2004-White-A Chemostratigraphic and Geochemical Facies Analysis of Strata.pdf

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A Chemostrat igraphic and Geochemical Facies Analysis of StrataDeposited in an Eocene Australo-Antarctic Seaway:Is Cyclici ty Evidence for Glacioeustasy?

T i m o t h y S . W h i t eEMS Environment Institute, The Pennsylvania State University, University Park, PennsylvaniaIn t h i s p ap er , geo ch e mi ca l f ac ie s corre lat ion s f rom O ce an Dr i l l in g Pr ogram

S i t e s 1 1 6 8 , 1 1 7 0 , 1 1 7 1 a n d 1 1 7 2 a r e p r e s e n t e d . T h e s e c o r r e l a ti o n s , i n t e g r a te d w i t hsh ip b oar d - d et erm in ed l i t h o lo g ic an d b ios t rat igrap h ic in f ormat ion , d e f in e s t rat igrap h ic s eq u e n ce s . Th e seq u en c es are t yp ica l ly ch aract er ized as coarsen in gu p ward : c lays t on e an d c layey s i l t s t on e over la in b y s i l t s t on e , an d in some casessan d y s i l t s t on e an d san d . S eq u en ce b ou n d ar ies are mark ed b y coarse n in g u p wa rds e q u e n c e t o p s , a s w e l l a s g e o c h e m i c a l l y - d e f i n e d f l o o d i n g s u r f a c e s c h a r a c t e r iz e dp r imar i ly b y p e ak s in t o ta l su l fu r con t en t , an d secon d ar i ly b y p eak s in to t a l org an iccarb on an d carb on at e con t en t . Th e seq u en ce s t ack in g p at t ern s can b es t b ee x p l a i n e d b y s e a - l e v e l c y c l e s , i n d i c a ti n g t ha t e a r l y t o m i d d l e E o c e n e g l a c i o e u s t a s ym a y h a v e a f f e c t e d th e A u s t r a l o - A n t a r c t ic S e a w a y . T h i s c o n c l u s i o n s u p p o rt s s o m ec o n c e p t u a l m o d e l s , bu t o p p o s e s t h e m o d e l i n w h i c h A n t a r c ti c c o n t i n e n t a l - s c a l eg l a c i a t i o n , a n d h e n c e g l a c i o e u s t a s y , d i d n o t d e v e l o p u n t il E o c e n e / O l i g o c e n eb ou n d ary in i t ia t ion of t h e An t arc t ic Circ u mp olar Cu rren t. Th e ch em os t rat igrap h iccorre lat ion s a l so p rovid e s t rat igrap h ic re f in emen t o f cr i t i ca l ch ron os t rat igrap h icb o u n d a r i e s i n c l u d in g t h e E o c e n e / O l i g o c e n e b o u n d a r y a t S it e 1 1 7 1 , t h e l a t e / m i d d l eEo cen e b ou n d ary at S i t e 1171 ( an d 1168 ?) , t h e mid d le /ear ly Eo cen e b ou n d ary atS i t e 1 1 7 0 , a n d t h e P a l e o c e n e / E o c e n e b o u n d a r y a t S i t e s 1 1 7 1 a n d 1 1 7 2 .

I N T R O D U C T I O NRobust second-order, litho- and bio-stratigraphic correla

tions have been established between the various cored intervals obtained during Ocean Drilling Program (ODP) L eg 189to the western Tasmanian margin, the East Tasman Plateauand the South Tasman Rise (STR) [e.g., Stickleyet al, 2 0 0 4 ; Shipboard Scientific Party, 2 0 0 1 , L e gSummary]. In general, Paleogene siliciclastic sediments areoverlain by upper Eocene glauconitic siliciclastics, andfinally by lowermost Oligocene pelagic carbonates. This

The Cenozoic Southern Ocean: Tectonics, Sedimentation, andClimate Change Between Australia and AntarcticaGeophysical Monograph Series 151Copyright 2004 by the American Geophysical Union.10.1029/151GM10

sediment package is interpreted to record three stages odepos ition: 1) Paleog ene shelf al and deltaic sedimen tationunder mostly poorly-ventilated bottom waters of shallowmarine gulfs formed during increased spreading, and strikeslip activity, between Australia and Antarctica; 2) late Eoceneglauconite-bearing siliciclastic sedimentation associated withstrong bottom-current winnowing at shelf water depthsand, 3) early Oligocene carbonate sedimentation accompanied by increased bottom-water ventilation once the twcontinents had separated and the shelf had foundered intodeep water [Shipboard Scientific Party, 2001] .

One major goal of ODP Leg 189 was to obtain a sedimentary record of the inception of the AntarctiCircumpolar Current (ACC), and this goal was obtainedThe importance of the inception of the ACC is that it habeen regarded as leading to continental-scale glaciation oAntarctica [Kennett, 1977] .H owev er, other data suggest tha

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154 EOCE NE CHEMOSTRATIGRAPHY, ODP LEG 189

Antarct ic glaciat ion, or some other cont inental-scaleglaciation capable of affecting sea level, must have existedduring the middle to perhaps early Eocene prior to initiationof the ACC [e.g. Browning et al, 1996] . This paper demonstrates that early through late Eocene sequence boundaries,at ODP Sites 1168, 1170, 1171 and 1172, point to Eoceneglacioeustasy.

The analysis presented here follows the so-called holisticapproach [Arthur and Dean, 1991 ] by integrating shipboardlithologic descriptions and geochemical data with a shore-based geochemical data set . Some chronostratigraphic control is provided by biostratigraphy [Stickley et al, 2004] .The analysis resulted in a chemostratigraphic synthesis ofthe Eocene depositional units encountered during the leg,and provides a stratigraphic framework for subsequent studies to understand the Eocene evolution of climate, oceanography, and depositional environments in the SouthernOcean. The basic approach is discussed under the sectionsentit led Chem ostratigraphic profiling and Holisticchemostratigraphic approach to the Eocene strata .

E O C E N E E A R T HHistorically, ice-free conditions are considered to have

existed throughout much of the Paleocene and EoceneEpochs, while continental ice sheets capable of initiatingeustatic sea-level change have existed during much of theOligocene to Recent [Shackleton and Kennett, 1975; Milleret al, 1987;Zachos et al, 2001] . This view of glacial historyis supported by a number of proxy- and model-based observations. For example, the early Eocen e has been characterized asone of the warmest episodes of the Cenozoic with globally-averaged surface temperatures 2-4C greater than today, andice-free poles inhabited by mammals, reptiles and deciduousforests [Barron, 1987; Rea et al, 1990; Sloan and Barron,1990; Sloan et al, 1992; Greenwood and Wing, 1995].Paradoxically, early Eocene tropical sea surface temperatureshave been interpreted by some as the same or slightly coolerthan today [Shackleton and Boersma, 1981] . However, morerecent analyses of middle Eocene foraminifers indicate tropical sea surface temperatures were 28-32C, values that aremore consistent with a globally warm Earth [Pearson et al,2001] , and support coupled ocean-atmosphere general circulation models that predict tropical sea surface temperatures3-5C higher than today [Huber and Sloan, 2001] .

The initiation of Antarctic continental glaciation is generally considered to have begun as a result of the opening ofSouthern Ocean gateways that allowed for the developmentof the ACC [Kennett, 1977] . The initial results of Leg 189indicate that the opening of the Tasmanian Gateway occurredapproximately at the Eocene/O ligocen e boundary [-33.7Ma;Exon, Kennett, M alone et al, 2001] , thus providing a date

for initiation of the ACC, progressive thermal isolation ofAntarctica, and subsequent Antarctic glaciation and globacooling that is compatible with some reconstructions oTertiary glacial history [e.g. Kennett, 1977].

However, a number of reconstructions indicate thaAntarctic glaciation may h ave beg un prior to the opening othe Tasmanian Gateway. For example, early/middle Eoceneboundary (-48.5 Ma) t ills from the South Shetland IslandsAntarctica [Birkenmajer, 1988] , although possibly attributable to alpine glaciation, suggest the presence of older-thanthe-ACC glacial ice in Antarctica. Similarly, isolated graveand terrigenous sand grains in pelagic oozes and chalks othe Maud Rise and Kerguelen Plateau indicate that ice rafting had commenced during the middle Eocene [Ehrmanand Mackensen, 1992] . Browning et al, [1996] , using comparisons of stratal stacking patterns and foraminiferal oxygen-isotopic studies of New Jersey margin Eocene strataposited that glacioeustasy had affected sedimentation theras early as the middle Eocene. Furthermore, Diester-Haasand Zahn [199 6] used oxy gen-iso topic analyses of benthforaminifera from the Weddell Sea to infer a middle/latEo cen e boundary (37 Ma ) proto-polar front in thSouthern Ocean that formed during the initial stages oAntarctic ice sheet growth. Significantly, recent coupledatmosphere-ocean-ice sheet-sediment models demonstratthat atmospheric C 0 2 concentration may have played greater role in the inception and expansion of Antarctiglacial ice, than the opening of Southern Ocean gateway[DeConto and Pollard, 2003] . So, although the t iming oTasmanian Gateway opening, as determined by ODP Leg189, supports the model for latest Eocene/Oligocene expansion of Antarctic glacial ice, continental glaciers capable ocausing measurable changes in eustatic sea level and paleoceanography, and therefore global climate, may ha ve e xistedprior to inception of the ACC .

EO CENE S TRATAL S TACK ING PATTERNS FRO MA U S T R A L I A - A N T A R C T I C A A N D B E Y O N D

Not surprisingly, Eocene to lower Oligocene generalizedlithologic and stratal stacking patterns observed from theoutcrop belt of the southern Australia margin [Gallagheand Holdgate, 20 00] correspond to the patterns observeduring ODP Leg 189. For example, in the Otway Basinlower Eocene siliciclastic paralic facies are locally overlainby middle Eocene siliciclastic marine units, then upperEocene ferruginous and glauconitic (mostly shelfal) siliciclastics once subjected to winnowing and sorting by wavaction, all capped by lower Oligocene mainly carbonatdeposits. These stratigraphic patterns are also characteristicof the region from the Great Australian Bight to the RossSea margin [Exon, Kennett, M alone etal, 2001] , suggestin


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that the basinal histories in the Australo-Antarctic Seawaywer e genera lly compara ble. The patterns of onshore-offshore similarity include the distribution of hiatuses: onshore,the Eocene/Oligocene boundary is marked by an -100,000year hiatus [Gallagher and Holdgate, 2000] , while offshorethe boundary is unconformable at ODP Sites 1170, 1171,and 1172 [Exon, Kennett, Malone et al, 2001] ; a major hiatus exists at the late/middle Eocene boundary at Site 1171[Exon, Kennett, Malone et al., 2001] , and in the outcrop belt[Gallagher and Holdgate, 2000] ; and finally, an onshorehiatus representing up to 2 m.y. in the middle Eocene[Gallagher and Holdgate, 2000] , may be coeval with, orrepresent amalgamation of, any of the various middleEocene hiatuses [Exon, Kennett, Malone et al, 2001] recognized at ODP Sites 1170, 1171 and 1172.

A major middle to upper Eoc ene unconform ity and a probable upper Eocene hiatus appear to be present throughout theGulf of M exic o and North Atlantic basins; the older featurehas been attributed to global cooling and a sea-level low-stand, while the younger may mark the onset of a globallycooler paleocl imate [Keller, 1985] . On the New Jersey margin, the Eocene/Oligocene and late/middle Eocene boundaries are each marked by at least one hiatus [Milleret ai, 1994 , 1996] , while at least three major hiatuses wererecognized within middle Eocene strata [Browning et al.,1996] . Interestingly, of the fourteen sequences predicted bythe global sea-level curve of Haq et al. [1987 ] , nine of thesequences were resolved in lower-middle Eocene strata ofthe New Jersey margin, whereas the remaining five unrecognized sequences were regarded as combined with othersequences. Carbon and oxygen isotopic records from plank-tonic and benthic foraminifera led to the view that theseNew Jersey records represented the in it iat ion ofglacioeustasy by at least the middle Eocene [43-42 Ma;Browning et al., 1996] .

The very general correspondence between the NorthAmerican record and the observations from Australia suggest that planetary-scale processes may have affected second- to third-order sea-level change during the Eocene.Therefore, since glacioeu stasy is kn own to cau se third-ordersea-level change [Vail et al., 1977] , it seems reasonable toconsider whether or not ice-volume changes may have beenoperational in the early to middle E ocen e A ustralo-AntarcticSeaway, i.e. , prior to initiation of the ACC. To accomplishthis, the remainder of this paper focuses on creating high-resolution chemostratigraphic correlations, the definition ofthird-order sequences, and the resulting interpretations.

CH EMO S TRATIG RAPH IC PRO FILINGDetailed geochemical profiles provide one way of esta

blishing basin-scale correlations by recognizing similar

patterns in different localit ies. A chemostratigraphiapproach can be particularly useful in f ine-grainedhemipelagic strata often devoid of noticeable lithologichanges. For example, chemostratigraphic profiles may bconstructed using total organic carbon (TOC) content, alsallowing an assessment of the dynamics of organic-mattesedimentation. In marine facies, low (


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156 EOCEN E CHEMOSTRATIGRAPHY, ODP LEG 189

siliciclastic-carbonate sequence stratigraphy the readershould refer to the vast literature, for example, VanWaggon er et al. [1990] andSchlager [1992] .

Reco gnition of a maxim um flooding surface can be particularly useful in sequence stratigraphic correlation since itrepresents a virtually synchronous surface that typically canbe traced from shoreline to continental slope deposits[Mancini and Tew, 1997] . In this study, relative increases in% T S, % C a C 0 3 , and Hydrogen Index (HI) are all geochemical features considered to be potentially indicative of flooding surfaces. In strata characterized by the presence o f marineorganic matter, relative increases in total organic carbon content (%TOC) can be associated with flooding surfaces.Further, low Th/U values indicative of suboxic to anoxicseafloor conditions may also be present at flooding surfaces.

A variety of lithologic characteristics also provide clues forthe recognition of flooding surfaces. In this study, the presence of glauconite, often considered to have formed duringcondensation associated with relative sea-level rise, e.g.Hesselbo and Huggett, 20 01 , and in one sequence, shell lags,suggestive of a condensed transgressive lag or erosionalravinement surface, e.g. Kidwell, 1989 , were most useful.

A critical component in recognizing sequence boundariesis observations of a basinward shift in facies that is demonstrably significant over a broad area [Van Wagon ner et al.1990] . One manifestation of a sequence boundary that maybe observed in geochemical data is elevated values of HI,%TS, and/or %CaC0 3 , representing a marine flooding surface, immediately overlain up-section by progressivelyincreasing %TOC values characterized as terrestrial organicmatter ( low HI). The organic matter trends may be accompanied by elevated Th/K values possibly indicative ofincreased inputs of continentally derived kaolinite, with co ncomitant ly decreasing %CaC0 3 . In wholly marine strata, thebasinward shift in facies is more likely manifest as decreasing %TOC values, characterized by low HI values indicative of relative increases in terrestrial organic detrital inputs.

In this study, the top of coarsening upward sequencesas determined from the detailed lithologic logs available inExon, Kennett, M alone et ai, [200 1] proved useful insequence boundary recognition. Most of the coarseningupward tops are overlain by one or more geochemical parameters interpreted as representing marine flooding surfaces.Other useful lithologic observations included significantchanges in hardness, lithology, bioturbation, and mineralogy, and paleontologically determined hiatuses, all derivedfrom Exon, Kenn ett, M alone et al. [2001] .

L A B O R A T O R Y M E T H O D O L O G YFor this study, a new total sulfur data set was integrated with

other shipboard geoch emic al data sets to create high-resolution

chemostratigraphic correlations between ODP Sites 11681170, 1171 and 1172. All of the shipboard data are availablein Exon, K ennett, M alone et ai, [2001 ] . Shore-based totasulfur (%TS) analyses were determined using a Leco SC132 781-400 Sulfur System. The Leco Sulfur System usesa sulfur infrared cel l to detect total sulfur, in this cas e in bulksediments. During the combustion process, sulfur is oxidized to sulfur dioxide that subsequently passes through aninfrared cell and absorbs infrared energy at a specificinfrared wa velength. A w aveleng th filter allows only the sulfur dioxide absorption spectrum to reach a detector. Threduction of infrared energy corresponds to that absorbed bythe sulfur dioxide, and the energy that reaches the detectocan be attributed to a certain concentration of sulfur dioxide(Leco Corporation, 1993).

Shipboard %TS data [Exon, Kennett, M alone et ai, 2001suggested that %TS values for this study wo uld likely rangfrom ~0 to 2%, so the Leco Sulfur System was calibratedusing a 1%TS standard with a rating of + / - 1 % . Samples thaexhibited %TS values >2 were rerun after recalibrating thsystem using a 3%TS standard with a rating of +1-2%. Th%TS values presented in Table 1 are the average of at leastwo replicates for each sampled horizon.

For this study, %TS is assumed to be equivalent to pyritisulfur since no sulfate minerals were identified in the coredsediments [Exon, Kennett, Malone etal, 2001] . Furthermora petrographic evaluation of sedimentary pyrite, usintwenty thin sections that span the study intervals, verifiedthe assumption that all of the pyritic sulfur is syngenetic, annot influenced by later stage diagenesis (see further discussion under R esults) .

DATA ANALYS ISThe aforementioned concepts of holistic chemostrati

graphy were applied to a f looding surface and sequencboundary evaluation of Eocene strata at Sites 1168, 11701171 and 1172. Subsequently the effort shifted to visual pattern matching between sites. In many cases, pattern matching was straightforward, while in some instances severaiterations were necessary before an acceptable correlationwas found. These correlations were then compared to thebiostratigraphic age data of Stickley et al. [2004] to ensurconsistency with the best age control available for thstrata.

Once sequence boundaries had been identif ied and correlated among the four sites, the geochemical facies in eachsequence was described. Descriptions at each site were subsequently compared to overlying and underlying sequencdescriptions to understand the marine or terrestrial variations, or stacking patterns, at a site.


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R E S U L T SThe results of shore-based total sulfur analyses are pre

sented in Table 1, and both shipboard and shore-based totalsulfur value s are show n in Fig ure 1. Th e shipboa rd trend swere ver if ied by the shore-based work , but much greater

detai l was provided by the shore-based results , and sevenhigh-amplitude and numerous smaller ampli tude %TS hor izons first appeared in the shore-based values.

Petrographic e xaminations indicate that al l of the pyr i te itwenty thin-sections consists of varying amounts of: a) smaldomains of finely disseminated euhedral to anhedral crystal

Table 1. Shore-based Total Sulfur Analyses for Eocene Strata, ODP Leg 189.Site 1168 Site 1170 Site 1171 Site 1172

Depth (mbsf) %Total S Depth (mbsf) %Total S Depth (mbsf) %Total S Depth (mbsf) %Total S244.1 0.01 463.02 0.03 266.69 0 350.9 0.02247.12 0.02 472.54 0.01 269.6 0.04 354.6 0.04250.21 0.07 477.33 0.23 276.21 1.21 354.6 0.06253.72 0.04 482.22 0.74 279.21 1.21 356.1 0.04256.64 0.04 485.22 0.62 285.8 1.02 356.1 0.03259.64 0.16 488.22 1.23 293.8 0.03 357.6 0.02263.32 0.01 491.82 0.98 300.4 0.57 357.6 0.1266.32 0.92 494.82 1.05 305.42 0.62 359.1 0.19269.32 0.83 502.2 0.96 314.71 1.14 359.1 0.06272.92 0.02 505.92 1.54 317.7 0.49 360.6 0.06275.92 0 511.02 0.74 324.3 0.76 360.6 0.41278.92 0 513.3 0.43 327.3 0.7 362.1 0.22282.52 0 517.02 0.25 372.4 1.86 362.1 0.63285.52 0.05 520.52 0.15 382 1.93 362.8 0.49288.52 0.08 523.52 0.73 391.61 1.1 364.2 0.75292.12 0.01 530.09 0.9 394.6 0.81 365.8 0.67295.12 0.24 533.08 0.49 410.82 0.6 367.2 0.65298.12 0.13 539.82 2.1 413.82 0.77 368.8 0.36301.42 0.24 542.82 2.37 416.88 5.02 370.2 0.56304.42 0.05 545.82 6.5 420.4 1.37 373.8 0.5307.42 0.11 549.42 2.53 423.4 1.78 376.8 0.9310.72 0.1 552.42 1.97 426.4 2.4 379.8 0.83313.72 0.01 555.42 2.45 439.6 1.52 383.4 0.38316.72 0.02 559.02 2.52 442.6 1.02 386.4 0.52320.32 0.05 562.51 2.55 445.61 0.96 389.4 0.39323.32 0.14 568.55 2.47 449.2 1.6 393 0.27326.32 2.11 571.62 2.16 452.2 1.22 396 0.45329.92 4.54 574.62 1.28 458.8 1.53 399 0.34332.92 0.76 578.22 2.3 461.8 1.75 402.6 0.53335.92 0.56 581.22 2.34 468.5 2.42 405.6 0.34339.49 0.03 584.18 1.68 471.5 2.08 408.6 0.44342.07 0.05 587.48 0.09 474.5 2 412.2 0.48349.12 0.01 589.74 1.62 478 .1 1.86 415.2 0.36352.12 0.12 592.74 1.31 481 .1 1.88 418.2 0.35355.12 0.08 597.58 1.78 484.1 1.83 421.8 0.76358.72 0.32 600.43 1.31 487.7 1.91 424.8 0.56361.72 0.02 603.39 1.6 490.7 1.98 427.8 0.48364.72 0.16 607.02 2.04 493.7 1.59 431.4 0.57368.32 0 610.02 1.63 497.31 2.04 434.4 0.3371.32 0.12 613.02 1.7 500.31 1.11 437.4 0.27374.32 0.11 618.47 1.72 503.3 0.98 441 0.57378.12 0.12 621.47 1.45 507 0.5 444 0.7381.01 0.04 626.27 1.53 510 0.79 447 0.74


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Table 1 . (Continued).Site 1168 Site 1170 Site 1171 Site1172

Depth (mbsf) TotalS Depth (mbsf) TotalS Depth (mbsf) TotalS Depth (mbsf) TotalS384.08 0.71 629.36 1.66 513 0.98 450.6 1.71387.62 0.1 632.34 1.35 516.61 1.21 453.6 1.57390.62 0.37 636.07 1.26 519.41 1.25 456.6 1.44394.08 0.15 639.08 1.51 522.41 1.56 469.8 0.77397.22 6.53 641.96 1.32 526.21 1.14 472.8 0.65400.22 0.61 645.62 1.38 527.71 0.81 479.4 0.7403.22 0.21 648.62 1.32 530.71 0.9 482.4 0.91406.82 0.19 651.62 1.55 535.81 0.74 485.4 1.03409.88 0.25 655.32 1.11 541.82 0.51 492 0.67412.85 0.16 658.32 1.35 545.51 0.76 495 0.55416.42 0.32 661.32 1.46 548.5 1.15 498.6 0.62419.42 0.31 664.92 1.33 551.5 0.67 501.6 0.52422.42 0.32 667.92 1.14 555.11 0.32 507 0.39425.86 0.36 670.92 1.22 558.11 0.67 510 0.38429.02 0.24 674.52 1.3 561.13 0.55 516.6 0.96432.14 0.19 677.34 1.56 564.71 0.87 519.6 0.68435.62 0.2 679.86 1.87 567.71 0.37 526.2 0.5438.62 0.12 684.22 1.06 570.7 0.27 529.2 0.72441.62 0.14 687.08 1.58 574.31 0.25 532.2 0.27445.22 0.21 690.02 1.8 577.31 0.37 535.8 0.6448.22 0.41 693.92 1.51 580.31 0.84 538.8 0.38451.22 0.16 696.77 1.81 583.91 0.57 541.8 0.66454.82 0.12 699.77 1.86 586.91 0.82 545.4 0.44457.82 0.17 703.52 2.09 589.91 0.87 548.4 0.35460.82 0.04 706.52 1.97 593.61 1.12 551.4 0.18464.42 0.06 709.52 1.63 596.62 0.61 555.1 0.38467.42 0.09 713.12 1.8 599.61 0.79 558.1 0.35470.42 0.24 716.12 1.73 603.21 0.47 561.1 0.23474.02 0.21 719.12 1.83 606.21 0.9 564.7 0.47477.34 0.12 722.72 1.81 609.21 0.65 567.7 0.26480.33 0.13 725.72 2.2 612.81 0.86 570.7 0.16483.62 0.26 728.72 1.86 615.8 0.82 574.3 0.15486.62 0.07 732.32 1.69 618.8 0.71 577.3 0.17489.62 0.23 735.32 1.62 622.4 0.61 580.3 0.11493.22 0.19 738.32 1.39 625.4 0.65 583.9 0.08496.22 0.08 741.92 1.65 628.4 0.97 586.9 0.28499.22 0.37 744.92 1.63 632.01 1.13 589.9 0.49502.82 0.64 747.92 1.36 635.01 1.04 593.5 0.86506.06 0.37 751.52 1.21 638.01 0.55 596.5 0.61508.82 0.17 754.52 1.42 641.62 0.38 599.5 1.38512.42 0.19 757.52 1.57 644.62 0.18 603.1 1.4515.42 0.05 761.22 1.34 647.61 0.34 606.1 0.94518.52 0.11 764.22 1.33 651.32 0.07 609.1 0.29522.12 0.95 767.22 1.2 654.32 0.26 612.7 0.31525.12 0.3 770.82 1.04 657.32 0.34 615.7 0.62528.12 0.17 773.8 0.88 660.92 0.33 622.3 1.27531.82 1.1 776.8 1.1 670.52 0.24 625.3 2.38534.82 0.23 673.52 0.28 628.3 1.07537.82 0.45 676.52 0.22 631.9 2.59541.42 0.46 680.22 0.24 634.9 1.55544.42 1.51 681.94 0.21 637.9 0.96


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Table 1 . (Continued).Site 1168 Site 1170 Site 1171 Site 1172

Depth (mbsf) TotalS Depth (mbsf) TotalS Depth (mbsf) TotalS547.42 0.79 684.93 0.19551.12 1.25 689.91 0.53554.12 1.11 692.9 0.88557.29 0.73 695.9 0.24560.81 0.75 701.52 0.17563.82 6 704.53 0.14566.83 0.75 709.1 0.84570.32 0.28 712.1 0.43573.32 0.47 715.1 0.27576.32 1.01 718.7 0.13579.32 0.63 721.7 0.12582.92 0.35 724.7 0.61585.92 0.2 728.31 0.42590.02 0.22 731.3 0.92592.52 0.46 734.3 0.51595.65 0.29 737.9 1.29598.95 1.03 740.9 1.08602.15 0.56 743.9 0.88605.21 0.38 747.51 0.42608.72 0.48 750.5 0.46611.63 1.38 753.5 0.35614.57 0.21 757.1 0.44618.32 0.65 760.1 0.21621.32 1.29 763.1 0.8624.32 0.16 766.7 0.47627.91 0.34 769.7 0.37630.64 0.3 776.31 0.53633.27 0.34 779.3 0.65637.34 0.1 785.9 0.49640.52 0.62 788.9 0.7643.43 0.83 791.9 1.07647.15 0.8 795.5 0.4650.12 0.45 798.5 0.53653.06 5.3 801.51 0.3656.82 0.19 805.1 0.75659.82 0.39 808.1 0.96666.52 0.19 811.1 1.7669.52 0.13 814.7 1.06672.52 0.8 817.7 0.95676.09 0.38 820.7 0.92679.1 0.32 824.3 0.79685.72 0.41 827.3 0.82688.7 0.55 830.3 1695.08 0.19 833.9 0.97698.42 0.3 836.9 0.93701.4 0.63 839.9 1.02705.02 0.5 843.5 1.27708.02 2.59 846.5 1.55711.02 0.69 849.5 1.02714.62 0.69 853.1 1.28717.62 0.49 856.1 0.81

Depth (mbsf) TotalS641.5644.5651.1

0.860.990.81


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Table1. (Continued).

Depth (mbsf) TotalS Depth (mbsf) TotalS Depth (mbsf) TotalS Depth (mbsf) TotalS720.62 1.4 859.1 1.4724.32 0.83 862.7 0.96727.32 0.29 865.7 1.11730.32 0.66 868.7 0.99735.87 0.65 872.3 0.99739 0.7 875.3 0.97743.43 1.9 878.3 1.06746.58 0.84 883.2 0.75749.81 1.31 884.7 0.76753.12 1.32 888.7 0.79756.12 1.1 891.3 0.55759.12 1.54 894.3 0.74762.72 1.2 897.3 0.94765.61 0.77 900.9 1768.2 0.77 906.9 1.33772.04 1.62 910 .5 1.71775.32 0.87 912.01 1.16778.32 0.86 913.5 1.13781.64 2.15 920.2 1.69784.8 1.73 923.2 1.95787.9 1.79 926.2 1.83791.52 1.17 929.9 1.45794.82 1.58 932.9 1.4797.56 2.07 935.9 1.39801.06 1.8 949.21 1.34804.08 2.01 952.2 1.45807.02 1.98810.62 1.56813.62 1.43816.62 1.43820.22 1.59823.22 1.62826.21 0.93829.8 1.61832.82 0.92835.8 0.38839.42 0.28842.42 0.13845.42 1.74849.02 1.12856.12 1.13859.12 1.04862.12 0.92862.11 1.01865.14 0.57868.12 0.99868.28 0.8871.22 1.53874.2 0.8874.22 1.17877.05 1.86878 0.85

Site 1168 Site 1170 Site 1171 Site1172


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%Total S %C aC0 3

%T0C HydrogenIndexFigure 2. Depth profiles of %CaC03 , %Total Organic Carbon, %Total Sulfur, and Hydrogen Index for upper Eocene strata encountered aODP Sites 1168, 1170, 1171 and 1172. Note that the O/E sym bol marks the biostratigraphically de termined Eoce ne/Oligocene boundary (seeExon, Kennett, Malone et al, 2001), and SB designates sequence boun daries determined in this study (also marked by light gray linesVertical arrows mark coarsening upward sequence tops.sequences. The overall duplication of relative sequencestacking profiles betw een the Leg 189 sites suggests that themethod is reasonably reliable.

D I S C U S S I O NA typical Eocene sequence in the offshore Tasmanian

region is characterized by claystone and clayey siltstoneoverlain by siltstone, and in some cases sandy siltstone andsand. Most of the Eocene sequences contain relatively lowtotal organic carbon and carbonate contents, although several sequences display slightly elevated values; total sulfurcontents are mostly - 1 % . Sequence boundaries are markedby coarsening upward sequence tops, as well as geochemi-cally defined flooding surfaces characterized primarily bypeaks in total sulfur content, and secondarily by total organiccarbon and carbonate peaks.

There are weaknesses in the resolution of upper Eocenesequences between Sites 1168, 1170, 1171 and 1172.Sequences (2 and 3) recognized at Site 1168 were undefinedat Sites 1170, 1171 and 1 172. Furthermore, a basal sequenceboundary at Site 1168 (SB6) has been correlated to the

uppermost middle Eocene sequence boundary at Sites 11701171 and 1172. The Site 1168 age model only tentativelyindicates the presence of late Middle Eocene strata in thhole [Stickley et al., 2004] , so a second upper Eocensequence m ay exist at Site 1168 that has not been recognizedat Sites 1170, 1171 and 1172.

The stratigraphic interval near the Paleocene/Eocenboundary at Sites 1171 and 1172 is noteworthy with regardto sequence resolution because of the presence of a prominent double sulfur peak (Figure 5). The double sulfur peakcan be interpreted as a marine flooding surface overlain by maximum flooding surface, or as two condensed intervalseparated by a sequence boundary. I located geochemicallydefined seq uence boundary SB 19 betwee n the two sulfupeaks, based on the presence o f a distinct lithologic surfacthat equates to the trough of the sulfur peak doublet [-91 3mbsf in Core 1171D-71R-2; Exon, Kennett, Malone et a2001 ] . This corresponds to the biostratigraphically-defineboundary pick for Site 1171 [~910 mbsf;Stickley et al, 2004However, the boundary at Site 1172 [-620 mbsf;Rohl et athis volume] is located above the double sulfur peak andSB19 . Nevertheless, on the basis of these observations


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WHITE 16

Site 1170 Si te 1171Figure 3.Depth profiles of %CaC03 , %Total Organic Carbon, and %Total Sulfur for upper middle Eocene strata encountered at ODP Sites1170,1171 and 1172. Note that SB designates sequence boundaries determ ined in this study (light gray lines), and vertical arrows mark coarsening upward sequence tops. SB8 was inferred at Site 1172 (dotted line). Also note that limestones w ere noted at >630 mbsf at Site 1170 and-370 to 375 mbsf at Site 1171 in lithologic descriptions in Exon, Kennett, Malone et al.(2001) and were not sampled for carbonate analysis

I interpret the Paleocene /Eoce ne boundary at Site 1172 to liewithin the double sulfur peak, i.e. at -628 mbsf.

In middle Eocene strata, two sequences (9A and 12) weredefined sole ly on geo chem ical data, and three (8, 13 and 14)were recognized in part on the observation of a coarseningupward sequence at only one site. These middle Eocene discrepancies perhaps introduce the most potential error in mycorrelations, because their stratigraphic locations also coincide with intervals of poor biostratigraphic control [seeStickley et al, 2004] . Nevertheless, the similarity in geochemical profiles and the total number of resolvablesequences between sites still generally provide a robustthird-order chemostratigraphic framework for these Eocenestrata.

The total number of lower through middle Eocenesequences (sixteen) identified in this study equals the totalnumber predicted by the Haq et al [198 7] global coastalonlap profile, and their stacking patterns are similar. Discrepancies exist when counting and comparing purely earlyEocene (six), and purely middle Eocene (ten), sequencesfrom this study with the Haq et al. [1987] predictedsequenc es (Figure 6), but I consider this inconsistency to be

caused by the lack of an early/middle Eocene boundary onthe original Haq et al. [1987] curve.

Signif icant ly, the correspondence between sequencstacking patterns at Site 1172, the only Le g 189 site loca tedin the Eocene Pacific Ocean, and the other Leg 189 sites(Figure 6) suggests that whatever process controlled thdevelopment of accommodation space in the AustraloAntarctic Seaway was also operational in the nearby PacifiOcean basin. In addition, an overall correspondence existbetween hiatuses in New Jersey passive margin strata andthe sequence boundaries identified for the Leg 189 riftedmargin sites (Figure 6). Therefore, similar sequen ce stackinpatterns appear to have develo ped in disparate depositionabasins of differing structural style and paleolatitudinasetting.

Using the total number of sequences and the geochronological t ime scale of Berggren et al. [1995 ] , the averagduration for each sequence is: 1) early Eocene = 970,000years; 2) middle Eocene = 1 .2 m.y.; and 3) combined earlyand middle Eoc ene = 1 .1 m.y. The average age duration othe individual sequences, and the similarity between stratastacking patterns in disparate depositional basins and th


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i 1 1 1 10 1 2 3 4%T0C

Site 1170Figure 4.Depth profiles of %Total Organic Carbon and %Total Sulfur for lower middle Eocene strata encountered at ODP Sites 1170, 117and 1172. Note that SB designates sequence boundaries determined in this study (light gray lines), and the vertical arrows mark coarseningupward sequence tops.SB 14was inferred at Site 1170 (dotted line). Also note that the middle/early Eocene boundary is shown as a blacdashed line.

global curve, demonstrate that planetary-scale processecapable of affecting relative sea level on third-order timescales were operating during the early to middle Eocene.

While various processes of subsidence and sediment supply are known to affect the development of accommodationspace, or relative sea level, only variations in glacioeustasyand mid-ocean ridge spreading rates are capable of affectingsea level driven patterns of sedimentation on a global scaleWhile mid-ocean ridge spreading rates appear to vary onsecond-order time scales [Pitman, 1978] , only glacioeustasis known to produce repetit ive or cyclic variations capableof effecting global change on third-order time scales [Vaetal, 1977; Vail and Haq, 1988].

Figure 5 . Depth profiles of %Total Organic Carbon and %TotaSulfur for lower Eocene strata encountered at ODP Sites 1171 and1172. Note that SB designates sequence boundaries determined ithis study (light gray lines), and the vertical arrows mark coarsening upward sequence tops. The Paleocene/Eocene boundary as designated for Site 1172[Ro hl et al, this volume] and for Site 117[ tickleyet al, 2004] is shown as a black dashedline;note myprerence for a stratigraphic pick corresponding to geochemicallydefined sequence boundary SB19.

%Total S0 1 2i u

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WHITE 16

Figure 6. Sequence stacking patterns for Eocene strata from ODP Sites 1168, 1170, 1171 and 1172, compared to the global eustatic curvofHaq etal.(1987). Large arrows on theHaq etal.(1987) curve designate sequence boundaries predicted by the curve and observed on thNew Jersey margin byBrowning et al. (1996), while large dashed arrows represent those sequence boundaries inferred to be amalgamatein hiatuses on the New Jersey margin(Browning et al, 1996), and small arrows designate those sequence boundaries predicted by theHaet al.(1987) curve but not identified in the New Je rsey margin study. The dashed line between Sequences 4 and 5 at Site 1168 acknowledgethat the recognition of late middle Eocene strata at the site is tentative.

C O N C L U S I O N S1. The integration of chemo stratigraphy with lithostrati-

graphic and biostratigraphic information providesa useful tool for defining sequence-scale correlations.Higher resolution data sets might even provide forhigher-resolution, i.e. parasequence-scale, correlat ions . By comparing robust b iostrat igraphically-defined boundaries with the geochemically definedsequence boundaries, boundaries can be inferredusing geochemistry in sequences at sites lacking biostratigraphic definition.

2. The stratigraphy of the Eo cene/O ligoc ene boundary atSite 1171 has been refined through recognition of theboundary's proximity to a %CaC0 3 increase and thetop of a coarsening upward se quence, features presentat the other Leg 189 sites.

3. The late/middle Eoc ene boundary has been tentativelyidentif ied at Site 1168 (-862 mbsf) and more accurately identif ied at Site 1171 (-293 mbsf) . The location of the middle/early Eocene boundary is inferredat Site 1170 (-775 mbsf) , by correlating coarseningupward sequences within similar chemostratigraphicprofiles.

4. The Paleo cene/E ocen e boundary is defined as existinwithin a prominent double %total sulfur peak at bothSites 1171 and 1172.

5. A typical Eoc ene sequence in the offshore Tasmanianregion contains relatively lo w total organic carbon andcarbonate, and total sulfur values of - 1 % . Thesegeochemical characteristics exist within coarseningupward sequences comprised mostly of claystonand clayey siltstone overlain by siltstone. Sequenceboundaries exist at the top of the coarseningupward sequences, and are primarily overlain byflooding surfaces characterized by peaks in totasulfur.

6. The early and middle Eoc ene sequences defined fromthe Australo-Antarctic Seaw ay and nearby P acifiOcean basins, their repetitive nature, and their apparent similarity to coeval sequences defined on the NewJersey margin and those predicted by the globacoastal onlap curves of Haq et al. [1987 ] , stronglsuggest sea- level cycles .

7. The most likely driving force of third-order sea-lev ecycles is glacioeustasy, so the evidence suggests it waoperational in the early to middle Eocene, prior tinitiation of the Antarctic Circumpolar Current.


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Acknowledgments. This research used samples and/or data provided by the Ocean Drilling Program (ODP). The ODPis sponsored by the U.S. National Science Foundationand participating countries under management of JointOceanographic Institutions, Inc. Funding for this research wasprovided by JOI/USSSP. C. Lernihan, P. Morath, and T. Whiteperformed shore-based total sulfur analyses. The author acknowledges helpful reviews by J. Kennard andP.DeDeckker, and especially those of editor and shipboard colleague N. Exon.

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Timothy S. White, EMS Environment Institute, 2217 EESBuilding, The Pennsylvania State University, University Park, PAUSA 16802; [email protected]
http://www-odp.tamu.-/http://www-odp.tamu.edu/publications/mailto:[email protected]:[email protected]://www-odp.tamu.edu/publications/http://www-odp.tamu.-/

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