revised composite depth scales and integration of iodp sites

Proc. IODP | Volume 320/321

Plike, H., Lyle, M., Nishi, H., Raffi, I., Gamage, K., Klaus, A., and the Expedition 320/321 ScientistsProceedings of the Integrated Ocean Drilling Program, Volume 320/321

Revised composite depth scales and integrationof IODP Sites U1331U1334 and ODP Sites 121812201

Thomas Westerhold,2 Ursula Rhl,2 Roy Wilkens,3 Heiko Plike,4 Mitch Lyle,5 Tom Dunkley Jones,6 Paul Bown,7 Ted Moore,8 Shin-ichi Kamikuri,9 Gary Acton,10 Christian Ohneiser,11 Yuhji Yamamoto,12

Carl Richter,13 Peter Fitch,6 Howie Scher,14 Diederik Liebrand,4 and the Expedition 320/321 Scientists15

Chapter contents

Abstract . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 1

Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . 1

Material and methods. . . . . . . . . . . . . . . . . . . . 2

Results and discussion . . . . . . . . . . . . . . . . . . . . 3

Summary . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 8

Acknowledgments. . . . . . . . . . . . . . . . . . . . . . . 8

References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 9

Figures . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 11

Tables. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 68

1Westerhold, T., Rhl, U., Wilkens, R., Plike, H., Lyle, M., Jones, T.D., Bown, P., Moore, T., Kamikuri, S., Acton, G., Ohneiser, C., Yamamoto, Y., Richter, C., Fitch, P., Scher, H., Liebrand, D., and the Expedition 320/321 Scientists, 2012. Revised composite depth scales and integration of IODP Sites U1331U1334 and ODP Sites 12181220. In Plike, H., Lyle, M., Nishi, H., Raffi, I., Gamage, K., Klaus, A., and the Expedition 320/321 Scientists, Proc. IODP, 320/321: Tokyo (Integrated Ocean Drilling Program Management International, Inc.). doi:10.2204/iodp.proc.320321.201.20122Center for Marine Environmental Sciences, University of Bremen, 28359 Germany. Correspondence author: [email protected] of Geophysics and Planetology, Univ. Hawaii, Honolulu HI 96822, USA.4School of Ocean & Earth Sci., Univ. Southampton S014 3ZH, UK.5Dept. of Oceanography, Texas A&M Univ., College Station TX 77845, USA.6Dept. of Earth Sci. and Engineering, Imperial College, London SW7 2AZ, UK.7 Dept. of Earth Sci., Univ. College, London WC1E 6BT, UK.8Dept. of Geological Sci., Univ. Michigan, Ann Arbor MI 48109, USA.9Univ. Tsukuba, Ibaraki 305-8572, Japan.10Dept. of Geology, Univ. California, Davis CA 95616, USA.11Geology Dept., Univ. Otago, Dunedin, NZ.12Marine and Core Research Center, Kochi Univ., Kochi 783-8502, Japan.13Dept. of Geology and Energy Institute, Univ. Louisiana, Lafayette LA 70504, USA.14Dept. of Earth and Ocean Sci., Univ. South Carolina, Columbia SC 29208, USA.15Expedition 320/321 Scientists addresses.

AbstractTo reconstruct the climate history of the equatorial Pacific, onemajor objective of the Pacific Equatorial Age Transect (PEAT) pro-gram is to compile a Cenozoic megasplice that integrates all avail-able bio-, chemo-, and magnetostratigraphic data including keyrecords from Ocean Drilling Program (ODP) Leg 199. In order todo so, extended postcruise refinements of the shipboard compos-ite depth scales and composite records are required. Here, we pres-ent a revised depth scale of Integrated Ocean Drilling Program(IODP) Expedition 320 Sites U1331, U1332, U1333, and U1334 aswell as Leg 199 Sites 1218, 1219, and 1220. The revised compositerecords were used to perform site-to-site correlation and integra-tion of Leg 199 and Expedition 320 sites. Based on this decimeter-scale correlation, a high-resolution integrated paleomagnetic, cal-careous nannofossil, and radiolarian stratigraphy for the equato-rial Pacific is established that covers the time from 20 to 40 Ma.This sedimentary compendium from the equatorial Pacific will bethe backbone for paleoceanographic reconstructions for the latePaleogene.

IntroductionIntegrated Ocean Drilling Program (IODP) Expedition 320/321(Pacific Equatorial Age Transect [PEAT]) cored eight sites (U1331U1338) during MarchJuly in 2009 (Fig. F1), recovering an agetransect at the Pacific paleoequatorial region from the time ofmaximum Cenozoic warmth in the Eocene, through initial majorglaciations in the Oligocene, to the present (see the Expedition320/321 summary chapter [Expedition 320/321 Scientists,2010a]; Lyle et al., 2009). The overall aim was to obtain continu-ous and well-preserved calcareous sediment sections for specifictime slices. Of major importance for the objectives of the PEATexpeditions is the assembly of an integrated bio-, chemo-, andmagnetostratigraphy at the Equator, hereafter referred to as theCenozoic megasplice.

In addition to those from the PEAT drill sites, key records for thebreakthrough in reconstructing the equatorial climate system ofthe late Eocene and Oligocene epochs were recovered duringOcean Drilling Program (ODP) Leg 199 (Lyle, Wilson, Janecek, etal., 2002), Site 1218 in particular (Fig. F1). Data from Site 1218 al-lowed astronomical calibration of the entire Oligocene (Wade and

doi:10.2204/iodp.proc.320321.201.2012

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T. Westerhold et al. Revised composite depth scales

Plike, 2004; Coxall et al., 2005; Plike et al., 2006),but the lack of carbonate in the uppermost Eocene atthis site made detailed time control much less ro-bust. Although the paleomagnetic record for thesetime intervals is of high quality (e.g., Lanci et al.,2004, 2005), global stratigraphic correlation is hin-dered by the lower mass accumulation rate, the ab-sence of a detailed isotope stratigraphy, and low-res-olution biostratigraphic control. In order to facilitatethe development of an integrated magneto- and bio-stratigraphic framework with a stable isotope stratig-raphy (necessary to enable global correlation), recov-ery of Eocene carbonate sediment with a high-quality magnetostratigraphy was targeted and suc-cessfully retrieved during Expedition 320.

During Expedition 320/321, at least three holes ateach site were cored and used to construct compositesections (see the Methods chapter [Expedition320/321 Scientists, 2010b]) in order to assure the re-covery of a complete stratigraphic section needed forthe assembly of the Cenozoic megasplice. As shownat ODP Leg 199 Sites 1218 and 1219 (Plike et al.,2005), extensive postcruise work is required to re-evaluate the shipboard composite depth stratigraphyand to provide a high-resolution revised meters com-posite depth (rmcd) scale. In addition, squeezing andstretching of cored intervals is necessary to compen-sate for depth distortion within individual cores(Hagelberg et al., 1992). To locate hiatuses and con-densed intervals, it is essential to do a site-to-site cor-relation using physical property data (Shackleton etal., 1995, 1999; Shackleton and Crowhurst, 1997; P-like et al., 2005; Westerhold and Rhl, 2006; Wester-hold et al., 2007, 2008). Subsequently, the correla-tion allows integration of any kind of data from onesite to another. A prerequisite for correlation is thatdecimeter-scale features in the sedimentary recordcan be correlated between holes and, if possible, be-tween sites.

Both Leg 199 and Expedition 320/321 magnetic sus-ceptibility and gamma ray attenuation (GRA) bulkdensity data can be correlated over large distances(>1000 km) across the Pacific seafloor (Plike et al.,2005, 2009). Physical property data, a proxy for cal-cium carbonate oscillations, at Sites U1331 andU1332 show a remarkable match with those fromODP Site 1220, a site with an excellent magneto-stratigraphy. Similarly, Sites U1333 and U1334 canbe correlated to Site 1218. Together, these sites pro-vide a coherent and integrated record for the equato-rial Pacific and enable study of sedimentation pat-terns and mass accumulation rates at orbitalresolution (Plike et al., 2009). Here, we present re-vised composite depth scales and revised splicedcomposite records for Expedition 320 Sites U1331,


U1332, U1333, and U1334 and Leg 199 Sites 1218,1219, and 1220 (Fig. F1). We also correlate and inte-grate Leg 199 and Expedition 320 physical propertyand stratigraphic data (including shipboard and re-vised biostratigraphic data) to define a completehigh-resolution time series for the middlelate Eocene,the entire Oligocene, and the early Miocene.

Material and methodsMagnetic susceptibility and GRA bulk density datafrom the Whole-Round Multisensor Logger and vir-tual geomagnetic pole (VGP) data calculated fromnatural remanent magnetization measurements in asuperconducting rock magnetometer collected at Ex-pedition 320 sites (see the Expedition 320/321summary chapter [Expedition 320/321 Scientists,2010a]) were used to refine depth offsets and to re-vise the shipboard composite section for SitesU1331, U1332, U1333, and U1334. Similarly, mag-netic susceptibility, GRA, and VGP data from Leg 199sites (Shipboard Scientific Party, 2002a, 2002b,2002c; Plike et al., 2005) were used to refine offsetsand splices at Sites 1218, 1219, and 1220. Refine-ments are also based on detailed high-resolution X-ray fluorescence (XRF) core scanning data (T. Wester-hold et al., unpubl. data; D. Liebrand et al., unpubl.data).

In 20062007 new classification and nomenclaturefor depth scale types were defined for IODP (seeIODP Depth Scales Terminology at www.iodp.org/program-policies/). The new methods and nomen-clature for calculating sample depth in a hole haschanged to be method specific to ensure that dataacquisition, mapping of scales, and construction ofcomposite scales and splices are unequivocal. Be-cause this study integrates data with different depthscale nomenclatures, we will describe in detail theclassifications and definitions of depth scales as usedhere for Leg 199 and Expedition 320. A much moredetailed definition of IODP depth scales used duringExpedition 320/321 is given in the Methods chap-ter (Expedition 320/321 Scientists, 2010b).

For this study, the most important depth is the coredepth below seafloor. This depth for each drilled coreis based on the actual length of the recovered coreand the drillers depth. It is defined as core depth be-low seafloor (CSF) for Expedition 320 and meters be-low seafloor (mbsf) for Leg 199. For consistency, wesuggest the use of mbsf (m CSF-A) for Expedition320 sites and mbsf for Leg 199 sites. Each point inthe core can now be located by adding the offset be-tween sample and core top to the drilling depth be-low seafloor (DSF) of the top of the core. To con-struct an initial continuous stratigraphic reference

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during the expedition, individual cores were depthshifted to maximize correlation between multipleadjacent holes and spliced together into a compositerecord. The new shipboard depth scale of the splicedsection is defined as the composite core depth belowseafloor (CCSF-A) for Expedition 320 and meterscomposite depth (mcd) for Leg 199. For consistencywe suggest the use of mcd (m CCSF-A) for Expedi-tion 320 and mcd for Leg 199. The addendum -Ato Expedition 320 cores to the CCSF denotes that in-dividual cores were shifted vertically without permit-ting expansion or contraction of the relative depthscale within any core.

Postcruise, we evaluated and revised the shipboardspliced composite section, establishing new core off-sets and refined the shipboard splice if necessary. In-tervals having significant disturbance or distortionwere not used for composite section construction.For construction of the revised records, we tried tomaintain those tie points given in the shipboardcomposite, where possible. Changes in the positionof tie points in the revised spliced record have beenhighlighted as bold letters in the splice tables of eachsite. The new refined depth scale is defined as the re-vised composite core depth below seafloor (revisedCCSF-A) for Expedition 320 and revised meters com-posite depth (rmcd) for Leg 199. For consistency wesuggest the use of rmcd (m revised CCSF-A) for Ex-pedition 320 and rmcd for Leg 199. Correction tothe rmcd depth scales of Leg 199 (Plike et al., 2005)are indicated by the corrected revised meters com-posite depth (corrected rmcd).

After assembling the new composite records, we ad-justed sedimentary sections outside the revised com-posite splice by squeezing and stretching to conformto the overall rmcd and rmcd (m revised CCSF-A)depth scales. To indicate this adjustment we addedthe prefix adjusted to the rmcd (m revised CCSF-A)and the corrected rmcd if necessary. This mappingprocedure allows data and samples located outsidethe spliced composite record to be placed in the newrevised composite depth scale at each site.

Finally, to integrate all available data we correlatedmagnetic susceptibility, GRA, and VGP data betweensites using the time series analysis program Analy-Series (Paillard et al., 1996). All tables and cleanedcomposite records of magnetic susceptibility andGRA data from Sites 1218, 1219, 1220, U1331,U1332, U1333, and U1334 and VGP data from Sites1218, 1219, and 1220 are available online in theWDC-MARE PANGAEA database (doi.pangaea.de/10.1594/PANGAEA.757215).

Composite core images were created as an additionalaid in site-to-site correlation using an approach mod-ified from that described in Wilkens et al. (2009). In-


dividual section images collected by the shipboardSection Half Imaging Logger (SHIL) during Expedi-tion 320 were initially assigned a core depth belowseafloor (CSF-A) depth range based on site coringdata. Section images were then mapped onto a singleimage of an entire core. Core image depth rangeswere then shifted by constant offsets to revisedCCSF-A depths based on the revised composite splicefor each site (e.g., Table T1). The final step in creat-ing a single image of the entire revised compositesection involved another mapping of depth intervalsfrom individual core images defined in site splice tables(e.g., Table T2) onto a composite image. As the reso-lution of the original SHIL images is on the order of50 m, each mapping step included image interpola-tion to a coarser scale250 m for the individualcore images and 1 mm for the composite image. Leg199 was the first use of an earlier version of the ship-board digital imaging system (DIS), and unfamiliar-ity with its operation led to inconsistent image expo-sures. Rather than attempt to correct the DIS images,we elected to use the digitized core photos availableonline at the IODP data website to construct com-posite site images. Images of each section of eachcore were digitally cut from the core images andthen combined as described above. As the corephoto images were much lower resolution (nomi-nally 2.5 mm), there was no need to downsize whilemapping. A slight unevenness in lighting of the corephotos (darker around the perimeter) produced anartifact when cutting and combining section imagesfrom digitized core photos into total core images.Apparent 1.5 m wavelength banding is particularlyevident in lighter colored sediments. An examplecan be seen in the composite image of Site 1218 be-tween 150 and 200 corrected rmcd.

Results and discussionRevised composite depth scales

Revised composite depth scales for Expedition 320 Sites U1331U1334Site U1331The shipboard splice for Site U1331 (see the SiteU1331 chapter [Expedition 320/321 Scientists,2010c]) was extensively revised (Figs. F2, F3, F4; TablesT1, T2, T3). The weak magnetic susceptibility andGRA signals in the siliceous ooze dominated the Eo-cene section of Site U1331, and frequent turbiditeshampered straightforward correlation. The exact po-sition and extent of turbidites is given in Table T4.The most problematic section is located around 3540 rmcd (m revised CCSF-A), where a turbidite oc-curs that shows different thicknesses in each coredhole. This could be due to coring disturbance at the

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top of the Hole U1331C or strong thickness varia-tions of the turbidite itself. We improved the spliceto 175 rmcd (m revised CCSF-A), resulting in agrowth factor of 1.12 (Fig. F4). Detailed correlationshowed that the shipboard declination record ofCores 320-U1331B-4H and 9H had to be flipped by180.

Site U1332

The shipboard splice for Site U1332 (see the SiteU1332 chapter [Expedition 320/321 Scientists,2010d]) had to be moderately revised (Figs. F5, F6,F7; Tables T5, T6, T7). Good VGP, magnetic suscepti-bility, and GRA data enable improvement of theshipboard splice to 141 m revised CCSF-A, resultingin a growth factor of 1.09 (Fig. F7). At around 83rmcd (m revised CCSF-A), a small gap in the data(Fig. F5) marks an uncertain tie point in the splice.However, detailed correlation to Sites U1331 and1220 suggests no major break at the base of ChronC15n in the composite record of Site U1332 (see Fig.F23, 50100 corrected rmcd).

Site U1333

The splice at Site U1333 (see the Site U1333 chap-ter [Expedition 320/321 Scientists, 2010e]) neededno change in the upper 48 rmcd (m revised CCSF-A)(Figs. F8, F9, F10; Tables T8, T9, T10). Pronouncedcycles in magnetic susceptibility and GRA data inthis interval allowed the construction of a robustshipboard splice. Correlation to Sites U1334 and1218 revealed an incorrect splice interval in the ship-board splice at Site U1333 around 48 rmcd (m re-vised CCSF-A). Readjustments of the splice reveal a2 m gap in the shipboard splice, which has beeneliminated by the new revised splice. Although themagnetic susceptibility signal is low between 82 and132 rmcd (m revised CCSF-A), small distinct peakscan be correlated and then verified by VGP data (Fig.F8, 50100 m). A minor change in the shipboardsplice is required at 126 rmcd (m revised CCSF-A).We then follow the tie points of the shipboard spliceto 151 rmcd (m revised CCSF-A) and maintain thecomplete uninterrupted splice to 156.44 rmcd (m re-vised CCSF-A). Below this depth, the splice can onlybe appended because there is no clear overlap be-tween cores from adjacent holes. Between 180 and200 rmcd (m revised CCSF-A), a composite recordcould be established mainly based on the VGP andmagnetic susceptibility data. The new splice has agrowth factor of 1.14 (Fig. F10).

Site U1334

At Site U1334 (see the Site U1334 chapter [Expedi-tion 320/321 Scientists, 2010f]), the shipboard splice


was verified to 210 rmcd (m revised CCSF-A) (Figs.F11, F12, F13; Tables T11, T12, T13). Because of geo-chemical alteration of the magnetic susceptibility re-cord, splicing was uncertain between 150 and 270rmcd (m revised CCSF-A). Through extensive usageof augmented magnetic susceptibility, GRA, VGP,core images, and especially postcruise XRF core scan-ning data (T. Westerhold et al., unpubl. data; D. Li-ebrand et al., unpubl. data), we secured a completecomposite record across the geochemically alteredinterval to 271 rmcd (m revised CCSF-A). Below thisdepth, we follow the shipboard splice with a majorchange in the interval from 297 to 306 rmcd (m re-vised CCSF-A). This change is important because itcovers the interval before the Eocene/Oligoceneboundary, which is characterized by strong fluctua-tions in calcium carbonate content (see the Expedi-tion 320/321 summary chapter [Expedition 320/321Scientists, 2010a]). Splicing this interval was a chal-lenge because extended core barrel drilling producedstrong biscuiting of the sediment. A complete splicewas assembled for Site U1334 to 341 rmcd (m revisedCCSF-A) with a growth factor of 1.16 (Fig. F13).

Revised composite depth scales for Leg 199 Sites 12181220Before we accomplished a site-to-site correlation ofExpedition 320 and Leg 199 sites, it was necessary torecheck the revised splices of Sites 1218 and 1219(Plike et al., 2005) and the shipboard splice of Site1220 (Shipboard Scientific Party, 2002c).

Site 1218

At Site 1218 (Figs. F14, F15, F16; Tables T14, T15,T16), the revised splice had to be corrected below210 corrected rmcd. Most of these adjustments bene-fited from detailed comparison to Site U1334. Priorto Expedition 320, Site 1218 was the only strati-graphically expanded and complete site from theequatorial Pacific covering the late Eocene and earlyOligocene. The revisions are mainly in intervals withvery high calcium carbonate content and low mag-netic susceptibility. A complete splice can be con-structed to 287 corrected rmcd, adding a growth fac-tor of 1.11 (Fig. F16).

Site 1219

Changes to the splice of Site 1219 (Figs. F17, F18; Ta-bles T17, T18) are very small, and thus we suggestcontinuing to use the table by Plike et al. (2005) toconstruct a composite record.

Site 1220

In contrast, the shipboard splice of Site 1220 had tobe corrected below 71 rmcd (Figs. F19, F20, F21; Ta-

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bles T19, T20, T21). Compared to the shipboardsplice the changes are minor, a few decimeters atmost. The new revised composite record reached 136rmcd and provided a growth factor of 1.10 (Fig. F21).Please note that Site 1220 was not part of the Plikeet al. (2005) splice revision. Therefore, this study isthe first revision of the shipboard splice of Site 1220and is indicated by the depth scale nomenclature re-vised meters composite depth (rmcd).

Cleaned magnetic susceptibility, GRA, and VGP data setsFor reference, we provide cleaned magnetic suscepti-bility and GRA density data sets for every splicedcomposite section of Sites U1331 (Table T22), U1332(Table T23), U1333 (Table T24), and U1334 (TableT25). Cleaned magnetic susceptibility, GRA density,and VGP latitude data are compiled for Sites 1218(Table T26), 1219 (Table T27), and 1220 (Table T28)(data sets are also available in Supplementary ma-terial). To obtain cleaned data we removed outliersand data collected close to end caps and cut out dis-turbed intervals (e.g., core tops). These data sets havebeen used for the subsequent site-to-site correlationand squeezing and stretching of core sections out-side the spliced records. The mapping pairs from thesqueezing and stretching can be used to positionsamples taken outside the splice to be placed intothe new revised composite depth scales.

Site-to-site correlationMore than 800 dated paleomagnetic reversals areavailable for all PEAT sites (Plike et al., 2009) andthus provide the perfect framework for the detailedintercalibration of all major fossil groups and refine-ment of magnetic polarity chrons, particularly in theEocene. However, the shipboard preliminary paleo-magnetic data from Expedition 320 used here haveto be considered incomplete. To improve the qualityof the magnetostratigraphy, stepwise demagnetiza-tion of U-channel samples accompanied by rockmagnetic studies are being done as part of the post-cruise science. High-quality and high-resolutionpaleomagnetic records covering the late Eocene, Oli-gocene, and early Miocene are available from Leg199 (Plike et al., 2005; Lanci et al., 2004, 2005). Thesites from both expeditions presented here are idealfor the establishment of a fully integrated calibratedbio-, chemo-, and magnetostratigraphy for the earlyEoceneearly Miocene time interval for the equato-rial Pacific. A prerequisite for successful integrationof the stratigraphic data and subsequent assembly ofthe proposed equatorial Pacific Cenozoic megaspliceis the correlation of decimeter-scale features in thesedimentary record from the drilled sites from both


Leg 199 and Expedition 320/321 (Plike et al., 2005,2009). We follow the successful approach of previousdeep-sea drilling expeditions (Shackleton et al.,1995, 1999; Shackleton and Crowhurst, 1997; Plikeet al., 2005; Westerhold and Rhl, 2006; Westerholdet al., 2007, 2008) by using physical property data(magnetic susceptibility and GRA) and XRF corescanning data to correlate site to site. In doing so wecan transfer, for example, the high-resolution bio-stratigraphic data from one site to intervals of an-other site where, due to poor preservation, datumsare not well constrained. Furthermore, we can locatehiatuses and condensed intervals that otherwisewould not have been identified. For correlation, wefirst identified a reference site that has the mostcomplete record and high sedimentation rates com-pared to the other sites. Then we correlated the othersites to the reference site by selecting tie points. Weapplied a linear interpolation of depth between tiepoints. Tie points are listed in Tables T29 and T30.

Correlation between Sites 1218, 1219, U1333, and U1334Physical property data at Sites 1218, 1219, U1333,and U1334 show a remarkable match (Fig. F22) eventhough the sites are between 375 and 1100 km apart.All sites have an excellent magnetostratigraphy, andthus comparison of the VGP data indicate the highquality of correlation. We have chosen Site 1218 tobe the reference site because Site 1218 is the mostcomplete down to the Eocene/Oligocene boundaryand has no geochemically altered interval, as foundin the mid-Oligocene of Site U1334. The integratedrecord spans the interval from Chron C1 (Pleisto-cene) back to Chron C20 (middle Eocene) covering>40 m.y. of equatorial Pacific history. We correlatedSites 1219, U1333, and U1334 to Site 1218 (TableT29), providing a coherent and integrated record forthe equatorial Pacific.

The correlation shows full coverage of magneto-stratigraphy back to the base of early OligoceneChron C11n.2n using Sites 1218 and U1334 alone.All four sites cover the interval from the base ofChron C6n to the base of C10n.2n (~20 to ~28 Ma)with a complete magnetostratigraphy. In the timespan older than Chron C12n (~30.8 Ma), the magne-tostratigraphic boundary positions can be trans-ferred from Site U1333 to Sites 1218, 1219, andU1334 when necessary. The complete magnetostrati-graphic record reaches back to the top of middle Eo-cene Chron C19n (~41 Ma).

Sedimentation rates in the section from 0 to 20 Maat all sites are highest at Site 1218 (a low 0.35 cm/k.y.).Sites 1219 and U1333 have even lower sedimenta-tion rates in that interval and a hiatus between the

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PliocenePleistocene and the lower Miocene (Plikeet al., 2009). All these sediments consist of clays de-posited near or below the calcium carbonate com-pensation depth. In the upper 40 m of the integratedstratigraphy (Fig. F22), correlations are based on theVGP data because magnetic susceptibility and GRAdata do not provide patterns that can be matchedwith certainty. Below that interval, matching of dif-ferent records was straightforward. From 20 Ma tothe Eocene/Oligocene boundary, Site U1334 has thehighest sedimentation rate (1.6 cm/k.y.) of all thesites (Site 1218 = 1.3 cm/k.y., Site 1219 = 1.2 cm/k.y.,and Site U1333 = 1.1 cm/k.y.). In the upper Eocenesection, sedimentation rates are slightly lower be-cause of the decreased carbonate content (see theExpedition 320/321 summary chapter [Expedi-tion 320/321 Scientists, 2010a]). Two short con-densed intervals were discovered: one at Site 1219between 112 and 114 corrected rmcd and one at SiteU1333 between 137 and 140 rmcd (m revised CCSF-A)(Fig. F22).

Correlation between Sites 1220, U1331, and U1332Physical property data from Sites 1220, U1331, andU1332 show a remarkable match (Fig. F23), beingonly 120 to 270 km apart. Sites 1220 and U1332have an excellent magnetostratigraphy from ChronsC6n to C20n (Table T31). Site U1331 sediment cov-ers Chrons C11C20n. We chose Site 1220 to be thereference site because it is the most complete for thisinterval. The correlation with Sites U1331 andU1332 (Table T30) provides a coherent and inte-grated record.

All three sites show rather low sedimentation rates(~0.5 cm/k.y.) compared to the shallower sites (1218,1219, U1333, and U1334) (Fig. F24). The upper Eo-cene sediments are dominated by siliceous ooze andalmost entirely lack carbonate sediment. The domi-nance of siliceous ooze leads to low variability in theGRA density; hence, correlation could only beachieved using magnetic susceptibility data. Thecomparison of the VGP data suggests a very goodmatch of the three sites in the Eocene. The increasedsedimentation rate at Site U1331 in the Eocene is anartifact of the frequent turbidites in the record. Thecorrelation of the Oligocene and Miocene section isstraightforward to 28 rmcd (Fig. F23). Above this,Site 1220 can only be matched to Site U1332 usingVGP data.

Radiolarians in the tropical PacificCenozoic radiolarian stratigraphy of the tropics waslargely developed in sediments from the Pacific


Ocean; however, it did not begin to reach its full po-tential until Leg 199 studies were completed by Ni-grini et al. (2006). This work, combined with that ofearlier studies (e.g., Moore, 1995), sought to tie ra-diolarian datums to a paleomagnetic timescale thatcould be tuned to orbital frequencies. These studiesalso greatly expanded the number of first and last oc-currences of species that were recorded and cali-brated. This effort took advantage of the many im-portant taxonomic and stratigraphic papers thathave appeared over the last 50 years, in particularthose written by such authors as William Riedel, An-nika Sanfilippo, Catherine Nigrini, David Johnson,and Jean Westberg, who focused much of their ef-forts on material collected in the tropical Pacific.

Expedition 320 was very successful in recovering Pa-cific Cenozoic sections deposited on or very close tothe paleoequator. Two of these drilled sites (U1333and U1334) recovered what appear to be completesections across the Eocene/Oligocene boundary.Only one other section, from Site 1218, has been re-covered in the tropical Pacific that clearly shows thetwo-step shift in lithology and geochemistry atthis boundary that we believe marks a truly completestratigraphic section (Coxall et al., 2005). Using thestratigraphic datums defined primarily in Nigrini etal. (2006), we were able to provide very detailed stra-tigraphic control on the sections recovered duringExpedition 320 (Tables T32, T33, T34, T35, T36,T37, T38). While producing this detailed integratedstratigraphy of the equatorial Pacific, we have had todeal with some complicated stratigraphic problemsthat still need to be fully addressed.

Reworking and mixing of older specimens into younger sectionsFinding reworked older radiolarian specimens inyounger sediments plagued the development of a re-liable radiolarian stratigraphy in its early days. Suchreworking was commonly found in piston cores andgravity cores from the tropical Pacific (e.g., Riedeland Funnell, 1964), and it was not until the Deep SeaDrilling Project (DSDP) and ODP started to collectthick pelagic sections that we were able to begin todevelop a reliable sequence of first and last appear-ances of species. In studying these sections, severalimportant observations have been made: (1) the re-worked older forms were never older than the age ofthe crust on which the sediment lay, (2) reworking ofolder forms is most common in the upper parts of re-covered sections, and (3) reworking of older formsfrom the Eocene is commonly found around the Eo-cene/Oligocene boundary and is often associatedwith a hiatus at this boundary (Moore et al., 1978;

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Moore, 1995). Because many of the biostratigraphicdatums near the uppermost part of the Eocene arelast appearances, the dependability of such datumsare highly suspect and their calibration to a time-scale is still open to question.

Taxonomic definitionNigrini et al. (2006) described 12 new species, severalof which are important in defining the Eocene/Oli-gocene boundary and in refining the stratigraphy ofthe Oligocene. These new species require the test oftime and usage to make sure their definitions ade-quately encompass the characteristics and variabilityof their form. Similarly, other species may need mod-ification of their descriptions in order to more con-sistently define biostratigraphic datums. Only asmall percentage of the total number of radiolarianspecies present at any given time has been identifiedas being stratigraphically useful (Riedel and San-filippo, 1978). Further work in this area will con-tinue to expand the resolution possible using radio-larian stratigraphy.

PreservationRadiolarians are generally well preserved in the trop-ical Pacific; however, they are subject to dissolution,particularly just above basement and at levels ofchert formation. Aside from these two problems, Eo-cene radiolarians are particularly robust (Moore,1969; Lazarus et al., 2009), and, with their very di-verse fauna, usually provide good stratigraphic con-trol. Preservation in the Oligocene of the sites stud-ied, however, is often only moderate and sometimesquite poor. It has yet to be determined if this varia-tion in Oligocene preservation is site specific or timespecific.

The radiolarian stratigraphic data presented hereinrepresent a work in progress. Additional samples arebeing studied and the detailed site-to-site correlationthat has been developed by the work presented herewill be used to further refine the positions of individ-ual biostratigraphic datums. Some of this more de-tailed work is shown in the radiolarian data tables(denoted by Revised in the column labeledSource). There remain many apparent small dis-crepancies in the levels of individual datums at dif-ferent sites. It is yet to be determined whether thesediscrepancies are a result of reworking of radiolariansabove or below the true level of the datum, a failureto recognize the presence of a rare species near itsfirst or last appearance, a true diachrony of the da-tum, or a minor miscorrelation of the lithologic re-cords themselves. Until these discrepancies can bestudied further, we use the age assigned each of thedatums as published by Nigrini et al. (2006).


Calcareous nannofossilsShipboard calcareous nannofossil biostratigraphyprovided critical age control during Leg 199 and Ex-pedition 320, allowing for the identification ofpaleomagnetic reversals and the development ofcomposite sections, especially within the successionsof carbonate-rich OligoceneMiocene nannofossiloozes. The new correlations presented here enablemore refined assessments of the timing and controlson the expression of calcareous nannofossil datumsin the equatorial Pacific. The presented tables ofnannofossil datums (Tables T39, T40, T41, T42, T43,T44, T45) are a compilation of data from both ship-board and postcruise biostratigraphy from Expedi-tion 320 and Leg 199 (Shipboard Scientific Party,2002a, 2002b, 2002c; Plike et al., 2006; see alsoBiostratigraphy in each site chapter [Expedition320/321 Scientists, 2010c, 2010d, 2010e, 2010f]).Calibration ages for calcareous nannofossil datumsfrom the Leg 199 timescale were made consistentwith those of Expedition 320 (bottom [B] Sphenoli-thus ciperoensis at 27.1 Ma rather than 28.1 Ma; BSphenolithus distentus at 30.0 Ma rather than 30.4 Ma;top [T] Reticulofenestra umbilicus at 32.0 Ma ratherthan 31.7 Ma), as were taxonomic concepts (use ofCoccolithus formosus rather than Ericsonia formosa).These changes do not imply that the datum agesused during Expedition 320 are better calibratedthan those used during Leg 199; revisions were un-dertaken prior to Expedition 320 partly based onpostcruise work from Leg 199 material (e.g., Blaj etal., 2009). For example, during Expedition 320 it be-came clear that the Leg 199 biostratigraphic datumage of 28.1 Ma for B S. ciperoensis produced a betterfit within the integrated stratigraphy than the re-vised age provided by Blaj et al. (2009) used duringExpedition 320/321 of 27.1 Ma. These discrepanciesare likely due to differences in taxonomic conceptand boundaries within the intergrading Oligocenesphenolith lineage Sphenolithus predistentus-distentus-ciperoensis. Ongoing postcruise taxonomic and bio-stratigraphic work will address these issues.

Placing the existing calcareous nannofossil biostra-tigraphy of Leg 199 and Expedition 320 within theframework of these new stratigraphic correlationsclearly shows that the accurate placement of calcare-ous nannofossil events is compromised by the occur-rence of intervals with low or no carbonate deposi-tion during the middle to late Eocene. A clearexample of this is the placement of the latest Eoceneevent T Discoaster saipanensis (see Tables T42, T43,T44). This event is well constrained at Site 1218 at244.52 0.06 corrected rmcd and at Site U1334 at301.33 0.53 rmcd (m revised CCSF-A) (equal to243.29 0.45 corrected rmcd [Site 1218]). But this

7


event is poorly constrained at Site 1219 within theinterval 190.06 13.83 rmcd (equal to 254.66 12.03corrected rmcd [Site 1218]), although the identifiedrange is fully consistent with the stratigraphy of Sites1218 and U1334. Where there is continuous carbon-ate sedimentation and reasonable nannofossil pres-ervation, most of the nannofossil datums correlateamong these equatorial Pacific sites within the accu-racy of the current sampling resolution (e.g., top ofR. umbilicus placed at 221.42, 222.97, 224.44, and220.99 corrected rmcd [Site 1218] at Sites 1218,1219, U1333, and U1334, respectively). Notable ex-ceptions to this are the placement of the base andtop of S. ciperoensis and the top of S. distentus. Thebase of S. ciperoensis is relatively consistent betweenSites 1218, 1219, and U1333 at ~144 corrected rmcd(Site 1218), but S. ciperoensis is first noted at lowabundance ~20 m lower at Site U1334 at ~164 cor-rected rmcd (Site 1218). This suggests the initial evo-lutionary appearance of S. ciperoensis is followed by aperiod of low abundance in the equatorial Pacificand then a marked abundance increase that is pickedas the B S. ciperoensis in the majority of these studysites. The top of S. ciperoensis is also depressed by ~20 mat Site U1333 (~130 corrected rmcd [Site 1218]) withrespect to the other sites (~111 corrected rmcd [Site1218] at Sites 1218, 1219, and U1334); again, thismay be due to low abundances at the top of this spe-cies range. The top of S. distentus is placed ~10 mhigher in the biostratigraphy of Leg 199 than that ofExpedition 320 (~130 corrected rmcd [Site 1218] atSites 1218 and 1219 versus ~140 corrected rmcd [Site1218] at Sites U1333 and U1334). This most likely re-flects slightly different taxonomic concepts appliedby different workers or simply the difficulty in apply-ing consistent taxonomy in a complex species plexusundergoing gradual change, as we observe withinthis lineage of Oligocene sphenoliths. Improving thetaxonomic definition of these sphenolith lineagesand determining the abundance patterns and timingof their origin and extinction will be the focus of on-going detailed biostratigraphic studies.

Reworked calcareous nannofossils were identified inlimited intervals of the Oligocene at the top of SiteU1331, associated with suspected gravity flow depos-its. These intervals were easily identified during ship-board biostratigraphy, and reworking of older nan-nofossils into younger strata is not thought to haveaffected the placement of nannofossil datums. Thestratigraphic framework presented here is an excel-lent basis for ongoing detailed assessments of lateEoceneOligocene nannofossil bioevents, with a par-ticular focus on the improved age resolution and theidentification of genuine diachrony across the easternequatorial Pacific. The integration of both radiolarian


and calcareous nannofossil biostratigraphy provedessential for shipboard operations during both Leg199 and Expedition 320, which both spanned themajor lithologic transition from Eocene radiolarianoozes to OligoceneMiocene calcareous nannofossiloozes. Continued biostratigraphic work on materialrecovered during these two expeditions and Expedi-tion 321 should produce a greatly improved inte-grated tropical Pacific radiolarian-nannofossil bio-stratigraphy of the last ~50 m.y.

SummaryWe revised the shipboard composite sections of SitesU1331, U1332, U1333, and U1334 from Expedition320 and Sites 1218, 1219, and 1220 from Leg 199 us-ing shipboard magnetic susceptibility data, GRA bulkdensity data, natural remanent magnetization data,and core images. Drilling distortions in cores arecompensated by differential squeezing and stretch-ing of parallel cores outside the splice at all investi-gated sites. This is of major importance because wewant to integrate all available data from all drilledholes. A detailed site-to-site correlation was per-formed. We linked the revised composite sections ofSites U1333, U1334, and 1219 to the corrected rmcdof Site 1218. Sites U1331 and U1332 were correlatedto the revised composite record of Site 1220. Wechose Sites 1218 and 1220 as reference sites becauseof their stratigraphic completeness. The decimeter-scale correlation was used to integrate and transferpaleomagnetic and biostratigraphic information.Our integrated stratigraphic framework presentedhere can be used as the backbone for the late Eocene,Oligocene, and early Miocene intervals of the equa-torial Pacific Cenozoic megasplice. Because of thepresence of clear paleomagnetic records and decime-ter-scale cyclic features, the investigated sedimentsare exceptionally suitable for further working on cy-clostratigraphy and orbital tuning. The integrationof Expedition 320 and Leg 199 data has the potentialto substantially improve the existing geologicaltimescale (Gradstein et al., 2004) and even extendthe astronomically calibrated timescale (Lourens etal., 2004; Plike et al., 2006) far back into the Eocene.

AcknowledgmentsThis manuscript benefitted from reviews by David J.Mallinson and Lucas J. Lourens. This research usedsamples and/or data provided by the IntegratedOcean Drilling Program (IODP). Funding for this re-search was provided by the Deutsche Forschungsge-meinschaft, the DFG-Leibniz Center for Surface Pro-

8


cess and Climate Studies at the University ofPotsdam, and by the National Science Foundation(NSF) through the US Science Support Program. Weare indebted to the IODP Bremen Core Repository(BCR) and Gulf Coast Repository (GCR) staff for corehandling.

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Figure F1. Location map of sites used in this study (red stars) and additional IODP/ODP/DSDP sites. F.Z. =fracture zone (modified from Plike et al., 2009).

160W 150 140 130 120 110

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Figure F2. Site U1331 paleomagnetic and physical property data on rmcd (m revised CCSF-A) scale. Splice mapand spliced core image on the left side, turbidite location on the right side. VGP = virtual geomagnetic pole,GRA = gamma ray attenuation. Red = Hole U1331A, blue = Hole U1331B, green = Hole U1331C, black = com-posite record. Composite record line is discontinuous because of distortion and data gaps. DI = drilled interval.(Continued on next three pages.)

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20

10

0

Magneticsusceptibility

(SI)GRA density

(g/cm3)U13

31A

U13

31B

U13

31C

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

Turb

iditeVGP latitude

()

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2Mag

netic

pola

rity



Figure F2 (continued). (Continued on next page.)

6H7H

8H9H

10H

6H7H

8H9H

10H

6H

100

90

80

70

60

50


(SI)GRA density

(g/cm3)U13

31A

U13

31B

U13

31C

Mag

netic

pola

rity

Turb

idite

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])VGP latitude

()-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2




11H

12H

13H

14H

15H

11H

12H

13H

14H

8H10

H12

H

150

140

130

120

110

100


(SI)GRA density

(g/cm3)U13

31A

U13

31B

U13

31C

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2Mag

netic

pola

rity

Turb

idite

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])VGP latitude

()

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2



Figure F2 (continued).

16X

17X

18X

19X

20X

21X

22X

15H

16H

17H

18X

19D

13H

14H

16H

17H

220

210

200

190

180

170

160

150


(SI)GRA density

(g/cm3)U13

31A

U13

31B

U13

31C

no data no data

VGP latitude()

Mag

netic

pola

rity

Turb

idite

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2


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of splice sections and yellow lines are the bases of those sections (tie to next software.

d [m revised CCSF-A])

Figure F3. Digital line scan images, Site U1331. Red lines are the topssection). Images were depth registered by R. Wilkens using IGOR-Pro

Depth (rmc


Figure F4. Growth factor calculated by plotting revised composite depth (rmcd [m revised CCSF-A]) againstdrilled core depth (CSF-A), Site U1331.

0

Depth (rmcd [m revised CCSF-A])

200

150

100

50

0

Dep

th C

SF

-A (

m)

Growth factor: 1.12

Site U1331

50 100 150 200

Hole 1331C

Hole 1331B

Hole 1331A



Figure F5. Site U1332 paleomagnetic and physical property data on rmcd (m revised CCSF-A) scale. Splice mapand spliced core image on the left side. VGP = virtual geomagnetic pole, GRA = gamma ray attenuation. Red =Hole U1332A, blue = Hole U1332B, green = Hole U1332C, black = composite record. Composite record line isdiscontinuous because of distortion and data gaps. (Continued on next two pages.)

1H2H

3H4H

5H6H

1H2H

3H4H

5H6H

1H2H

3H4H

5H6H50

40

30

20

10

0


(SI)GRA density

(g/cm3)

U13

32A

U13

32B

U13

32C VGP latitude

()

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 2Mag

netic

pola

rity

Hiatus

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])




7H8H

9H10

H11

H7H

8H9H

10H

11H

7H8H

9H10

H11

H12

H100

90

80

70

60

50


(SI)GRA density

(g/cm3)

U13

32A

U13

32B

U13

32C VGP latitude

()

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 21.2

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 21.2Mag

netic

pola

rity

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])




12H

13H

14H

15X

16X

12H

13H

14X

15X

16X

13H

14X

15X

16X

17X150

140

130

120

110

100


(SI)GRA density

(g/cm3)

U13

32A

U13

32B

U13

32C

Mag

netic

pola

rity

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

VGP latitude()

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 21.2

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 21.2


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Proc. IOD

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of splice sections and yellow lines are the bases of those sections (tie to nextsoftware.

[m revised CCSF-A])

Figure F6. Digital line scan images, Site U1332. Red lines are the tops section). Images were depth registered by R. Wilkens using IGOR-Pro

Depth (rmcd




150

100

50

0

Dep

th C

SF

-A (

m)

Growth factor: 1.09

Site U1332

0 50 100 150

Hole 1332C

Hole 1332B

Hole 1332A



Figure F8. Site U1333 paleomagnetic and physical property data on rmcd (m revised CCSF-A) scale. Splice mapand spliced core image on the left side. VGP = virtual geomagnetic pole, GRA = gamma ray attenuation. Red =Hole U1333A, blue = Hole U1333B, green = Hole U1333C, black = composite record. Composite record line isdiscontinuous because of distortion and data gaps. (Continued on next three pages.)

50

40

30

20

10

0-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 21.2

-90 -45 0 45 90 0 20 40 1.4 1.6 1.8 21.2

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

1H2H

3H4H

5H1H

2H3H

4H5H

1H2H

3H4H

5H6H


(SI)GRA density

(g/cm3)

U13

33A

U13

33B

U13

33C

Mag

netic

pola

rity

flow-in

VGP latitude()




100

90

80

70

60

50

6H7H

8H9H

6H7H

8H9H

10H

7H8H

9H10

H

GRA density(g/cm3)

U13

33A

U13

33B

U13

33C VGP latitude

()

Mag

netic

pola

rity

-5 0 5 10 15 20


(SI)D

epth

(rm

cd [m

rev

ised

CC

SF

-A])

-90 -45 0 45 90 1.4 1.6 1.8 21.21

-5 0 5 10 15 20-90 -45 0 45 90 1.4 1.6 1.8 21.21




150

140

130

120

110

100

VGP latitude()


(SI)GRA density

(g/cm3)

U13

33A

U13

33B

U13

33C

Mag

netic

pola

rity

10H

11X

12X

13X

14X

11H

12H

13H

14H

11H

12H

13H

14H

15H

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40D

epth

(rm

cd [m

rev

ised

CC

SF

-A])




200

190

180

170

160

150

VGP latitude()

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])


(SI)GRA density

(g/cm3)

U13

33A

U13

33B

U13

33C

Mag

netic

pola

rity

15X

16X

17X

18X

19X

15H

16H

17H

18H

19X

20X

16H

17H

18H

19H

20H

21H

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40


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Proc. IOD

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[m revised CCSF-A])

Figure F9. Digital line scan images, Site U1333. Red lines are the topssection). Images were depth registered by R. Wilkens using IGOR-Pro

Depth (rmcd

U13

33 S

plic

eU

1333

CU

1333

BU

1333

A




200

150

100

50

0

Dep

th C

SF

-A (

m)

Growth factor: 1.14

Site U1333

0 50 100 150 200

Hole 1333C

Hole 1333B

Hole 1333A



Figure F11. Site U1334 paleomagnetic and physical property data on rmcd (m revised CCSF-A) scale. Splicemap and spliced core image on the left side. VGP = virtual geomagnetic pole, GRA = gamma ray attenuation.Red = Hole U1334A, blue = Hole U1334B, green = Hole U1334C, black = composite record. Composite recordline is discontinuous because of distortion and data gaps. (Continued on next six pages.)

1H2H

3H4H

5H1H

2H3H

4H5H

1H2H

3H4H

5H50

40

30

20

10

0


(SI)GRA density

(g/cm3)

U13

34A

U13

34B

U13

34C VGP latitude

()-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40M

agne

ticpo

larit

y

Condensed

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40




6H7H

8H9H

10H

6H7H

8H9H

6H7H

8H9H

100

90

80

70

60

50


(SI)GRA density

(g/cm3)

U13

34A

U13

34B

U13

34C VGP latitude

()

Mag

netic

pola

rity

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40D

epth

(rm

cd [m

rev

ised

CC

SF

-A])




11H

12H

13H

14H

10H

11H

12H

13H

14H

10H

11H

12H

13H

150

140

130

120

110

100


(SI)GRA density

(g/cm3)

U13

34A

U13

34B

U13

34C VGP latitude

()

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40Mag

netic

pola

rity

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])




15H

16H

17H

18H

19H

15H

16H

17H

18H

14H

15H

16H

17H

18H

200

190

180

170

160

150

GRA density(g/cm3)

U13

34A

U13

34B

U13

34C


(SI)VGP latitude

()

-4 0 4 8 12

Mag

netic

pola

rity

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

-90 -45 0 45 90 1.4 1.6 1.8 21.21

-4 0 4 8 12-90 -45 0 45 90 1.4 1.6 1.8 21.21




20H

21H

22H

19H

20H

21H

22H

23X

19H

20H

21H

22H

250

240

230

220

210

200

GRA density(g/cm3)

U13

34A

U13

34B

U13

34C

Mag

netic

pola

rity

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

VGP latitude()

-5 0 5 10 15-90 -45 0 45 90 1.4 1.6 1.8 21.2120

-5 0 5 10 15-90 -45 0 45 90 1.4 1.6 1.8 21.2120


(SI)




23X

24X

25X

26X

27X

24X

25X

26X

23X

24X

25X

26X

27X

28X

300

290

280

270

260

250


(SI)GRA density

(g/cm3)

U13

34A

U13

34B

U13

34C

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40




28X

29X

30X

31X

32X

27X

28X

29X

30X

31X

29X

30X

31X

350

340

330

320

310

300


(SI)GRA density

(g/cm3)

U13

34A

U13

34B

U13

34C

Dep

th (

rmcd

[m r

evis

ed C

CS

F-A

])VGP latitude

()

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40

-90 -45 0 45 90 1.4 1.6 1.8 21.210 20 40


T. Westerh

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Proc. IOD

P | Volume 320/321

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s of splice sections and yellow lines are the bases of those sections (tie toPro software.

revised CCSF-A])

Figure F12. Digital line scan images, Site U1334. Red lines are the topnext section). Images were depth registered by R. Wilkens using IGOR-

Depth (rmcd [m




350

300

250

200

150

100

50

0

Dep

th C

SF

-A (

m)

Growth factor: 1.16

Site U1334

0 100 200 300

Hole 1334C

Hole 1334B

Hole 1334A



Figure F14. Site 1218 paleomagnetic and physical property data on corrected rmcd scale. Splice map andspliced core image on the left side. VGP = virtual geomagnetic pole, GRA = gamma ray attenuation. Red = Hole1218A, blue = Hole 1218B, green = Hole 1218C, black = composite record. Composite record line is discon-tinuous because of distortion and data gaps. (Continued on next five pages.)

1H2H

3H4H

5H1H

2H3H

4H5H

6H

50

40

30

20

10

0

GRA density(g/cm3)

1218

A12

18B

1218

C

Mag

netic

pola

rity

Dep

th (

corr

ecte

d rm

cd)


(SI)VGP latitude

()

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60




6H7H

8H9H

10H

7H8H

9H10

H1H

2H3H

4H

100

90

80

70

60

50


(SI)GRA density

(g/cm3)

1218

A12

18B

1218

C

Mag

netic

pola

rity

Dep

th (

corr

ecte

d rm

cd)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60




11H

12H

13H

14H

15H

11H

12H

13H

14H

15H

5H6H

7H8H

9H

150

140

130

120

110

100

-90 -45 0 45 90 0 20 40 60


(SI)

1 1.2 1.4 1.6 1.8

GRA density(g/cm3)

1218

A12

18B

1218

C

Mag

netic

pola

rity

Dep

th (

corr

ecte

d rm

cd)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60




16H

17H

18H

19H

16H

17H

18H

19X

20X

10H

11H

12X

13X

200

190

180

170

160

150


(SI)GRA density

(g/cm3)

1218

A12

18B

1218

C

Mag

netic

pola

rity

Dep

th (

corr

ecte

d rm

cd)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60




20H

22X

23X

24X

21X

22X

23X

24X

14X

15X

16X

17X

18X

250

240

230

220

210

200


(SI)GRA density

(g/cm3)

1218

A12

18B

1218

C

Mag

netic

pola

rity

Dep

th (

corr

ecte

d rm

cd)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60




25X

26X

27X

28X

29X

30X

25X

26X

27X

28X

29X

19X

20X

21X

300

290

280

270

260

250


(SI)GRA density

(g/cm3)

1218

A12

18B

1218

C

Mag

netic

pola

rity

Dep

th (

corr

ecte

d rm

cd)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60

-90 -45 0 45 90 1.4 1.6 1.81.210 20 40 60


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Proc. IOD

P | Volume 320/321

44

s of splice sections and yellow lines are the bases of those sections (tie to next software.

epth (rmcd)

Figure F15. Digital line scan images, Site 1218. Red lines are the topsection). Images were depth registered by R. Wilkens using IGOR-Pro

D


Figure F16. Growth factor calculated by plotting revised composite depth (rmcd) against drilled core depth(mbsf), Site 1218.

Depth (rmcd)

300

250

200

150

100

50

0

Dep

th (

mbs

f)

Growth factor: 1.11

Site 1218

0 50 100 150 200 250 300

Hole 1218C

Hole 1218B

Hole 1218A



Figure F17. Site 1219 paleomagnetic and physical property data on rmcd scale. Splice map and spliced coreimage on the left side. VGP = virtual geomagnetic pole, GRA = gamma ray attenuation. Red = Hole 1219A, blue= Hole 1219B, black = composite record. Composite record line is discontinuous because of distortion and datagaps. (Continued on next four pages.)

1H2H

3H4H

5H6H

2H3H

4H

50

40

30

20

10

0


(SI)GRA density

(g/cm3)

1219

A12

19B

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50




7H8H

9H10

H5H

6H7H

8H9H

100

90

80

70

60

50


(SI)GRA density

(g/cm3)

1219

A12

19B

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50




11H

12H

13H

14H

15H

10H

11H

12H

13H

14H

150

140

130

120

110

100


(SI)GRA density

(g/cm3)

1219

A12

19B

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50




16H

17H

18H

19H

15H

16H

200

190

180

170

160

150


(SI)GRA density

(g/cm3)

1219

A12

19B

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50




20H

21H

22H

23H

24H

250

240

230

220

210

200


(SI)GRA density

(g/cm3)

1219

A12

19B

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50

-90 -45 0 45 90 1.4 1.6 1.81.210 10 4020 30 50


T. Westerh

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et al.R

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Proc. IOD

P | Volume 320/321

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s are the tops of splice sections and yellow lines are the bases of those sections (tie to nexting IGOR-Pro software.

Depth (rmcd)

Figure F18. Digital line scan images, Site 1219. Red linesection). Images were depth registered by R. Wilkens us


Figure F19. Site 1220 paleomagnetic and physical property data on rmcd scale. Splice map and spliced coreimage on the left side. VGP = virtual geomagnetic pole, GRA = gamma ray attenuation. Red = Hole 1220A, blue= Hole 1220B, green = Hole 1220C, black = composite record. Composite record line is discontinuous becauseof distortion and data gaps. (Continued on next three pages.)

1H2H

3H4H

5H1H

2H1H

50

40

30

20

10

0


(SI)GRA density

(g/cm3)

1220

A12

20B

1220

C

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.61.210 40 12080 160

-90 -45 0 45 90 1.4 1.61.210 40 12080 160




6H7H

8H9H

10H

3H4H

5H6H

2H3H

4H5H

100

90

80

70

60

50


(SI)GRA density

(g/cm3)

1220

A12

20B

1220

C

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.61.210 40 12080 160

-90 -45 0 45 90 1.4 1.61.210 40 12080 160




11H

12H

7H8H

9H10

H11

H6H

7H8H

9H10

H

150

140

130

120

110

100


(SI)GRA density

(g/cm3)

1220

A12

20B

1220

C

Mag

netic

pola

rity

Dep

th (

rmcd

)

VGP latitude()

-90 -45 0 45 90 1.4 1.61.210 10 4020 30 50

-90 -45 0 45 90 1.4 1.61.210 10 4020 30 50




12H

13H

16X

11X

14X

200

190

180

170

160

150


(SI)GRA density

(g/cm3)

1220

A12

20B

1220

C

Mag

netic

pola

rity

Dep

th (

rmcd

)VGP latitude

()-90 -45 0 45 90 1.4 1.61.210 10 4020 30 50

-90 -45 0 45 90 1.4 1.61.210 10 4020 30 50


T. Westerh

old

et al.R

evised co

mp

osite d

epth

scales

Proc. IOD

P | Volume 320/321

56


pth (rmcd)

Figure F20. Digital line scan images, Site 1220. Red lines are the tops section). Images were depth registered by R. Wilkens using IGOR-Pro

De


Figure F21. Growth factor calculated by plotting revised composite depth (rmcd) against drilled core depth(mbsf), Site 1220.

Depth (rmcd)

200

150

100

50

0

Dep

th (

mbs

f)

Growth factor: 1.10

Site 1220

0 50 100 150 200

Hole 1220C

Hole 1220B

Hole 1220A



Figure F22. Site-to-site correlation of paleomagnetic and physical property data from Sites 1218, 1219, U1333,and U1334 on corrected rmcd scale of Site 1218. VGP = virtual geomagnetic pole, GRA = gamma ray attenu-ation. Black = Site 1218, green = Site 1219, blue = Site U1333, red = Site U1334. Composite record lines are dis-continuous because of distortion and data gaps. (Continued on next five pages.)

1218

1219

U13

33U

1334

1218

1219

U13

33U

1334

C1

C2

C3

C4

C5

Site

121

8 de

pth

(cor

rect

ed r

mcd

)

Core images

Magneticpolarity

0

5

10

15

20

25

30

35

40

45

50


(SI)GRA density

(g/cm3)VGP latitude

()-60 0 60 1.4 1.61.21 0 20 6040 801.8 2




C5

C6

1218

1219

U13

33U

1334

1218

1219

U13

33U

1334

Site

121

8 de

pth

(cor

rect

ed r

mcd

)

50

55

60

65

70

75

80

85

90

95

100

Core images

Magneticpolarity


(SI)GRA density

(g/cm3)VGP latitude

()-60 0 60 1.4 1.61.21 0 20 60401.8 2




C6

C7

C8

C9

1218

1219

U13

33U

1334

1218

1219

U13

33U

1334

Core images

Magneticpolarity


(SI)GRA density

(g/cm3)VGP latitude

()-60 0 60 1.4 1.61.21 0 10 3020 401.8 2

Site

121

8 de

pth

(cor

rect

ed r

mcd

)

100

105

110

115

120

125

130

135

140

145

150




C9

C10

C11

C12

1218

1219

U13

33U

1334

1218

1219

U13

33U

1334

Site

121

8 de

pth

(cor

rect

ed r

mcd

)

150

155

160

165

170

175

180

185

190

195

200

Core images

Magneticpolarity


(SI)GRA density

(g/cm3)VGP latitude

()-60 0 60 1.4 1.61.21 0 20101.8 2




C12

C13

C15

C16

Core images

Magneticp

revised composite depth scales and integration of iodp sites

Documents