlebaum, T., 2004, A humid climate state during the Palaeocene/Eocene thermal maximum: Nature, v. 432, p. 495-499.

Bowen, G.J., Bralower, T.J., Delaney, M.L., Dickens, G.R., Kelly, D.C., Koch, P.L., Kump, L.R., Meng, J., Sloan, L.C., Thomas, E., Wing, S.L., and Zachos, J.C., in press, The Paleocene-Eocene thermal maximum gives insight into greenhouse gas-induced environmental and biotic change: EOS.

Bralower, T.J., 2002, Evidence of surface water oligotrophy during the Paleocene-Eocene thermal maximum: Nannofossil assemblage data from Ocean Drilling Program Site 690, Maud Rise, Weddell Sea (vol 17, pg 1023, 2002) - art. no. 1060: Paleoceanography, v. 17, p. 1060.

Bralower, T.J., Premoli-Silva, I., Malone, M., and al., e., 2002, Proc. ODP, Initial Reports: College Station, TX, Ocean Drilling Program, v. 198.

Bralower, T.J., Thomas, D.J., Zachos, J.C., Hirschmann, M.M., Rohl, U., Sigurdsson, H., Thomas, E., and Whitney, D.L., 1997, High-resolution records of the late Paleocene thermal maximum and circum-Caribbean volcanism: Is there a causal link?: Geology, v. 25, p. 963-966.

Bralower, T.J., Zachos, J.C., Thomas, E., Parrow, M., Paull, C.K., Kelly, D.C., Silva, I.P., Sliter, W.V., and Lohmann, K.C., 1995, Late Paleocene to Eocene Paleoceanography of the Equatorial Pacific-

0628719

D-2

Ocean - Stable Isotopes Recorded at Ocean Drilling Program Site-865, Allison-Guyot: Paleoceanography, v. 10, p. 841-865.

Broecker, W.S., 2002, Constraints on the glacial operation of the Atlantic Ocean's conveyor circulation: Israel Journal of Chemistry, v. 42, p. 1-14.

Caldeira, K., and Wicket, M.E., 2003, Anthropogenic carbon and ocean pH: nature, v. 425, p. 365. Charisi, S.D., and Schmitz, B., 1998, Paleocene to early Eocene paleoceanography of the Middle East:

The delta C-13 and delta O-18 isotopes from foraminiferal calcite: Paleoceanography, v. 13, p. 106-118.

Colosimo, A.B., Bralower, T.J., and Zachos, J.C., Evidence for lysocline shoaling and methane hydrate dissociation at the Paleocene-Eocene thermal maximum on Shatsky Rise, ODP Leg 198, In Bralower, T. J., Premoli Silva, I., Malone, M., (Eds.), Proc. ODP, Sci. Results, v. 198, 2005.

Cramer, B.S., Aubry, M.P., Miller, K.G., Olsson, R.K., Wright, J.D., and Kent, D.V., 1999, An exceptional chronologic, isotopic, and clay mineralogic record of the latest Paleocene thermal maximum, Bass River, NJ, ODP 174AX: Bulletin De La Societe Geologique De France, v. 170, p. 883-897.

Cramer, B.S., Wright, J.D., Kent, D.V., and Aubry, M.P., 2003, Orbital climate forcing of delta C-13 excursions in the late Paleocene-early Eocene (chrons C24n-C25n): Paleoceanography, v. 18.

Crouch, E.M., Dickens, G.R., Brinkhuis, H., Aubry, M.P., Hollis, C.J., Rogers, K.M., and Visscher, H., 2003, The Apectodinium acme and terrestrial discharge during the Paleocene-Eocene thermal maximum: new palynological, geochemical and calcareous nannoplankton observations at Tawanui, New Zealand: Palaeogeography Palaeoclimatology Palaeoecology, v. 194, p. 387-403.

Crouch, E.M., Heilmann-Clausen, C., Brinkhuis, H., Morgans, H.E.G., Rogers, K.M., Egger, H., and Schmitz, B., 2001, Global dinoflagellate event associated with the late Paleocene thermal maximum: Geology, v. 29, p. 315-318.

Dickens, G.R., Castillo, M.M., and Walker, J.C.G., 1997, A blast of gas in the latest Paleocene: Simulating first-order effects of massive dissociation of oceanic methane hydrate: Geology, v. 25, p. 259-262.

Dickens, G.R., Oneil, J.R., Rea, D.K., and Owen, R.M., 1995, Dissociation of Oceanic Methane Hydrate As a Cause of the Carbon Isotope Excursion At the End of the Paleocene: Paleoceanography, v. 10, p. 965-971.

Dickson J. A. D., 2002. Fossil echinoderms as monitor of the Mg/Ca ratio of phanerozoic oceans. Science 298(5596), 1222-1224.

Edwards, N.R. and Marsh, R., 2005. Uncertainties due to transport-parameter sensitivity in an efficient 3-D ocean-climate model. Climate Dynamics 24: 415-433.

Egger, H., Homayoun, M., and Schnabel, W., 2002, Tectonic and climatic control of Paleogene sedimentation in the Rhenodanubian Flysch basin (Eastern Alps, Austria): Sedimentary Geology, v. 152, p. 247-262.

Erbacher, J., Mosher, D. Malone, M. et al., 2004, Proc. ODP, Initial Reports: College Station, TX, Ocean Drilling Program, v. 207.

Farley, K. A., 2001. Extraterrestrial helium in seafloor sediments: identification, characteristics, and accretion rate over geologic time. Accretion of Extraterrestrial Matter Throughout Earth's History. B. Peucker-Ehrinbrink and B. Schmitz. New York, Kluwer: 179-204.

Farley, K. A., et al. 1997. Atmospheric entry heating and helium retentivity of interplanetary dust particles. Geochimica Et Cosmochimica Acta 61(11): 2309-2316.

Farley, K. A., et al. 2006. A late Miocene dust shower from the break-up of an asteroid in the main belt. Nature 439(7074): 295-297.

Farley, K.A., and Eltgroth, S.F., 2003, An alternative age model for the Paleocene-Eocene thermal maximum using extraterrestrial He-3: Earth and Planetary Science Letters, v. 208, p. 135-148.

Feely, R.A., Sabine, C.L., Lee, K., Berelson, W., Kleypas, J., Fabry, V.J., and Millero, F.J., 2004, Impact of anthropogenic CO2 on the CaCO3 system in the oceans: Science, v. 305, p. 362-366.

0628719

D-3

Fehrenbacher, J.S., and Martin, P., 2006, Foraminiferal Mg/Ca as a proxy for deep water carbonate chemistry, Ocean Sci. Meet., Volume 87 (36): Eos Trans., Supp. Abstract, AGU, p. OS43P-01.

Food and Agriculture Organization of the United Nations (2003), Digital Soil Map of the World and Derived Soil Properties, FAO Land and Water Digital Media Series, Rome.

Galeotti, S., Angori, E., Coccioni, R., Ferrari, G., Galbrun, B., Monechi, S., Premoli-Silva, I., Speijer, R.P., and Turi, B., 2000, Integrated stratigraphy across the Paleocene/Eocene Boundary in the Contessa Road Section, Gubbio (central Italy): Geologic Society of France Bulletin, v. 171, p. 355-365.

Galeotti, S., Kaminski, M.A., Coccioni, R., and Speijer, R.P., in press, High resolution deep water Agglutinated Foraminiferal records across the Paleocene/Eocene transistion in the contessa Road Section (central Italy), in Bubik, M., and Kaminski, M.A., eds., Proceedings of the Sixth International Workshop on Agglutinated Foraminifera, Volume in press: in Press, Grzybowski Foundation Special Publications.

Gibbs, M. T., Bluth, G. J., Fawcett, P. J., and Kump, L.R., 1999. Global chemical erosion over the last 250 MY: Variations due to changes in paleogeography, paleoclimate, and paleogeology. Amer. J. of Sci., v.299, p 611-651.

Gibbs, M.T., Kump, L.R., 1994. Global chemical erosion during the last glacial maximum and the present; sensitivity to changes in lithology and hydrology. Paleoceanography 9, 529-543.

Gibson, T.G., Bybell, L.M. and Mason, D.B., 2000. Stratigraphic and climatic implications of clay mineral changes around the Paleocene/Eocene boundary of the northeastern US margin. Sedimentary Geology, 134(1-2): 65-92.

Giusberti, L., Rio, D., Agnini, C., Backman, J., Fornaciari, E., Tateo, F., and Oddone, M., submitted, An Expanded Marine PETM Section in the Venetian Pre-Alps, Italy: GSA Bulletin.

Hancock, H.J.L., Chaproniere, G.C., Dickens, G.R., and Henderson, R.A., 2002, Early Palaeogene planktic foraminiferal and carbon isotope stratigraphy, Hole 762C, Exmouth Plateau, northwest Australian margin: Journal of Micropalaeontology, v. 21, p. 29-42.

Hancock, H.J.L., Dickens, G.R., Strong, C.P., Hollis, C.J., and Field, B.D., 2003, Foraminiferal and carbon isotope stratigraphy through the Ppaleocene-Eocene transition at Dee Stream, Marlborough, New Zealand: New Zealand Journal of Geology and Geophysics, v. 46, p. 1-19.

Hasegawa, T., Yamamoto, S., and Pratt, L.M., submitted, Data Report: Stable carbon isotope fluctuation of long chain n-alkanes from Leg 208, Site 1263A across the Paleocene/Eocene boundary, in Kroon, D., Zachos, J.C., and Richter, C., eds., Scientific Results, Volume 208: College Station, Ocean Drilling Program.

Heinze, C., 2004. Simulating the CaCO3 counter pump in the greenhouse. Geophys. Res. Lett., 31(L16308):doi:10.1029/2004GL026013.

Hollis, C.J., Dickens, G.R., Field, B.D., Jones, C.M., and Strong, C.P., 2005, The Paleocene-Eocene transition at Mead Stream, New Zealand: a southern Pacific record of early Cenozoic global change: Palaeogeography Palaeoclimatology Palaeoecology, v. 215, p. 313-343.

Hooke, R.L., 2000. Toward a uniform theory of clastic sediment yield in fluvial systems. Geological Society of America Bulletin, 112(12): 1778-1786.

Horita J., Zimmermann H., and Holland H. D., 2002. Chemical evolution of seawater during the Phanerozoic: Implications from the record of marine evaporites. Geochim. Cosmochim. Acta 66(21), 3733-3756.

Howard, M.T., Klass, C., Maier-Reimer, E., Winguth, A.M.E., (2005). Mineral Ballasting of POC in an Ocean Carbon Cycle Model. Global Biogeochemical Cycles, in press.

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

Huber, M., and Caballero, R., 2003, Eocene El Nino: Evidence for robust tropical dynamics in the "hothouse": Science, v. 299, p. 877-881.

Huber, M., and Sloan, L.C., 2001, Heat transport, deep waters, and thermal gradients: Coupled simulation of an Eocene Greenhouse Climate: Geophysical Research Letters, v. 28, p. 3481-3484.

0628719

D-4

John, C., Bohaty, S.M., Sluijs, A., Brinkhuis, H., and Zachos, J., 2005, Coast-to-Coast Record of the Paleocene-Eocene Thermal Maximum in shallow marine environments, EOS Trans. AGU, Volume 86: Fall Meet. Suppl., p. Abstract PP51B-0591.

Kaiho, K., Arinobu, T., Ishiwatari, R., Morgans, H.E.G., Okada, H., Takeda, N., Tazaki, K., Zhou, G.P., Kajiwara, Y., Matsumoto, R., Hirai, A., Niitsuma, N., and Wada, H., 1996, Latest paleocene benthic foraminiferal extinction and environmental changes at Tawanui, New Zealand: Paleoceanography, v. 11, p. 447-465.

Kaiho, K., Takeda, K., Petrizzo, M.R., and Zachos, J.C., in press, Anomalous shifts in tropical Pacific planktonic and benthic foraminiferal test size during the Paleocene-Eocene thermal maximum: Palaeogeogr., Palaeoclimatol., Palaeoecol.

Katz, M. E., D. K. Pak, G. R. Dickens, and K. G. Miller. The source and fate of massive carbon input during the Latest Paleocene Thermal Maximum. Science 286: 1531-33, 1999.

Keir, R., 1982. Dissolution of calcite in the deep sea: Theoretical predictions for the case of uniform size particles settling into a well-mixed sediment. Am. J. Sci., 282, 193-236.

Kelly, D.C., 2002, Response of Antarctic (ODP Site 690) planktonic foraminifera to the Paleocene-Eocene thermal maximum: Faunal evidence for ocean/climate change: Paleoceanography, v. 17, p. 1071.

Kelly, D.C., Bralower, T.J., and Zachos, J.C., 1998, Evolutionary consequences of the latest Paleocene thermal maximum for tropical planktonic foraminifera: Palaeogeography Palaeoclimatology Palaeoecology, v. 141, p. 139-161.

Kelly, D.C., Bralower, T.J., Zachos, J.C., Silva, I.P., and Thomas, E., 1996, Rapid Diversification of Planktonic Foraminifera in the Tropical Pacific (Odp Site 865) During the Late Paleocene Thermal Maximum: Geology, v. 24, p. 423-426.

Kelly, D.C., Zachos, J.C., Bralower, T.J., and Schellenberg, S.A., 2005, Enhanced terrestrial weathering/runoff and surface ocean carbonate production during the recovery stages of the Paleocene-Eocene thermal maximum: Paleoceanography, v. 20, p. -.

Kennett, J.P., and Stott, L.D., 1991, Abrupt Deep-Sea Warming, Palaeoceanographic Changes and Benthic Extinctions At the End of the Palaeocene: Nature, v. 353, p. 225-229.

Klaas, C., and D. E. Archer, Association of sinking organic matter with various types of mineral ballast in the deep sea: Implications for the rain ratio, Global Biogeochem. Cycles, 16(4), 1116, doi:10.1029/2001GB001765, 2002.

Koch, P.L., Zachos, J.C., and Gingerich, P.D., 1992, Correlation Between Isotope Records in Marine and Continental Carbon Reservoirs Near the Palaeocene Eocene Boundary: Nature, v. 358, p. 319-322.

Kurtz, A., Kump, L.R., Arthur, M.A., Zachos, J.C., and Paytan, A., 2003, Early Cenozoic decoupling of the global carbon and sulfur cycles: Paleoceanography, v. 18, p. 1090.

Langer, G., Nehrke, G., Riebesell, U., Eisenhauer, A., Kuhnert, H., Rost, B., Trimborn, S., and Thoms, S., 2006, Coccolith strontium to calcium ratios in Emiliania huxleyi: the dependence on seawater strontium and calcium concentrations: Limnology and Oceanography, v. 51, p. 310-320.

Lourens, L.J., Sluijs, A., Kroon, D., Zachos, J.C., Thomas, E., Rohl, U., Bowles, J., and Raffi, I., 2005, Astronomical pacing of late Palaeocene to early Eocene global warming events: Nature, v. 435, p. 1083-1087.

Lowenstein T. K., Timofeeff M. N., Brennan S. T., Hardie L. A., and Demicco R. V. Oscillations in Phanerozoic seawater chemistry: Evidence from fluid inclusions. Science, 294, 1086-1088, 2001.

Lu, G.Y., Adatte, T., Keller, G., and Ortiz, N., 1998, Abrupt climatic, oceanographic and ecologic changes near the Paleocene-Eocene transition in the deep Tethys basin: The Alademilla section, southern Spain: Eclogae Geologicae Helvetiae, v. 91, p. 293-306.

Ludwig W.; Amiotte-Suchet P.; Probst J.-L., 1999. Enhanced chemical weathering of rocks during the last glacial maximum: a sink for atmospheric CO2? Chemical Geology 159: 147-161.

Lyle, M., Wilson, P.A., Janecek, T., et al., 2002, Proc. ODP, Initial Reports: College Station, TX, Ocean Drilling Program, v. 199.

0628719

D-5

Maier-Reimer, E., 1993. Geochemical cycles in an ocean general circulation model Preindustrial tracer distributions, Global Biogeochem. Cycles, 7, 645-677.

Marcantonio, F., et al. 1995. Comparative study of accumulation rates derived by Th and He isotope analyses of marine sediments. Earth and Planetary Science Letters 133: 549-555.

Marcantonio, F., et al. 1996. Extraterrestrial 3He as a tracer of marine sediment transport and accumulation. Nature 383: 705-707.

Markwick, P.J. and Valdes, P.J., 2004. Paleaeo-digital elevation models for use as boundary conditions in coupled ocean-atmosphere GCM experiments: a Maastrichtian (late Cretaceous) example. Palaeogeogr. Palaeoclim. Palaeoecol. 213: 37-63.

McCarren, H., Thomas, E., and Zachos, J.C., 2005a, Depth dependant variations in benthic foraminiferal assemblages and stable isotopes across the P-E boundary, Walvis Ridge (ODP Leg 208), AGU Fall Meeting: San Francisco.

McCarren, H., Zachos, J.C., Roehl, U., and Westerhold, T., 2005b, Long Term orbital scale paleoceanographic variability across the Paleocene-Eocene boundary in the central Pacific: inference fron stable isotope and geochemical core log data, Geologic Society of America Annual Meeting: Salt Lake City, UT.

McCarren, H., Zachos, J.C., Roehl, U., and Westerhold, T., in prep, A 3 m.y. long orbitally-tuned carbon isotope record across the Paleocene-Eocene Boundary.

Millero, F. J. and D. Pierrot, A chemical equilibrium model for natural waters, Aquatic Geochemistry, 4, 153-199, 1998.

Milliman, J.D. and Syvitski, J.P.M. 1992. Geomorphic /tectonic control of sediment discharge to the ocean: The importance of small mountainous rivers. J. Geol. 100: 525-544.

Mukhopadhyay, S., et al., 2001. A 35 Myr record of helium in pelagic limestones: implications for interplanetary dust accretion from the early Maastrichtian to the Middle Eocene. Geochimica et Cosmochimica Acta 65: 653-669.

New, M., Hulme, and, P. Jones, Representing Twentieth-Century Space–Time Climate Variability. Part I: Development of a 1961–90 Mean Monthly Terrestrial Climatology Journal of Clim. 1999 12: 829-856.

Nicolo, M.J., 2005, Searching for New Zealand Outcrops for ELMO, Geologic Society of America Annual Meeting, Volume 37: Salt Lake City, UT.

Nunes, F., and Norris, R.D., 2006, Abrupt reversal in ocean overturning during the Palaeocene/Eocene warm period: Nature, v. 439, p. 60-63.

Opdyke, B.N., and Wilkinson, B.H., 1993. Oceanic carbonate saturation and cratonic carbonate accumulation: American Journal of Science, v. 293, p. 217-234.

Orr, J.C., Fabry, V.J., Aumont, O., Bopp, L., Doney, S.C., Feely, R.A., Gnanadesikan, A., Gruber, N., Ishida, A., Joos, F., Key, R.M., Lindsay, K., Maier-Reimer, E., Matear, R., Monfray, P., Mouchet, A., Najjar, R.G., Plattner, G.K., Rodgers, K.B., Sabine, C.L., Sarmiento, J.L., Schlitzer, R., Slater, R.D., Totterdell, I.J., Weirig, M.F., Yamanaka, Y., and Yool, A., 2005, Anthropogenic ocean acidification over the twenty-first century and its impact on calcifying organisms: Nature, v. 437, p. 681-686.

Ozima, M., et al., 1984. High 3He/4He ratios in ocean sediments. Nature 311: 449-451. Pagani, M., Pedentchouk, N., Huber, M., Sluijs, A., Schouten, S., Brinkhuis, H., Sinninghe Damsté, J.S.,

Dickens, G.R., and Scientists, I.E.E., in press, Arctic’s hydrology during global warming at the Palaeocene-Eocene thermal maximum: Nature.

Pagani, M., Zachos, J.C., Freeman, K.H., Tipple, B., and Bohaty, S., 2005, Marked decline in atmospheric carbon dioxide concentrations during the Paleogene: Science, v. 309, p. 600-603.

Parton, W.J., D.S. Schimel, C.V. Cole, and D.S. Ojima. 1987. Analysis of factors controlling soil organic matter levels in Great Plains grasslands. Soil Sci. Soc. Amer. J. 51:1173–1179.

Ravizza, G., Norris, R.N., Blusztajn, J., and Aubry, M.P., 2001, An osmium isotope excursion associated with the late Paleocene thermal maximum: Evidence of intensified chemical weathering: Paleoceanography, v. 16, p. 155-163.

0628719

D-6

Rickaby, R.E.M., Bard, E., Sonzogni, C., Rostek, F., Beaufort, L., Barker, S., Rees, G., and Schrag, D.P., in review, Coccolith chemistry reveals secular variations in the global ocean carbon cycle?: Earth and Planetary Science Letters.

Rickaby, R.E.M., Schrag, D.P., Zondervan, I., and Riebesell, U., 2002, Growth rate dependence of Sr incorporation during calcification of Emiliania huxleyi: Global Biogeochemical Cycles, v. 16.

Ridgwell, A., and Zeebe, R.E., 2005, The role of the global carbonate cycle in the regulation and evolution of the Earth system: Earth and Planetary Science Letters, v. 234, p. 299-315.

Ridgwell, A., Panchuk, K., and Kump, L., 2005. Carbonate lysocline and d13C changes at the PETM: How much carbon. EOS Trans. AGU, 86(52), Fall Meet. Suppl., Abstract PP42A-06.

Riebesell, U., Zondervan, I., Rost, B., Tortell, P.D., Zeebe, R.E., and Morel, F.M.M., 2000, Reduced calcification of marine plankton in response to increased atmospheric CO2: Nature, v. 407, p. 364-367.

Robert, C., and Kennett, J.P., 1994, Antarctic Subtropical Humid Episode At the Paleocene-Eocene Boundary - Clay-Mineral Evidence: Geology, v. 22, p. 211-214.

Röhl, U., Bralower, T.J., Norris, R.D., and Wefer, G., 2000, New chronology for the late Paleocene thermal maximum and its environmental implications: Geology, v. 28, p. 927-930.

Schmitz, B., Pujalte, V., and Nunez-Betelu, K., 2001, Climate and sea-level perturbations during the initial eocene thermal maximum: evidence from siliciclastic units in the Basque Basin (Ermua, Zumaia and Trabakua Pass), northern Spain: Palaeogeography Palaeoclimatology Palaeoecology, v. 165, p. 299-320.

Schmitz, B., Speijer, R.P., and Aubry, M.P., 1996, Latest paleocene benthic extinction event on the southern tethyan shelf (Egypt): Foraminiferal stable isotopic (delta C- 13,delta O-18) records: Geology, v. 24, p. 347-350.

Shellito, C.J., Sloan, L.C., and Huber, M., 2003, Climate model sensitivity to atmospheric CO2 levels in the Early-Middle Paleogene: Palaeogeography Palaeoclimatology Palaeoecology, v. 193, p. 113-123.

Sigman D.M., D.C. McCorkle, and W.R. Martin, 1998. The calcite lysocline as a constraint on glacial/interglacial low-latitude production changes.Global Biogeochem. Cycles, 12(3), 409-427.

Speijer, R.P., and Schmitz, B., 1998, A benthic foraminiferal record of Paleocene sea level and trophic/redox conditions at Gebel Aweina, Egypt: Palaeogeography Palaeoclimatology Palaeoecology, v. 137, p. 79-101.

Spero, H.J., Bijma, J., Lea, D.W., and Bemis, B.E., 1997, Effect of Seawater Carbonate Concentration on Foraminiferal Carbon and Oxygen Isotopes: Nature, v. 390, p. 497-500.

Stoll, H., and Ziveri, P., 2004, Coccolithophorid-based geochemical proxies, in Thierstein, H., and Young, J., eds., Coccolithophores: From Molecular Processes to Global Impact: New York, Springer-Verlag, p. 529-562.

Stoll, H., Ziveri, P., Shimizu, N., Conte, M.H., and Theroux, S., in review-a, Relationship between coccolith Sr/Ca ratios and coccolithophore production and export in the Arabian Sea and Sargasso Sea: Deep Sea Research II.

Stoll, H.M., 2005, Limited range of interspecific vital effects in coccolith stable isotopic records during the Paleocene Eocene thermal maximum: Paleoceanography, v. 20.

Stoll, H.M., and Bains, S., 2003, Coccolith Sr/Ca records of productivity during the Paleocene-Eocene thermal maximum from the Weddell Sea: Paleoceanography, v. 18.

Stoll, H.M., and Ziveri, P., 2002, Separation of monospecific and restricted coccolith assemblages from sediments using differential settling velocity: Marine Micropaleontology, v. 46, p. 209-221.

Stoll, H.M., Shimizu, N., Ziveri, P., and Archer, D., in review-b, Marine Productivity Response to Greenhouse Event of the Paleocene-Eocene Thermal Maximum: Nature.

Stott, L.D., Sinha, A., Thirty, M., Aubry, M.P., and Berggren, W.A., 1996, Global d13C changes across the Paleocene/Eocene boundary: Criteria for terrestrial-marine correlations., in Prothero, D.A.a.B., W. A., ed., Eocene-Oligocene Climate and Biotic Evolution: Princton, Princton University Press, p. 245-271.

0628719

D-7

Summerfield, M.A. and Hulton, N.J., 1994. Natural controls of fluvial denudation rates in major world drainage basins. J. Geop. Res. 99: 13871-13883.

Sundquist, E. T. , 1986. Geologic Analogs: Their value and limitations in carbon dioxide research, In The Changing Carbon cycle: A Global Analysis, eds. J.R. Trabalka and D.E. Reichle, 371-402, Springer-Verlag, New York.

Svenson, H., Planke, S., Malthe-Sorenssen, A., Jamtveit, B., Myklebust, R., Eidem, T.R., and Rey, S.S., 2004, Release of methane from a volcanic basin as a mechanism for initial Eocene global warming.: Nature, v. 429, p. 524-527.

Takayanagi, M., et al., 1987.. Temporal variation of 3He/4He in deep-sea sediment cores. Journal of Geophysical Research 92: 12531-12538.

Thiry, M., 2000. Palaeoclimatic interpretation of clay minerals in marine deposits: an outlook from the continental origin [Review]. Earth-Science Reviews, 49(1-4): 201-221.

Thomas, D.J., Bralower, T.J., and Jones, C.E., 2003, Neodymium isotopic reconstruction of late Paleocene-early Eocene thermohaline circulation: Earth & Planetary Science Letters, v. 209, p. 309-322.

Thomas, D.J., Bralower, T.J., and Zachos, J.C., 1999, New evidence for subtropical warming during the late Paleocene thermal maximum: Stable isotopes from Deep Sea Drilling Project Site 527, Walvis Ridge: Paleoceanography, v. 14, p. 561-570.

Thomas, E., and Shackleton, N.J., 1996, The Paleocene-Eocene benthic foraminiferal extinction and stable isotope anomalies, in Knox, R.W.O.B., Corfield, R.M., and Dunay, R.E., eds., Correlation of the early Paleogene in Northwest Europe, Volume 101: Geoligical Society Special Publication: London, p. 401-441.

Tripati, A.K., and Elderfield, H., 2004, Abrupt hydrographic changes in the equatorial Pacific and subtropical Atlantic from foraminiferal Mg//Ca indicate greenhouse origin for the thermal maximum at the Paleocene-Eocene Boundary: Geochemistry Geophysics Geosystems, v. 5, p. 2003GC000631.

Tyrrell, T. and R. E. Zeebe. History of carbonate ion concentration over the last 100 million years. Geochim. Cosmochim. Acta, 68(17), 3521-3530, 2004.

Walker, J.C.G., and Kasting, J.F., 1992, Effects of fuel and forest conservation on future levels of atmospheric carbon dioxide: Palaeogeogr., Palaeoclimatol., Palaeoecol., v. 97, p. 151-189.

Weaver, A.J., 11 co-authors, 2001. The UVic earth system climate model: model description, climatology, applications to past,present and future climates. Submitted to Atmos. Ocean.

Westerhold, T., Röhl, U., Laskar, J., Raffi, I., Bowles, J., Lourens, L.J., and Zachos, J.C., 2005, New high-resolution chronology from the first complete late Paleocene – early Eocene marine records from Walvis Ridge: duration of Chron 24r and new constraints on the timing of early Eocene global warming events, Geologic Society of America Ann. Meeting: Salt Lake City.

Westerhold, T., Röhl, U., Laskar, J., Raffi, I., Bowles, J., Lourens, L.J., and Zachos, J.C., in prep., New high-resolution chronology from the first complete late Paleocene – early Eocene marine records from Walvis Ridge: duration of Chron 24r and new constraints on the timing of early Eocene global warming event. To be submitted to Paleoceanography.

Williams, J.R., and Bralower, T.J., 1995, Nannofossil Assemblages, Fine Fraction Stable Isotopes, and the Paleoceanography of the Valanginian-Barremian (Early Cretaceous) North-Sea Basin: Paleoceanography, v. 10, p. 815-839.

Wing, S.L., Harrington, G.J., Smith, F.A., Bloch, J.I., Boyer, D.M., and Freeman, K.H., 2005, Transient floral change and rapid global warming at the Paleocene-Eocene boundary: Science, v. 310, p. 993-996.

Winguth, A., Mikolajewicz, U., Groger, M., Maier-Reimer, E., Schurgers, G., and Vizcaino, M., 2005, Centennial-scale interactions between the carbon cycle and anthropogenic climate change using a dynamic Earth system model: Geophysical Research Letters, v. 32, p. -.

Winguth, A.M.E., and Maier-Reimer, E., 2005, Causes of the marine productivity and oxygen changes associated with the Permian-Triassic boundary: A reevaluation with ocean general circulation models: Marine Geology, v. 217, p. 283-304.

0628719

D-8

Winguth, A.M.E., Archer, D., Duplessy, J.C., Maier-Reimer, E., and Mikolajewicz, U., 1999, Sensitivity of paleonutrient tracer distributions and deep-sea circulation to glacial boundary conditions: Paleoceanography, v. 14, p. 304-323.

Winguth, A.M.E., Heimann, M., Kurz, K.D., Maierreimer, E., Mikolajewicz, U., and Segschneider, J., 1994, El-Nino-Southern Oscillation Related Fluctuations of the Marine Carbon-Cycle: Global Biogeochemical Cycles, v. 8, p. 39-63.

Zachos, J., Pagani, M., Sloan, L., Thomas, E., and Billups, K., 2001, Trends, rhythms, and aberrations in global climate 65 Ma to present: Science, v. 292, p. 686-693.

Zachos, J.C., Kroon, D., Blum, P., et al., 2004, Early Cenozoic Extreme Climates: The Walvis Ridge Transect. Proc. ODP, Initial Reports: College Station.

Zachos, J.C., Rohl, U., Schellenberg, S.A., Sluijs, A., Hodell, D.A., Kelly, D.C., Thomas, E., Nicolo, M., Raffi, I., Lourens, L.J., McCarren, H., and Kroon, D., 2005, Rapid acidification of the ocean during the Paleocene-Eocene thermal maximum: Science, v. 308, p. 1611-1615.

Zachos, J.C., Schouten, S., Bohaty, S., Sluijs, A., Brinkhuis, H., Gibbs, S., Bralower, T., and Quattlebaum, T., submitted, Extreme warming of mid-latitude coastal ocean during the Paleocene-Eocene Thermal Maximum: Inferences from TEX86 and Isotope Data: Geology.

Zachos, J.C., Stott, L.D., and Lohmann, K.C., 1994, Evolution of Early Cenozoic Marine Temperatures: Paleoceanography, v. 9, p. 353-387.

Zachos, J.C., Wara, M.W., Bohaty, S., Delaney, M.L., Petrizzo, M.R., Brill, A., Bralower, T.J., and Premoli-Silva, I., 2003, A transient rise in tropical sea surface temperature during the Paleocene-Eocene Thermal Maximum: Science, v. 302, p. 1551-1554.

Zeebe, R. E. and D. A. Wolf-Gladrow, CO2 in Seawater: Equilibrium, Kinetics, Isotopes, Elsevier Oceanography Series, 65, pp. 346, Amsterdam, 2001.

Zeebe, R. E., and P. Westbroek. A simple model for the CaCO3 saturation state of the ocean: The ”Strangelove”, the ”Neritan”, and the ”Cretan” Ocean. Geochem. Geophys. Geosyst., 4(12):1104, doi:10.1029/2003GC000538, 2003.

Zeebe, R.E., and D. Archer, Feasibility of ocean fertilization and its impact on future atmospheric CO2 levels. Geophys. Res. Lett., 32, L09703,doi:10.1029/2005GL022449, 2005.

0628719

JAMES C. ZACHOSProfessor

Earth Sciences DepartmentUniversity of California, Santa Cruz, CA 95064

(831)459-4644; [email protected]

EDUCATION:

Ph.D. 1988Graduate School of Oceanography, University of Rhode Island

M.S. 1984University of South Carolina

B.S. 1981State University of New York, Oneonta

EMPLOYMENT

July 2000 - Present Professor, Univ. of California, Santa CruzJuly 1999 – June 2003 Director, Center DELSIJuly 1996 - 2000 Associate Professor, Univ. of California, Santa CruzJuly 1992 - June 1996 Assistant Professor, Univ. of California, Santa CruzNovember 1990 - June 1992 Assistant Research Scientist, Univ. of MichiganSeptember 1988 - November 1990 Post Doctoral Scholar, Univ. of MichiganSeptember 1983 - August 1987 Graduate Research Assistant, Univ. of Rhode IslandJanuary 1982 -August 1983 Graduate Teaching Assistant, Univ. of South Carolina

OTHER PROFESSIONAL ACTIVITIES:

July-Dec 2004 Bremen University Visiting FellowMarch 2003 Chief Scientist, ODP Leg 208August 2001 Sedimentologist, ODP Leg 198Fall 2000 Cambridge University, Visiting Fellow1996 - Present Fellow, Canadian Inst. Advanced ResearchJanuary 1994 Sedimentologist, ODP Leg 154February 1988 Organic Geochemist, ODP Leg 120August 1985 Inorganic Geochemist, ODP Leg 1051996-2001 Editorial Board, Geological Society America Bulletin1995-2003 Editorial Board Palaeogeography, Palaeoclimatology, Palaeoecology1995-1997 Editorial Board Geology

NATIONAL and INTERNATIONAL COMMITTEE & PANEL SERVICE

U.S. Carbon Cycle Scientific Steering Group (3/05-present); MESH, NSF Ocean SciencesSteering Committee (1/00 – present); NSF Panel (6/00); JOIDES Scientific Committee(6/99-6/01); Smithsonian Inst. Scholarly Studies Prog. Review Committee (6/99); JOIDESArctic Program Planning Group (1/99-1/01); JOIDES Extreme Climates Program PlanningGroup (1/98-1/00); JOIDES Ocean History Panel (3/92-6/95)

0628719

SELECTED PUBLICATIONS (2001-2005)

Zachos, J. C., N. J. Shackleton, J. S. Revenaugh, H. Pälike, and B. P. Flower, 2001, Periodicand non-periodic climate response to orbital forcing across the Oligocene-Mioceneboundary. Science, v. 292, p.274-277.

Zachos, J. C., M. Pagani, L. Sloan, K. Billups, and E. Thomas, 2001, Trends, rhythms, andaberrations in global climate 65 Ma to present. Science, v.292, p. 686-693.

Thomas, D., J. Zachos, T. Bralower, E. Thomas, S. Bohaty, 2002, Warming the Fuel forthe Fire: Evidence for the thermal dissociation of methane hydrate during the Paleocene-Eocene thermal maximum. Geology, v.30, p.1067-1070.

Zachos, J. C., M. W. Wara, S. M. Bohaty, M. L. Delaney, M. Rose-Petrizzo, A. Brill, T. J.Bralower, and I. Premoli -Silva, 2003, A transient rise in tropical sea surface temperatureduring the Paleocene-Eocene Thermal Maximum. Science v. 302, p. 1551-1554.

Bohaty, S. M. and J. C. Zachos, 2003, A significant Southern Ocean warming event in thelate middle Eocene. Geology. v. 31, p. 1017-1020.

Billups K., H. Palike, J.E.T. Channell, J.C. Zachos, N.J. Shackleton, 2004. Astronomiccalibration of the late Oligocene through early Miocene geomagnetic polarity time scale.Earth and Planetary Science Letters, v. 224 (1-2): 33-44.

Bowen, G.J., D.J. Beerling, P.L. Koch, J.C. Zachos, and T. Quattlebaum, 2004. A humidclimate state during the Paleocene/Eocene thermal maximum. Nature v. 432, p. 495-499.

Zachos, J.C., and L. R. Kump, 2005, Carbon cycle feedbacks and the initiation of Antarcticglaciation in the earliest Oligocene. Global & Planetary Change, v. 47, p. 51-66.

Zachos, J. C., U. Röhl, S.A. Schellenberg, A. Sluijs, D. A. Hodell, D. C. Kelly, E. Thomas,M. Nicolo, I. Raffi, L. J. Lourens, D. Kroon, H. McCarren, 2005. Rapid Acidification of theOcean during the Paleocene-Eocene Thermal Maximum. Science, v. 308, p.1611-1615.

Lourens, L. J., A. Sluijs , D. Kroon , J. C. Zachos , E. Thomas , U. Röhl , J. Bowles, 2005.An early Eocene transient warming (~53 Ma): Implications for astronomically paced earlyEocene hyperthermal events. Nature

Pagani, M. J.C. Zachos, K. H. Freeman, B. Tipple, S. Bohaty, 2005. Marked decline inatmospheric carbon dioxide concentrations during the Paleogene. Science, v. 308, p.

PhD. AdvisorMichael Arthur, PSU

CollaboratorsTim Bralower, PSUClay Kelly, WisconsinSteve D’Hondt, URILee Kump, PSUScott Wing, SmithsonianGabe Bowen, PurdueHenk Brinkhuis, UtrechtUrsula Rohl, BremenLucas Lourens, Utrecht

Heiko Palike, SOCEllen Thomas, YaleStefan Schouten, NIOSJerry Dickens, Rice ULisa Sloan, UCSCPaul Koch, UCSCPeggy Delaney UCSCChris Hollis, NZSamantha Gibbs, SOC

Former Post DocsBenjamin Flower, USFStephen Schellenberg,

Mark Pagani, Yale U.Cedric John, TAMU

Former GraduateStudentsK, Billups, U of DelawareH. Paul, ETHZK. Salamy, MBARIA, Tripati, CambridgeJulia FrazierThomas Quattlebau

0628719

Biographical Sketch for Daniel Clay Kelly

(i) Professional Preparation

Ph.D., Geology, University of North Carolina at Chapel Hill, 1999 M.S., Geology, Florida State University, 1993 B.S., Geology, Florida State University, 1985 (ii) Appointments 2001 – present, Assistant Professor, Dept. of Geology and Geophysics, University of

Wisconsin – Madison

2003, Ocean Drilling Program, Shipboard Scientist (Biostratigrapher) ODP Leg 208 2000 – 2001, Postdoctoral Investigator, Dept. of Geology and Geophysics, Woods Hole

Oceanographic Institution 2000, Ocean Drilling Program, Shipboard Scientist (Biostratigrapher) ODP Leg 189 1998 – 2000, Postdoctoral Scholar, Dept. of Geology and Geophysics, Woods Hole

Oceanographic Institution

(iiia) Five publications related to proposal:

Kelly, D.C., Zachos, J.C., Bralower, T.J., Schellenber, S.A., 2005. Enhanced terrestrial weathering/runoff and surface-ocean carbonate production during the recovery stages of the Paleocene-Eocene thermal maximum. Paleoceanography, v. 20, PA4023, doi: 10.1029/2005PA001163, 11 p. Zachos, J.C., Röhl, U., Schellenberg, S.A., Sluijs, A., Hodell, D.A., Kelly, D.C., et al., 2005. Rapid acidification of the ocean during the Paleocene-Eocene thermal maximum. Science, v. 308: 1611-1615. Kelly, D.C., 2002. Response of Antarctic (ODP Site 690) planktonic foraminifera to the Paleocene-Eocene thermal maximum: faunal evidence for ocean/climate change. Paleoceanography, v. 17(4), doi: 10.1029/2002PA000761, 13 p.

Kelly, D.C., Bralower, T.J., and Zachos, J.C., 1998. Evolutionary consequences of the latest Paleocene thermal maximum for tropical planktonic foraminifera. Palaeogeography, Palaeoclimatology, Palaeoecology, v. 141: 139-161. Kelly, D.C., Bralower, T.J., Zachos, J.C., Premoli Silva, I., and Thomas, E., 1996. Rapid diversification of planktonic foraminifera in the tropical Pacific (ODP Site 865) during the late Paleocene thermal maximum. Geology, v. 24: 423-426. (iiib) Selection of five other publications:

Harrington, G.J., Clechenko, E.R., Kelly, D.C., 2005. Palynology and organic-carbon isotope ratios across a terrestrial Palaeocene/Eocene boundary section in the Williston Basin, North Dakota, USA. Palaeogeography, Palaeoclimatology, Palaeoecology, v. 226: 214-232.

0628719

Bralower, T.J., Kelly, D.C., Thomas, D.J., 2004. Comment on “Coccolith Sr/Ca records of productivity during the Paleocene-Eocene thermal maximum from the Weddell Sea”. Paleoceanography, v. 19, PA1014, doi: 10.1029/2003PA000953. Tedford, R. A., Kelly, D. C., 2004. A deep-sea record of the Late Miocene carbon shift from the Southern Tasman Sea. In: Exon, N., Kennett, J.P., Malone, M. (eds.), The Cenozoic Southern Ocean: Tectonics, Sedimentation and Climate Change between Australia and Antarctica. AGU Geophysical Monograph Series, 151: 273-290.

Kelly, D.C., Norris, R.D., Zachos, J.C., 2003. Deciphering the paleoceanographic significance of Early Oligocene Braarudosphaera chalks in the South Atlantic. Marine Micropaleontology, v. 49: 49-63. Kelly, D.C., Bralower, T. J., and Zachos, J.C., 2001. On the demise of the Early Paleogene Morozovella velascoensis lineage: terminal progenesis in the planktonic foraminifera. Palaios, v. 16: 507-523. (iv) Synergistic Activities

2003-06, Public Outreach: Collaborating with Geology Museum at the University of Wisconsin to design an exhibit that showcases how deep-sea cores are used to study ocean/climate change and biotic evolution. 2001-05, Curriculum development: Designed, taught, and implemented both Geobiology and

Introductory Micropaleontology for department undergraduate/graduate curriculum. I also teach Survey of Oceanography to large undergraduate classes each year, and will be offering an upper division class on Marine Geology/Paleoceanography. 2001/02, Refurbished micropaleontology lab that is used daily by both undergraduate and graduate students. (va) Collaborators on papers in last 48 months: Rebecca Tedford (Louisiana State Univ.), Timothy J. Bralower (Pennsylvania State University), Linda Elkins-Tanton (Brown University), Guy Harrington (Birmingham Univ., U.K.), Richard D. Norris (Scripps), James C. Zachos (U.C. – Santa Cruz), James P. Kennett (U.C. – Santa Barbara), Neville Exon (Australian Geological Survey Organization), Debbie Thomas (Texas A&M Univ.), Ellen Thomas (Wesleyan College, CT), Elizabeth Clechenko (Univ. of Wisconsin – Madison), Adam Eisenach (Univ. of Wisconsin – Madison), Stephen Schellenberg (San Diego State Univ.)

(vb) Graduate and Postdoctoral Advisors: M.S.: Anthony J. Arnold (Florida State University); Ph.D.: Timothy J. Bralower (University of North Carolina – Chapel Hill); Postdoctoral: Richard D. Norris (WHOI/Scripps) (vc) Undergraduate and Graduate Advisor for Univ. of Wisconsin Students: Rebecca Tedford (M.S., 2003), Elizabeth Clechenko (Ph.D., 2007), Tina Nielsen (Ph.D., 2007), Jennifer Nielsen (M.S., 2006), Adam Eisenach (M.S., 2006), Eric Shullenberger (M.S., 2007), Laura Mitchell (M.S., 2007), Kathleen Bolger (M.S., 2007), Peter Gill (Senior Thesis, 2004)

0628719

TIMOTHY JAMES BRALOWER

Department of GeosciencesPennsylvania State University

University Park, PA 16802(814) 863-1240

[email protected]

Education: Ph.D. Earth Sciences, Scripps Institution of Oceanography,University of California, San Diego, 1986.

M.S. Oceanography, Scripps Institution of Oceanography,University of California, San Diego, 1982.

B.A. with Honours in Geology, Oxford University, England, 1980.

Professional Experience:Assistant Professor, Florida International University,State University of Florida at Miami, 1987-1990.

Assistant Professor, Geological and Marine Sciences, University ofNorth Carolina, Chapel Hill, 1990-1993.

Associate Professor, Geological and Marine Sciences, University ofNorth Carolina, Chapel Hill, 1993-1996.

Joseph Sloane Associate Professor of Geological and Marine Sciences,University of North Carolina, Chapel Hill, 1997-1998.

Joseph Sloane Professor of Geological and Marine Sciences,University of North Carolina, Chapel Hill, 1998-2002.

Chair, Department of Geological Sciences,University of North Carolina, Chapel Hill, 1998-2002.

Professor and Head, Department of Geosciences,Pennsylvania State University, 2003-.

Awards: Hettelman Junior Faculty Research Prize, UNC-CH, 1995.

Other Positions: Associate Editor, Geology, 1991-1993, 1999-2001, 2004-2006; MarineMicropaleontology, 1995-; Palaios, 1999-; Paleoceanography, 2001-.Member, Ocean History Panel, JOIDES, 1989-1992; JOI-USSAC (ODPUS Advisory Panel), 1999-2002.Distinguished Lecturer for Paleo. Soc., 1996-1997; ODP 2000-2001.Biostratigrapher, Ocean Drilling Program Legs 122, 143, 165.Co-Chief Scientist, Ocean Drilling Program Leg 198, 2001.Advisory Board of CHRONOS; Steering Committee of GeoSystems

0628486

BIBLIOGRAPHY (five most relevant publications)Bralower, T. J., 2002, Evidence for surface water oligotrophy during the Paleocene-Eocene Thermal

Maximum: Nannofossil assemblage data from Ocean Drilling Program Site 690, Maud Rise,Weddell Sea, Paleoceanography, v. 17, no. 2, 10.1029/2001PA000662

Bralower, T. J., Premoli Silva, I., Malone, M., and the Scientific Participants of Leg 198, 2002,Proceedings of the Ocean Drilling Program, Initial Report, v. 198. [Online]. Available from:http://www-odp.tamu.edu/publications/198_IR/198ir.htm.

Colosimo, A.B., Bralower, T.J., and Zachos, J.C., 2005, Evidence for lysocline shoaling andmethane hydrate dissociation at the Paleocene-Eocene thermal maximum on Shatsky Rise,ODP Leg 198. In Bralower, T.J., Premoli Silva, I., Malone, M.J., et al., 2002. Proc. ODP, Init.Repts., 198. Available from: http://www-odp.tamu.edu/publications/198_IR/198ir.htm.

Bralower, T.J., Premoli Silva, I., and Malone, M.J., 2006, Leg 198 Synthesis: A Remarkable 120-m.y. Record of Climate and Oceanography from Shatsky Rise, Northwest Pacific Ocean. InBralower, T.J., Premoli Silva, I., Malone, M.J., et al., 2002. Proc. ODP, Init. Repts., 198.Available from http://www-odp.tamu.edu/publications/198_IR/198ir.htm.

Gibbs, S. J., Bralower, T.J., Bown, P.R., Zachos, J.C., and Bybell, L., 2006, Decoupled shelf-ocean phytoplankton productivity responses across the Paleocene-Eocene ThermalMaximum. Geology, in press.

Five additional publicationsBralower, T. J., Zachos, J. C., Thomas, E., Parrow, M., Paull, C. K., Kelly, D. C., Premoli

Silva, I., Sliter, W. V., and Lohmann, K. C., 1995, Late Paleocene to Eocenepaleoceanography of the equatorial Pacific Ocean: stable isotopes recorded at ODP Site865, Allison Guyot: Paleoceanography, v. 10, p. 841-865.

Bralower, T. J., Thomas, D. J., Zachos, J. C., Hirschmann, M. M., Röhl, U., Sigurdsson, H.,Thomas, E., and Whitney, D. L., 1997, High-resolution records of the late Paleocenethermal maximum and circum-Caribbean volcanism: Is there a causal link?: Geology, v. 25,p. 963-967.

Bralower, T. J., Premoli Silva, I., Malone, M., and the Scientific Participants of Leg 198,2002, New Evidence for abrupt climate change in the Cretaceous and Paleogene: An OceanDrilling Program expedition to Shatsky Rise, northwest Pacific, GSA Today, v. 12, no. 11,p. 4-10.

Thomas, D. J., J. C. Zachos, T. J. Bralower, E. Thomas, and S. Bohaty, 2002, Warming theFuel for the Fire: Evidence for the thermal dissociation of methane hydrate during thePaleocene-Eocene thermal maximum, Geology, v. 30, p. 1067-1070.

Thomas, D. J., Bralower, T. J., and Jones, C. E., 2003, Neodymium isotopic reconstruction ofLate Paleocene-Early Eocene thermohaline circulation, EPSL, v. 209, p. 309-322.

Graduate Students—Current and FormerMS Sarah Mock (Middle School Teacher, Portland, OR), John Williams (Environmental

company, Portland, OR), Celeste Burns (Owner of Forestry Company, Durham, NC),Deborah Thomas (Assistant Professor, Texas A&M), Linda de Romero (Independentconsultant), Jason Eleson (Exxon-Mobil), Andrew Bowman (Nebraska Ph.D. program),Amanda Colosimo (Instructor, Monroe CC), Lauren Fuqua (Instructor, College ofCharleston), Anna Hilting (Instructor, Carteret CC; with L. Kump), Andrea Kalb (current)

Ph.D. D. Clay Kelly (Assistant Professor, Wisconsin-Madison), Deborah Thomas (AssistantProfessor, Texas A&M), Jocelyn Sessa (current, joint with M. Patzkowsky)

CollaboratorsM. Arthur, P. Bown, M. Delaney, G. Dickens, R. Duncan, P. Falkowski, S. Gibbs, T. Herbert, D.Kelly, P. Koch, L. Kump, M. Leckie, J. Mahoney, K. Miller, I. Montañez, R. Norris, D. Osleger, A.Paytan, I. Premoli Silva, I. Raffi, U. Röhl, L. Sloan, D. Thomas, E. Thomas, S. Wing, J. Zachos.

0628486

F-1

Lee R. Kump Professor of Geosciences, Affiliate, Earth System Science Center, Associate, NASA Astrobiology Institute

The Pennsylvania State University, University Park, Pennsylvania 16802 Education

A.B. Honors, University of Chicago, 1981, Geophysical Sciences Ph.D., University of South Florida, 1986, Marine Sciences

Professional Experience

1997- Professor of Geosciences, Penn State 2005 - Reviewing Editor, Science 2002- Editor, Virtual Journal of Geobiology 2002-2005 Associate Editor, Geochimica et Cosmochimica Acta 1996-2000 Co-Editor, Geology 1994-2000 Associate Head, Department of Geosciences, Penn State 1991-1997 Associate Professor of Geosciences, Penn State 1986-1991 Assistant Professor of Geosciences, Penn State 1981-1983 Geologist, United States Geological Survey Fisher Island Station (summers)

Honors and Awards

2005 Faculty Mentoring Award, Penn State, College of Earth and Mineral Sciences 2000 Distinguished Service Award, Geological Society of America 1999 Pardee (Keynote) Symposium Lecturer, Geological Society of America 1997 Fellow, Geological Society of America 1994 Deike Research Award, Penn State 1991-1995 Marine Biological Association of the U.K., Geophysiology Modeling Fellowship 1992 Provost's Award for Collaborative Instruction and Curricular Innovation 1990 Bursary Fellowship, Marine Biological Association of the UK 1986-1987 Faculty Research Award

Membership in Professional Organizations

Canadian Institute for Advanced Research, Earth System Evolution Program (Assistant Director), Geological Society of London, Geochemical Society, American Geophysical Union, Geological Society of America (Fellow)

Five Relevant Articles in Referred Journals and Books

Kump, L.R., Pavlov, A., and Arthur, M.A., 2005. Massive release of hydrogen sulfide to the surface ocean and

atmosphere during intervals of oceanic anoxia. Geology 33: 397-400. Zachos, J.C. and Kump, L.R., 2005. Carbon cycle feedbacks and the initiation of Antarctic glaciation in the

earliest Oligocene. Global and Planetary Change 47: 51-66. Kurtz, A.C., Kump, L.R., Arthur, M.A., Zachos, J.C., and Paytan, A., 2003. Early Cenozoic decoupling of the

global carbon and sulfur cycles. Paleoceanography 18(4), 1090, doi:10.1029/2003PA000908. Hotinski, R.M., Kump, L.R., and Arthur, M.A., 2004. A δ13C gradient from platform carbonates of the Pethei

Group (Great Slave Lake Supergroup, N.W.T. Bull. Geol. Soc. Amer. 116: 539-554. Hotinski, R.M., Bice, K.L., Kump, L.R., Najjar, R.G., Arthur, M.A., 2001. Ocean stagnation and end-Permian

anoxia. Geology, 29: 7-10.

Five Other Articles in Referred Journals and Books Kump, L.R. and Seyfried, W.E., 2005. Hydrothermal Fe fluxes during the Precambrian: Effect of low oceanic

sulfate concentrations and low hydrostatic pressure on the composition of black smokers. Earth and Planetary Science Letters 235: 654-662.

0628486

F-2

Panchuk, K.M., Holmden, C., and Kump, L.R., in press. Sensitivity of the epeiric sea carbon isotope record to local-scale carbon cycle processes: Tales from the Mohawkian Sea. Palaeogeography Palaeoclimatology Palaeoecology.

Kump, L.R., 2004. The geochemistry of mass extinction. In: Turekian, K.K. and Holland, H.D. (eds.) Treatise on Geochemistry. Holland: Elsevier, Ch. 7.14, p. 351-368.

Kump, L.R. and Slingerland, R.L., 1999. Circulation and stratification of the Early Turonian Western Interior Seaway: Sensitivity to a variety of forcings. In: Barrera, E. and Johnson, C. (eds.), The Evolution of Cretaceous Ocean/Climate Systems, Special Paper of the Geological Society of America 332: 181-190.

Kump, L.R., Kasting, J.F., and Barley, M.E., 2001. Rise of atmospheric oxygen and the “upside-down” Archean mantle. Geochem. Geophys. Geosyst., 2, Paper number 2000GC000114.

Synergistic Activities • Reviewing editor, Science 2005-present • Served as Editor of Geology from 1996-1999 • Editor of Virtual Journal of Geobiology 2002-present. • Associate Editor, Geochimica et Cosmochimica Acta, 2002-present • Associate Head of Department of Geosciences, 1994-1999 • Served on NSF committee to develop Environmental Geochemistry and Biogeochemistry program • Promoting Earth system science: Lead author on the new textbook The Earth System, 2/e, chairing sessions at

national meetings on Earth system science in education • Director of the Earth Systems Exemplar Area of the Worldwide Universities Network • Participant in NSF-sponsored recruitment activities for underrepresented groups, including a summer coastal

marine science program for Pittsburgh inner-city high-school students Collaborators and Other Affiliations Collaborators outside Penn State within last 48 months R. Capo (Pittsburgh), B. Stewart (Pittsburgh), M. Schoonen (SUNY-Stony Brook), K. Bice (WHOI), E.

Shinn (USGS), W. Burnett (FSU), J. Chanton (FSU), P. Sheehan (U. Wisc.), P. Fawcett (Arizona), W. Seyfried (U. Minn.), M. Barley (U. W. Australia), J. Zachos (UCSC), M. Huber (Purdue),

E. Grossman (Texas A&M), G. Dickens (Rice), L. Sloan (UCSC), E. Thomas (Yale), M. Saltzmann (Ohio State), T. Lyons (U. Missouri)

Graduate Advisor: R. Garrels (deceased) Thesis/Postdoctoral Advisor To: Katherine Elliott (Langan Engineering), Lea Monaghan (consultant), Mark Gibbs (self-

employed), Gregg Bluth (faculty, Michigan Tech), Don Machusak (RE Wright Environmental), Paul Richards (Research Scientist, Univ. Michigan), Andrew Gratz (deceased), Andrew Kurtz (faculty, Boston Univ.), Virginia Seymour (self-employed), Erin Griggs (ERM Corp, environmental consultant), Ellen Herman (Pursuing Ph.D.), Michael Moreland (Apex Environmental, consultant), Roberta Hotinski (Princeton)

Total Graduate Students and Postdoctoral Associates Advised: 13 + 6 currently active

0628486

Biographical Sketch(es)

Richard E. Zeebe University of Hawaii at Manoa SOEST Department of Oceanography 1000 Pope Road Marine Science Building 504 Honolulu, HI 96822

(i) Professional Preparation

Undergraduate Institution: University of Bremen, Physics Diploma, 1995. Graduate Institution: Alfred Wegener Institute Bremerhaven, PhD, 1998. Dissertation title: A diffusion-reaction model for carbon isotope fractionation in foraminifera. Postdoctoral Institutions: Alfred Wegener Institute, Bremerhaven, 1998-1999, Lamont Doherty Earth Observatory, New York, 1999-2000, Alfred Wegener Institute, Bremerhaven, 2000-2003.

(ii) Appointments

Assistant Professor, University of Hawaii at Manoa, SOEST, 12/2003-today. (iii) Publications Five publications most relevant to proposed research

1. Zeebe, R. E., and D. Archer, Feasibility of ocean fertilization and its impact on future

atmospheric CO2 levels. Geophys. Res. Lett., 32, L09703, doi:10.1029/2005GL022449, 2005.

2. Ridgwell, A., and R. E. Zeebe. The role of the global carbonate cycle in the regulation and volution of the Earth system. FRONTIERS ARTICLE. Earth Planet. Sci. Lett., 234, 299-315, 2005.

3. Zeebe, R. E. and P. Westbroek, A simple model for the CaCO3 saturation state of the ocean:

The “Strangelove”, the “Neritan”, and the “Cretan” ocean. Geochem. Geophys. Geosyst., 4(12), 1104, doi:10.1029/2003GC000538, 2003.

4. Zeebe, R. E. and D. A. Wolf-Gladrow, CO2 in Seawater: Equilibrium, Kinetics, Isotopes, Elsevier

Oceanography Series, 65, pp. 346, Amsterdam, 2001. Reprinted in 2003.

5. Riebesell U., I. Zondervan, B. Rost, P. D. Tortell, R. E. Zeebe, and F. M. M. Morel, Reduced calcification of marine plankton in response to increased atmospheric CO2. Nature, 407, 364-367, 2000.

Five other significant publications

6. Tyrrell, T. and R. E. Zeebe. History of carbonate ion concentration over the last 100 million years. Geochim. Cosmochim. Acta, 68(17), 3521-3530, 2004.

0628394

7. Zeebe, R. E., D. A. Wolf-Gladrow, J. Bijma, and B. Hönisch, Vital effects in planktonic foraminifera do not compromise the use of δ11B as a paleo-pH indicator: Evidence from modeling. Paleoceanography, 18(2), doi: 10.1029/2003PA000881, 2003.

8. Zeebe, R. E., Seawater pH and Isotopic Paleotemperatures of Cretaceous Oceans.

Palaeogeography, Palaeoclimatology, Palaeoecology, 170(1-2) 49-57, 2001. 9. Jansen, H., R. E. Zeebe, and D. A. Wolf-Gladrow, Modeling the dissolution of settling CaCO3 in

the ocean. Global Biogeochem. Cycles, 16(2), 10.1029/2000GB001279, 2002.

10. Zeebe, R. E., H. Eicken, D. H. Robinson, D. A. Wolf-Gladrow, and G. S. Dieckmann, Modeling the heating and melting of sea ice through light absorption by microalgae. J. Geophys. Res., 101, 1163-1181, 1996.

(iv) Synergistic Activities

1. Published a text book on CO2 in seawater (Publication 4). 2. Served on NSF Panel 2006, Division of Atmospheric Sciences. 3. Advising of students at graduate and undergraduate level: L. Menviel, A. Andersson, K. Schulz,

H. Jansen, A. Wischmeyer, I. Tebas, B. Hoenisch, B. Rost, I. Zondervan. 4. Lecturing in advanced courses for PhD students of German-Dutch collaboration. Teaching at

University of Bremen: Master Course in Environmental Physics for mainly underrepresented groups in Germany (students from Asia).

5. Developed numerical routines for the calculation of the carbonate chemistry and made them freely available on the Internet. http://www.soest.hawaii.edu/oceanography/faculty_html/Zeebe2/CO2_System_in_Seawater/csys.html

(v) Collaborators & Other Affiliations David Archer (Chicago, US), Jelle Bijma (AWI, Germany), Hubertus Fischer (AWI, Germany), Gerald Ganssen (U. Amsterdam, The Netherlands), Baerbel Hoenisch (LDEO, US), David Lea (UCSB), Joseph Ortiz (Kent, US), Frank Peeters (U. Amsterdam, The Netherlands), Ulf Riebesell (IFM Kiel, Germany), Andy Ridgwell (UBC, Canada), Howard J. Spero (UC Davis, US), Toby Tyrrell (Southampton, UK), Peter Westbroek (Leiden, The Netherlands), Dieter Wolf-Gladrow (AWI, Germany), Jim Zachos (UC Santa Cruz, US). Previous funding (for US, see current and pending) Europe DFG (“German NSF“) Research grant (Ze 468/1-1). Full salary support for project at LDEO, Lamont, New York, USA (1999-2001). DFG/NWO Bilateral Research Program. Co-PI of ''Divalent Cations: Development and valida-tion of proxy Relationships''. (PIs: Bijma, J., Arlinghaus, H.). € 277,000 Funded. Period 08/2003-07/2006. Helmholtz Research Field Earth and Environment: Participating scientist of proposed AWI program “Marine Coastal and Polar Systems (MARCOPOLI)”. ESF EuroCLIMATE: Co-PI of “Foraminiferal Chemistry in Unraveling Seasonality” (PIs: Peeters, F., Ganssen, G.), pending.

0628394

http://www.soest.hawaii.edu/oceanography/faculty_html/Zeebe2/CO2_System

collaborative research; the dynamics of ...silab/biocomplex/proposal_short.pdfthe strategy will...

Documents