Berger, W.H., Kroenke, L.W., Mayer, L.A., et al., 1993Proceedings of the Ocean Drilling Program, Scientific Results, Vol. 130

14. WHOLE-ROCK OXYGEN AND CARBON ISOTOPE STRATIGRAPHYOF THE PALEOGENE AND CRETACEOUS/TERTIARY BOUNDARY IN HOLE 807C1

Richard M. Corfield2 and Julie E. Cartlidge2

ABSTRACT

Whole-rock δ 1 8 θ analyses of the Paleogene and Upper Cretaceous succession at Ocean Drilling Program Hole 807C suggestthe presence of hiatuses between 876.95 and 894.47 mbsf and between 1138.82 and 1140.94 mbsf. The δ1 3C data show a pronouncedpositive excursion between 1130 and 1180 mbsf that corresponds to the positive δ1 3C values characteristic of the Paleocene. Despitethe stratigraphic breaks in the section, the δ 1 8 θ data show a systematic increase between 1360 mbsf and the hiatus between 876.95and 894.47 mbsf, which is consistent with previous suggestions of long-term climatic cooling through the Paleogene. TheCretaceous/Tertiary transition is apparently complete in this section and is of remarkable thickness. The expanded nature of thisportion of the succession is probably the result of secondary depositional processes. High-resolution sampling across this boundarymay reveal detailed structure of the δ1 3C decline associated with the extinctions that mark the termination of the Cretaceous.

INTRODUCTION

Ocean Drilling Program (ODP) Leg 130 Holes 807A and 807Ctogether form a composite section penetrating Neogene, Paleogene,and Cretaceous sediments on the flank of the Ontong Java Plateau.The upper part of the section consists of foraminiferal and nannofossilchalk that grades into limestone at approximately 1000 m below seafloor (mbsf). We made whole-rock δ13C and δ 1 8 θ measurementsthroughout the Paleogene and Cretaceous intervals of this section toassist in the identification of stratigraphic breaks and the documenta-tion of paleoceanographic trends. In particular, we concentrated onthe Cretaceous/Tertiary transition. The lithified nature of the Paleo-gene and Cretaceous does not presage well for detailed Creta-ceous/Tertiary boundary studies in comparison with such sites asDeep Sea Drilling Project (DSDP) Site 577 (Zachos et al., 1985) orHole 690B (Stott and Kennett, 1990). However, Hole 807C wasdrilled in a graben, and, as shown in this study, the unique sedimen-tological setting of this site may yield an exceptionally detailed recordof the Cretaceous/Tertiary boundary transition.

METHODS

The δ13C and 618O stratigraphies generated by the analysis ofwhole-rock samples were used to identify discontinuities that mightbe a result of the presence of hiatuses. Samples were drilled fromlimestone chips using a vibrotool, cleaned using 10% hydrogenperoxide and acetone, and then dried for 30 min at 60°C. The sampleswere analyzed isotopically using a VG Isotech PRISM mass spec-trometer with an on-line VG Isocarb carbonate preparation system inthe Oxford laboratory. The mass spectrometer is calibrated to PDBdaily by means of an in-house carbonate standard (NOCZ), which iscalibrated regularly to NBS 19. Reproducibility of replicate standardswas better than 0. l‰.

RESULTS AND DISCUSSION

Figure 1 shows the δ13C and δ 1 8 θ whole-rock stratigraphy of thecomposite Paleogene section of Holes 807A and 807C (data in Appen-dix). The δ 1 8 θ record in particular is useful for the identification of

'Berger, W.H., Kroenke, L.W., Mayer, L.A., et al., 1993. Proc. ODP, Sci. Results,130: College Station, TX (Ocean Drilling Program).

2 Department of Earth Sciences, University of Oxford, Park's Road, Oxford OX1 3PR,United Kingdom.

hiatuses because of its systematic change over the interval from thebase of the measured section (1360 mbsf) to a major discontinuitybetween 876.95 and 894.47 mbsf (Samples 130-807C-12R-1,35-37 cm, and -15R-1,57-59 cm). This generally monotonic trend isprobably the local expression of the long-term Cenozoic coolingdocumented in foraminifers by previous authors (e.g., Savin, 1977;Corfield et al., 1991). The discontinuity marked "A" between 876.95and 894.47 mbsf is not obviously connected to evidence of a hiatusfrom the shipboard biostratigraphy (Shipboard Scientific Party, 1991),but this may be because of the relative scarcity of biostratigraphicdatums within this interval of the core. Also, this level in Hole 807Cis characterized by poor recovery of sediment.

Another discontinuity (marked "B") occurs in the δ 1 8 θ recordbetween 1138.82and 1140.9 mbsf (between Samples 130-807C-46R-3,62-64 cm, and -47R-1,70-72 cm). Shipboard biostratigraphic data donot suggest the presence of a hiatus at this level in the hole. However,this may be caused by the difficulties of assigning age determinationsin limestone with a low abundance of marker species.

The interval between 1138.82 and 1188.8 mbsf (130-807C-46R-3,62-64 cm) and 1180 mbsf (130-807C-54R-1, 0-2 cm) exhibits verypositive δ1 3C values. This interval is within the Paleocene, as deter-mined by the shipboard biostratigraphers, and the isotopically posi-tive values are entirely typical of this interval (Shackleton and Hall,1984; Shackleton et al., 1985; Stott et al., 1990; Corfield et al., 1991).Figure 2 illustrates this portion of the core in more detail as well asthe Cretaceous/Tertiary boundary and the Late Cretaceous.

Premoli Silva (this volume) has identified a stratigraphic break(marked "C" on Fig. 2) between planktonic foraminiferal Zones Pl land P5 between 1160.24 and 1161.26 mbsf (between Samples 130-807C-51R-1, 3-5 cm, and -51R-1, 105-107 cm). Our δ13C data donot unequivocally support this interpretation however. The δ13Csignal across this portion of the core shows the monotonic declinecharacteristic of the upper Paleocene/Paleocene-Eocene boundaryinterval. The gap suggested by the biostratigraphy of Premoli Silva isapproximately 10 m.y. (between 58 and 48 Ma) using the time scaleof Berggren et al. (1985). This interval is characterized by a δ1 3Cdecline toward the δ13C minimum at or near the Paleocene/Eoceneboundary, followed by a recovery to values intermediate between the1 3C maximum of the late Paleocene and the minimum near thePaleocene/Eocene boundary. The whole-rock δ13C stratigraphy fromDSDP 527 illustrated by Shackleton et al. (1985, fig. 4) shows that at48 Ma δ13C values were at about approximately 2‰; 10 m.y. earlier(at 58 Ma) δ13C values from the same site were similar. Hence, nounique δ1 3C value for this interval is present that would discriminate

259

R.M. CORFIELD, J.E. CARTLIDGE

Se

rie

sO

ligo

cen

eE

oce

ne

P'cene

Maas.

j . Camp./1. Maas

Apt/Alb.

Div

isio

nupper

lower

upper

middle

lowerupperlowerUDDβT

middle

Ho

le

807A

807C

600

1400

4 -3 -2

6 C / PDB-18 06 O 7oo PDB

Figure 1. Oxygen and carbon isotope stratigraphy of the Paleogene and Cretaceous of Holes 807A and 807C. A = possible hiatus between 876.95and 894.47 mbsf, B = possible hiatus between 1138.82 and 1188.8 mbsf.

between the two possibilities. However, as Figure 1 shows, δ13C valuescontinue to decline after the interval between Samples 130-807C-51R-1, 3-5 cm, and -51R-1, 105-107 cm. This decline may be the localmanifestation of the continuing 513C decrease known from othersections to be characteristic of the early Eocene. If this is the case, thenit is unlikely that the biostratigraphic assignment of sediments up to1127.24 (Sample 130-807C-45R-2, 64 cm) where the possible hiatusmarked "B" occurs, are really from planktonic foraminifer biozonesPI 1 through P12/P13. This discrepancy may be reconciled by the factthat this portion of Hole 807C is known to be heavily reworked (Fig. 1;Premoli Silva, this volume); and, as she points out, because of thepervasive resedimentation in this part of the hole, zonal assignmentsare tentative. The δ 1 8 θ data also fail to show a discontinuity at this levelthat might support the presence of a hiatus.

Premoli Silva (this volume) also suggests the possibility of a hiatus(marked "D" on Fig. 2) between 1184.49 and 1185.51 mbsf betweenplanktonic foraminiferal Zone P3 and Subzone Plb (Samples 130-807C-53R-4, 58-60 cm, and -53R-5, 10-12 cm). Both the δ13C andthe δ 1 8 θ data indicate a disjunction that might support this hypothesis.Further biostratigraphic and chemostratigraphic work at a higher sam-ple spacing is clearly required to resolve these differences.

The Cretaceous/Tertiary Boundary at Hole 807C

We significantly increased our sampling resolution across the Cre-taceous/Tertiary boundary at Hole 807C based on the identification byshipboard biostratigraphers of the Thoracosphaera bloom that is char-acteristic of the immediate aftermath of the boundary interval(Pospichal and Wise, 1990). In addition, we used the biostratigraphicdata of Premoli Silva (this volume), which provides further constraintson the stratigraphy of this portion of Hole 807C. Premoli Silva (this

volume) places the Cretaceous/Tertiary boundary between Samples130-807C-55R-1, 49-50 cm, and -55R-1, 35-36 cm (1197.39 and1197.25 mbsf) on the basis of the first occurrence (FO) of Tertiaryplanktonic foraminifers. Hence, a median estimate of the position ofthis boundary is at Sample 130-807C-55R-1, 4 2 ^ 3 cm (1197.32mbsf). Premoli Silva (this volume) further estimates the FO of Sub-botina pseudobulloides (which according to the zonal scheme ofBerggren and Miller [1988] defines the base of planktonic foraminiferSubzone Pla) to lie at Sample 130-807C-54R-4,148-149 cm (1194.78mbsf). This is consistent with the placement by Mao and Wise (thisvolume) of the FO of Coccolithus pelagicus (within nannofossil Sub-zone CPlb) at Sample 130-54R-3,90 cm (1192.7 m). Using the FO ofDanian planktonic foraminifera and the FO of S. pseudobulloides, wecalculate a median thickness for this interval of 2.54 m. Using the timescale of Berggren et al. (1985), this yields a sedimentation rate for thispart of Hole 807C of 12.7 m/m.y. We note, however (Premoli Silva,this volume), that problems exist in unequivocally assigning zonalboundaries because of the lithified nature of the sediment. As Table 1shows, this is the highest sedimentation rate documented of severalintensively studied Cretaceous/Tertiary boundary sections, with thepossible exception of DSDP Site 524 (Hsü et al., 1982). We note thatour sedimentation rate estimate of 12.7 m/m.y. for the Cretaceous/Ter-tiary transition at Hole 807C is similar to the independent estimate of14 m/m.y. based on paleomagnetic data (J.A. Tarduno, pers. comm.,1992; Corfield et al., this volume). Thus, although Hole 807C is inlimestone facies, the potential to resolve closely spaced chemostrati-graphic and biostratigraphic events exists at this site, provided it canbe demonstrated that the sediments have not been too distorted bysecondary sedimentation.

Figure 3 illustrates our δ13C and δ 1 8 θ data from the Cretaceous/Tertiary boundary interval at Hole 807C. The δ13C decline noted by

260

WHOLE-ROCK OXYGEN AND CARBON ISOTOPE STRATIGRAPHY

Era

Te

rtia

ryC

reta

ce

ou

s

Pla

nk.

Fora

m

Zo

ne

P15?

P14

P12/P13

••"P11 " '

:::::«::::

P4

."*?.-.-PIf> j

Abathomphalusmayaroβnsrs

Gansserinaganssen

Globotnmcansaβgypbca

Co

re

39R

40R

fin43R

44R

45R

4βR

—flR—Si—SB

51R

52R

M R

M R

S5R

56R

57R

58R

59R

60R

61R

62R

63R

64R

6SR

6SR

67R

68R

70R

71R

-

-

•

-

1100 -

oo PDB

Figure 2. Oxygen and carbon isotope stratigraphy of the Paleocene and Upper Cretaceous of Hole 807C. Note the isotopically positive valuescharacteristic of the Paleocene epoch. Hiatus B is identified; C and D = possible hiatuses inferred from lack of identifiable foraminiferal zones (PremoliSilva, this volume).

authors at several different sites (e.g., Scholle and Arthur [1980],Renard [1986], and Corfield et al. [1991] at the Bottaccione Gorgesection in Italy; Shackleton and Hall [1984] atDSDPSite527;Zachosand Arthur [1986] at DSDP 577; Stott and Kennett [1990] at ODPHole 690B) is clearly discernible at Hole 807C. In addition, becauseof the high sedimentation rates in the Cretaceous/Tertiary boundaryinterval at Hole 807C, the δ13C decline occurs over a thickness of9.23 m. This is probably the most expanded Cretaceous/Tertiary δ13Cdecline yet documented.

Clearly, it is imperative to understand how such a thick Creta-ceous/Tertiary boundary section could have been deposited andwhether such a section can be regarded as stratigraphically continuousand sedimentologically undisturbed. The high sedimentation ratescalculated for the Cretaceous/Tertiary boundary interval at Hole 807Cstrongly suggest that deposition was not primary. W.H. Berger (pers.comm., 1991) has suggested that sedimentation rates at Hole 807Cwere significantly enhanced during this interval as a result of win-nowing of the sediment cover surrounding the graben. The increasedflux of sediment into the graben would result in significantly highersedimentation rates because of the confined nature of this smallsedimentary basin. Support for this hypothesis comes from the bio-stratigraphic data of Premoli Silva (this volume) and Sliter and Leckie(this volume), who identified both size and shape sorting of plank-tonic foraminifers from thin sections that suggest winnowing. As wellas size and shape sorting, Premoli Silva (this volume) has identifiedturbiditic layers within the Cretaceous/Tertiary succession atHole 8O7C. We have plotted these intervals of sedimentological dis-turbance on Figure 3. The setting of the Cretaceous/Tertiary boundaryat this site is further discussed in Corfield et al. (this volume).

In addition to this peculiar sedimentological environment, evidenceis present for stylolitization within this portion of Hole 807C. Thesediment compression implied by stylolitization suggests the prob-ability that carbonate-bearing pore fluids might have been mobilized,possibly leaching sediment from one part of the core and depositing itelsewhere in the form of carbonate cement. However, the presence ofstylolites is patchy within the Cretaceous/Tertiary boundary section ofHole 807C and is limited at most to centimeter-scale occurrence. Thus,we consider it unlikely that this process could have affected the whole9.23-m thickness of the δ13C decline at the Cretaceous/Tertiary bound-ary at Hole 807C. Diagenetic complications of the δ13C signal arefurther discussed in Corfield et al. (this volume).

Given the pervasive influence of foraminiferal resedimentationfrom winnowing and turbidity currents within the boundary intervalat Hole 807C, it is possible that the monotonic decline in δ13C overthis 9.23-m interval is a result at least in part of secondary depositionalprocesses, and therefore that the record is not a reliable portrait ofevents. Reworking of fine-fraction calcite could result theoreticallyin the transposition of heavy (Cretaceous) δ13C values to higher(Danian) levels in the core if the ratio of reworked material to materialin primary position were high and the reworked material were signifi-cantly older than the primary material. To rework the entire 9.23-mthickness of the Cretaceous/Tertiary boundary carbon isotope deple-tion at Hole 807C would require the mixing of older material rela-tively enriched in 13C with younger material relatively depleted in 13C,and its amalgamation into micrite, which would possess an averageδ13C composition. We note, however, that the δ13C record across theCretaceous/Tertiary boundary at Hole 807C proceeds remarkablyuniformly, a feature not necessarily predicted by the episodic rework-

261

R.M. CORFIELD, J.E. CARTLIDGE

Table 1. Comparative sedimentation rates acrossselected DSDP and ODP Cretaceous/Tertiaryboundary sections.

Hole

DSDP 577DSDP 524DSDP 527ODP 690CODP 689BODP 807C

Sedimentation rate(m/m.y.)

'1.95266.60

35.0042.50*41.00*12.70

Notes: Estimates based on depth difference between theCretaceous/ Tertiary boundary and the FO of Subbotinapseudo-bulloides (K/T boundary in this case is defined bythe FO of Danian planktonic foraminifers except wheremarked with an asterisk (*), in which case the boundary isdefined by the LO of Cretaceous planktonic foraminifers).

1 Date from Gerstel et al. (1986), but also see discussion byCorfield and Shackleton (1988).

2 This high value is almost certainly the result of the poordepth uncertainties associated with the planktonicforaminifer age control points over this interval in DSDPHole 524. Note, however, that Hsii et al. (1982) claimedvery high rates of 30 m/m.y. for this site on the basis ofother sedimentation rate constraints.

3 Data from Boersma (1984).4 Data from Thomas et al. (1990).

ing of older material suggested by size and shape sorting of foramini-fers. In addition, if secondary sedimentation from the region aroundthe graben walls occurred contemporaneously with primary sedimen-tation, as is conceivable from the winnowing and bottom-currentactivity suggested for this site, then there is no reason to suppose thatthe overall features of the δ13C decline would be lost. Clearly, the dataat present are insufficient to distinguish the relative contributions tothe δ13C decline of primary and secondary sedimentation across theCretaceous/Tertiary boundary at Hole 807C. As a check on the repro-ducibility of our data, we have repeated some measurements over theδ13C minimum as well as replicating five additional times selectedmeasurements over the entire δ13C decline (Tables 2 and 3). Bothtypes of repeat analyses show good agreement (Fig. 4) with ouroriginal measurements, confirming the expanded nature of this Cre-taceous/Tertiary boundary δ13C decline at Hole 807C.

Figure 3 shows that the initiation of the most rapid δ I 3C declineoccurs at 1202.25 mbsf (Sample 130-807C-55R-4, 85-87 cm). Thisis significantly below the FO of Tertiary planktonic foraminifers,which occurs at 1197.32 mbsf (Sample 130-807C-55R-1,42-43 cm).The δ13C values continue to decline with minor fluctuations, reachinga minimum at 1193.02 mbsf (Sample 130-807C-54R-3,122-124 cm).This is coincident with the peak in the Thoracosphaera bloom notedby the shipboard biostratigraphers (Shipboard Scientific Party, 1991)and initially used to locate the position of the Cretaceous/Tertiaryboundary at Hole 807C. The amplitude of the δ13C decline between1202.25 and 1193.02 mbsf is 1.7‰. If secondary sedimentation waspervasive during the deposition of this boundary succession, then thestratigraphic separation of the onset of δ13C decline and the lastoccurrence (LO) of Cretaceous planktonic foraminifers and Creta-ceous nannofossils could be caused by the reworking of these fossilshigher up the section. However, the Cretaceous/Tertiary boundary hasbeen placed on the FO of Danian planktonic foraminifers betweenSamples 130-807C-55R-1,49-50 cm, and -55R-1,35-36 cm (1197.39and 1197.25 mbsf; median = 1197.32). It is difficult to explain theseparation of the onset of δ13C decline and the first occurrence ofDanian planktonic foraminifers by reworking. Hence, this separationmust be considered a primary phenomenon in the absence of data tothe contrary.

The δ 1 8 θ data remain relatively constant over the interval between1202.5 mbsf (Sample 130-807C-55R-4, 110 cm) and 1196.97 mbsf

(Sample 130-807C-55R-1, 7-8 cm). After an interval of no recovery(placed by ODP convention at the base of the core barrel), δ 1 8 θ valuesare about 0. l‰ more negative at -1.8‰. At 1193.02 mbsf, coincidentwith the peak in the Thoracosphaera bloom, δ 1 8 θ values begin toincrease. The δ 1 8 θ increase peaks at 1190.26 mbsf (Sample 130-807C-54R-1, 146-148 cm) and its amplitude is 0.6‰. Recrystalliza-tion is widespread within this section, and it is impossible, therefore,to make specific assertions about absolute change in temperature. Inparticular, the δ 1 8 θ values are relatively negative (in general, fluctu-ating around -1.8‰) compared with other important Cretaceous/Ter-tiary boundary successions from the deep ocean. Whole-rock orfine-fraction measurements from DSDP Holes 47.2 and 577 (Zachoset al., 1985) fluctuate around approximately -l%o, whereas fine-frac-tion measurements from a depth transect of Cretaceous/Tertiaryboundary sites drilled during DSDP Leg 74 (Shackleton and Hall,1984) are in the O.O‰ to about -0.5‰ range. As DSDP Hole 577 wasin the tropics during the Late Cretaceous and Paleocene, these fine-fraction values may be considered to reflect sea-surface temperaturesas monitored predominantly by nannofossils. Our more negativeresults from Hole 807C are therefore likely to be the result ofrecrystallization at relatively elevated deep burial temperatures. How-ever, recrystallization in the absence of conspicuous quantities oforganic matter is unlikely to have significantly modified the shape ofthe δ13C decline (e.g., Williams et al., 1988).

Our data show that the beginning of the δ13C decrease precedesthe FO of Tertiary planktonic foraminifers, but that the apparent onsetof the δ13C decline may be more or less synchronous with thebeginning of the Cretaceous/Tertiary boundary interval as recognizedusing nannofossils (Mao and Wise, this volume). We note, however,that the position of the Cretaceous/Tertiary boundary is difficult toplace precisely because of poor preservation and reworking.

If we assume that the apparent separation of the FO of Tertiaryplanktonic foraminifers and the onset of δ13C decline is a primaryfeature of the record at Hole 807C, then it is useful to attempt toconstrain the relative timing of events. We have developed a time scalefor this interval of Hole 807C (Fig. 5), and our estimates suggest thatthe onset of the δ13C decline precedes the extinction by 450,000 yr.Note that this is certainly an overestimate due to the use of the S.pseudobulloides datum in a reworked succession. Other workers haveshown that the δ13C decline preceded the extinction of the planktonicforaminifers (e.g., at neritic sites exposed in Europe [Perch-Nielsonet al., 1982] and at DSDP 524 [Hsü et al., 1982]). Hence, it is notsurprising that in the expanded section recovered at Hole 807C thisfeature should also be distinguished.

Macleod and Keller (1991) have recently pointed out that theapparent rapidity of the δ13C decline at the Cretaceous/Tertiaryboundary in deep-sea sections may be a result of the widespreadoccurrence of hiatuses across the boundary interval. The implication,therefore, is that if the δ13C decline is gradual then the probabilityexists that the boundary is more complete than where the δ13C declineis abrupt. It is an unfortunate feature of the Cretaceous/Tertiaryboundary section at Hole 807C that at present the nannofossil biostra-tigraphy is inadequate to accurately constrain the precise sequence offloral events with respect to the δ13C curve. Given the reservations ofMao and Wise (this volume) concerning the poor preservation andreworking of nannofossils across this Cretaceous/Tertiary boundarysuccession, it may well be that further refinement of the nannofossilbiostratigraphy is not possible. It is clear, however, that the δ13Cdecline and the FO of Tertiary planktonic foraminifers occurs beforethe Thoracosphaera bloom. This is consistent with the hypothesis thatthe Thoracosphaera bloom was a response to vacated ecospace (the"Strangelove Ocean" of Hsü and McKenzie, 1985).

We conclude that the unique sedimentological setting ofHole 807C has led to the recovery of an apparently complete recordof the δ13C change across the Cretaceous/Tertiary boundary event,although the succession contains a significant component from re-sedimentation. We note, however, that reworking was apparently

262

WHOLE-ROCK OXYGEN AND CARBON ISOTOPE STRATIGRAPHY

pervasive at the relatively thick Cretaceous/Tertiary boundary sectionat DSDP Site 527 without markedly deforming the δ I 3C decline acrossthe Cretaceous/Tertiary boundary there. However, those measure-ments were made on unlithified samples and were relatively unaf-fected by the problems of secondary cementation noted in Hole 807C.

ACKNOWLEDGMENTS

We are grateful to Isabella Premoli Silva and Bill Sliter for makingavailable their planktonic foraminiferal biostratigraphy of the Creta-ceous/Tertiary boundary interval in Hole 807C. We thank John Tardunofor making available his paleomagnetic data for the Cretaceous/Terti-ary interval in Hole 807C. We are also grateful to Mike Durkin forvaluable and stimulating discussion and for reading earlier versions ofthis manuscript. Finally, we are sincerely grateful to Lowell Stott andJim Zachos for careful and constructive reviews of this paper, whichsubstantially improved the final version.

REFERENCES*

Berggren, W.A., Kent, D.V. and Flynn, J.J., 1985. Jurassic to Paleogene: Part2. Paleogene geochronology and chronostratigraphy. In Snelling, N.J.(Ed.), The Chronology of the Geological Record. Geol. Soc. LondonMem., 10:141-195.

Berggren, W.A., and Miller, K.G., 1988. Paleogene tropical planktonicforaminiferal biostratigraphy and magnetobiochronology. Micropaleon-tology, 34:362-380.

Boersma, A., 1984. Cretaceous-Tertiary planktonic foraminifers from thesoutheastern Atlantic, Walvis Ridge area, Deep Sea Drilling Project Leg74. In Moore, T.C., Jr., Rabinowitz, P.D., et al., Init. Repts. DSDP, 74:Washington (U.S. Govt. Printing Office), 501-524.

Corfield, R.M., Cartlidge, J.E., Premoli Silva, I., and Housley, R.A., 1991.Oxygen and carbon isotope stratigraphy of the Paleogene and Cretaceouslimestones in the Bottaccione Gorge and the Contessa Highway sections,Umbria, Italy. Terra Nova, 3:414-422.

Corfield, R.M., and Shackleton, N.J., 1988. Comment and reply on "Danianfaunal succession: planktonic foraminiferal response to a changing marineenvironment." Geology, 16:378-379.

Gerstel, J., Thunell, R.C., Zachos, J.C., and Arthur, M.A., 1986. The Creta-ceous/Tertiary boundary events in the North Pacific: planktonic foraminif-eral results from Deep Sea Drilling Project Site 577, Shatsky Rise.Paleoceanography, 1:97-117.

Hsü, K.J., He, Q., McKenzie, J.A., Weissert, H., Perch-Nielson, K., Oberhán-sli, H., Kelts, K., LaBrecque, J., Tauxe, L., Kràhenbühl, U., Percival, S.F.,Wright, R., Karpoff, A.M., Petersen, N., Tucker, P., Poore, R.Z., Gombos,A.M., Pisciotto, K., Carman, M.F., Schreiber, E., 1982. Mass mortality andits environmental and evolutionary consequences. Science, 216:249-256.

Hsü, K.J., and McKenzie, J.A., 1985. A "strangelove" ocean in the earliestTertiary. In Sundquist, E.T., and Broecker, W.S. (Eds.), The Carbon Cycleand Atmospheric CO2: Natural Variations Archean to Present. Am. Geo-phys. Union, Geophys. Monogr., 32:487^192.

Macleod, N., and Keller, G., 1991. Hiatus distributions and mass extinctionsat the Cretaceous/Tertiary boundary. Geology, 19:497-501.

Perch-Nielson, K., McKenzie, J., and He, Q., 1982. Biostratigraphy andisotope stratigraphy and the "catastrophic" extinction of calcareous nan-noplankton at the Cretaceous/Tertiary boundary. In Silver, L.T., and

Schultz, PH. (Eds.), Geological Implications of Impacts of Large Aster-oids and Comets on the Earth. Spec. Pap., Geol. Soc. Am., 190:353-371.

Pospichal, J.J., and Wise, S.W., Jr., 1990. Calcareous nannofossils across theK/T boundary, ODP Hole 690C, Maud Rise, Weddell Sea. In Barker, P.F.,Kennett, J.P., et al., Proc. ODP, Init. Repts., 113: College Station, TX(Ocean Drilling Program), 515-532.

Renard, M., 1986. Pelagic carbonate chemostratigraphy (Sr, Mg, 18O, 13C).Mar. Micropaleontol., 10:117-164.

Savin, S.M., 1977. The history of the EarúYs surface temperature during thepast 100 million years. Annu. Rev. Earth. Planet. Sci., 5:319-355.

Scholle, P.A., and Arthur, M.A., 1980. Carbon isotope fluctuations in Creta-ceous pelagic limestones: potential stratigraphic and petroleum explora-tion tool. AAPG Bull, 64:67-87

Shackleton, N.J., and Hall, M.A., 1984. Carbon isotope data from Leg 74sediments. In Moore, T.C., Jr., Rabinowitz, P.D., et al., Init. Repts. DSDP,74: Washington (U.S. Govt. Printing Office), 613-619.

Shackleton, N.J., Hall, M.A., and Bleil, U., 1985. Carbon isotope stratigraphy,Site 577. In Heath, G.R., Burckle, L.H., et al., Init. Repts. DSDP, 86:Washington (U.S. Govt. Printing Office), 503-512.

Shipboard Scientific Party, 1991. Site 807. In Kroenke, L.W., Berger, W.H.,Janecek, T.R., et al., Proc. ODP, Init. Repts., 130: College Station, TX(Ocean Drilling Program), 369^93.

Stott, L.D., and Kennett, J.P., 1990. The paleoceanographic and paleoclimaticsignature of the Cretaceous/Paleogene boundary in the Antarctic: stableisotopic results from ODP Leg 113. In Barker, P.F., Kennett, J.P., et al.,Proc. ODP, Init. Repts., 113: College Station, TX (Ocean Drilling Pro-gram), 829-848.

Stott, L.D., Kennett, J.P., Shackleton, N.J., and Corfield, R.M., 1990. Theevolution of Antarctic surface waters during the Paleogene: inferencesfrom stable isotopic composition of planktonic foraminifers, ODP Leg 113.Proc. ODP, Sci. Results, 113: College Station, TX (Ocean Drilling Pro-gram), 849-863.

Thomas, E., Barrera, E., Hamilton, N., Huber, B.T., Kennett, J.P., O'Connell,S.B., Pospichal, J.J., Spieß, V, Stott, L.D., Wei, W, and Wise, S.W., Jr.,1990. Upper Cretaceous-Paleogene stratigraphy of Sites 689 and 690,Maud Rise, (Antarctica). In Barker, P.F., Kennett, J.P., et al., Proc. ODP,Sci. Results, 113: College Station, TX (Ocean Drilling Program), 901-914.

Williams, D.F., Lerche, I., and Full, W.E., 1988. Isotope Chronostratigraphy:San Diego (Academic Press).

Zachos, J.C., and Arthur, M.A., 1986. Paleoceanography of the Creta-ceous/Tertiary boundary event: inferences from stable isotopic and otherdata. Paleoceanography, 1:5-26.

Zachos, J.C., Arthur, M.A., Thunell, R.C., Williams, D.F., and Tappa, E.J., 1985.Stable isotope and trace element geochemistry of carbonate sedimentsacross the Cretaceous/Tertiary boundary at Deep Sea Drilling ProjectHole 577, Leg 86. In Heath, G.R., Burckle, L.H., et al., Init. Repts. DSDP,86: Washington (U.S. Govt. Printing Office), 513-532.

Abbreviations for names of organizations and publication titles in ODPreference lists follow the style given in Chemical Abstracts Service SourceIndex (published by American Chemical Society).

Date of initial receipt: 9 September 1991Date of acceptance: 1 September 1992Ms 130B-027

263

R.M. CORFIELD, J.E. CARTLIDGE

CO

LU

çO•ECD

CO

OsBö

coCDcoN

P3a?

P1a

Pa

2"•gO CD

üco

cCD

CO

Turfoidite

σ>

Icc

1(0

1190

1195 -Q.ΦT3

O

1200

1205

-1.5 -1 -0.5

δ1 3C%oPDBr18 0/6 O 7ooPDB

Figure 3. Oxygen and carbon isotope stratigraphy of the Cretaceous/Tertiary transition at Hole 807C with foraminiferal zones and sedimentology ofPremoli Silva (this volume).

cö

LLJ

CD

CO

oCDO

Bö

COCDcoN

P3a?

P1a

Pa

SBO CD

üCT)

cCD > s

CO

Turbidite

15

§CD

tr

T3CD

1190

1195 •Q.CD

T3

o

-Qn 1200

1205

3-2.5 -2 -1.5 -1 -0.5

δ13C°/00PDB18 0/

O 'ooPDB

Figure 4. Repeat analyses of whole-rock carbonates across the Cretaceous/Tertiary boundary succession at Hole 807C. Circles refer to individuallyrepeated measurements, solid bars are 1 standard deviation around the mean of 5 additional measurements of that sample.

264

WHOLE-ROCK OXYGEN AND CARBON ISOTOPE STRATIGRAPHY

Table 2. Repeated single measurements on selected carbonatesacross the δ13C minimum of the Cretaceous/Tertiary boundary atHole 807C.

Lab no.

A90/2016A90/2017A90/2019A90/2020A90/2021A90/2022A90/2023A90/2024A90/2025A90/2026A90/2027A90/2028A90/2029A90/2030A90/2031A90/2032

Hole, core, section,interval (cm)

807C-54R-3, 139807C-54R-3, 149807C-54R-4, 20807C-54R-4, 31807C-54R-4, 40807C-54R-4, 50807C-54R-4, 62807C-54R-4, 80807C-54R-4, 90807C-54R-4, 100807C-54R-4, 113807C-54R-4, 125807C-54R-4, 135807C-54R-4, 148807C-55R-1.7807C-55R-1, 17

Depth(mbsf) t

1193.191193.291193.501193.611193.701193.801193.921194.101194.201194.301194.431194.551194.651194.781196.971197.07 :

13C

.28

.68

.64

.60

.13

.75

.69

.85

.74

.39

.75

.86

.83

.91

.96>.12

δ 8 o

-2.00-1.77-1.64-1.84-2.15-1.69-1.95-1.61__-__--

-

.96

.97

.87

.86

.14

.30

.69

.78

Age(Ma)

66.0766.0866.1066.1166.1166.1266.1366.1566.1566.1666.1766.1866.1966.2066.3766.38

Table 3. Multiple replicates of selected carbonates across the Cretaceous/Tertiaryboundary succession at Hole 807C.

Lab no.

NOCZNOCZNOCZNOCZA92/2244A92/2245A92/2246A92/2247A92/2248A92/2249A92/2250A92/2251A92/2252A92/2253A92/2254A92/2255A92/2256A92/2257A92/2258A92/2259A92/2260A92/2261A92/2262A92/2263A92/2264A92/2265A92/2266A92/2267A92/2268A92/2269A92/2270A92/2271A92/2272A92/2273A92/2274A92/2275A92/2276A92/2277A92/2278NOCZNOCZNOCZNOCZNOCZ

Hole, core, section,interval (cm)

807C (5/8/92)807C (5/8/92)807C (5/8/92)807C (5/8/92)807C-54R-2, 62807C-54R-2, 62807C-54R-2, 62807C-54R-2, 62807C-54R-2, 62807C-54R-3, 53807C-54R-3, 53807C-54R-3, 53807C-54R-3, 53807C-54R-3, 53807C-54R-3, 122807C-54R-3, 122807C-54R-3, 122807C-54R-3, 122807C-54R-3, 122807C-55R-1, 26807C-55R-1, 26807C-55R-1, 26807C-55R-1, 26807C-55R-1, 26807C-55R-3, 143807C-55R-3, 143807C-55R-3, 143807C-55R-3, 143807C-55R-3, 143807C-55R-4, 85807C-55R-4, 85807C-55R-4, 85807C-55R-4, 85807C-55R-4, 85807C-56R-l,20807C-56R-l,20807C-56R-1.20807C-56R-1.20807C-56R-1.20807C (5/8/92)807C (5/8/92)807C (5/8/92)807C (5/8/92)807C (5/8/92)

Depth(mbsf)

———

1190.921190.921190.921190.921190.921192.331192.331192.331192.331192.331193.021193.021193.021193.021193.021197.161197.161197.161197.161197.161201.331201.331201.331201.331201.331202.251202.251202.251202.251202.251206.801206.801206.801206.801206.80

—————

δ 1 3 c

2.242.262.292.282.302.031.981.982.001.071.151.081.051.081.001.101.091.041.042.072.162.202.112.182.392.712.482.562.502.692.692.722.722.722.812.842.742.782.812.322.302.332.312.30

δ 1 8 o

-1.96-1.93-1.80-1.90-0.95-0.96-1.04-1.01-1.00-1.59-1.54-1.45-1.52-1.49-1.81-1.70-1.79-1.65-1.86-1.63-1.55-1.56-1.62-1.52-1.94-1.78-1.92-1.84-1.79-1.60-1.63-1.58-1.68-1.59-1.61-1.55-1.77-1.60-1.67-1.89-1.91-1.80-1.83-1.81

Meanδ 1 3 c

2.27———

2.06————1.08————

1.05————

2.15————

2.53————

2.71————

2.80————

2.31————

Meanδ 1 8 o

-1.90———

-0.99————

-1.52————

-1.76————

-1.57————

-1.85————

-1.62————

-1.64————

-1.85————

lσδ1 3c

0.02———

0.14————

0.04————

0.04————

0.05————

0.12————

0.02————

0.04————

0.01————

lσδ 1 8 θ

0.07———

0.04————

0.05————

0.09————

0.05————

0.08————

0.04————

0.08————

0.05————

Notes: NOCZ refers to the Oxford in-house marble standard and is included to illustrate that reproducibilityof Hole 807C whole-rock carbonate samples was similar to the reproducibility of our calibratingstandard.

265

R.M. CORFIELD, J.E. CARTLIDGE

Era

rtia

CDh-

σ>IDoCDüCOα>ü

Epoch

CDcCDCJoCDCOCL

CCO

ü

COCOCO

65.6

66 -

66.4 -

CD

<

66.8 -

67.2 -

67.6 -

68-2 -1.5 -1 -0.5

6 C 'oo PDB-18 06 O 7oo PDB

Figure 5. Oxygen and carbon isotope chronostratigraphy of the Cretaceous/Tertiary transition at Hole 807C. Note that the δ 1 3C starts at 66.85 Mausing our age estimates, and this decline precedes the first occurrence of Tertiary planktonic foraminifers (at 66.4 Ma) by 450,000 yr. Also noteuncertainties in our time scale caused by the use of a foraminiferal datum (S. pseudobulloides) in a reworked succession.

266

WHOLE-ROCK OXYGEN AND CARBON ISOTOPE STRATIGRAPHY

APPENDIX

Oxygen and carbon isotope data from Holes 807A and 807C

Lab no.Hole, core, section,

interval (cm) δ1 3C δ 1 8 θDepth(mbsf) (Ma) Lab no.

Hole, core, section,interval (cm) δ1 3C δ 1 8 θ

Depth(mbsf)

Age(Ma)

A90/2674A90/2675A90/2676A90/2678A90/2679A90/2680A90/2681A90/2682A90/2683A90/2684A90/2686A90/2687A90/2688A90/2689A90/2690A90/2692A90/2693A90/2694A90/2695A90/2696A90/2697A90/2699A90/2713A90/2714A90/2715A90/2716A90/2717A90/2718A90/2719A90/2720A90/2721A90/2722A90/2723A90/2724A90/2725A90/2726A90/2727A90/2728A90/2729A90/2730A90/2731A90/2732A90/2734A90/2736A90/2743A90/2745A90/2746A90/2747A90/2748A90/2749A90/2750A90/2751A90/2752A90/2753A90/2754A90/2755A90/2756A90/2757A90/2758A90/2759A90/2760A90/2761A90/2762A90/2763A90/2764A90/2765A90/2766A90/2767A90/2768A90/2769A90/2770A90/2879A90/2880A90/2881A90/2882A90/2771

807A-68X-1, 138807A-68X-2, 78807A-68X-3, 61807A-68X-5, 37807 A-69X-1,75807A-70X-1, 10807A-70X-2, 108O7A-7OX-3, 10807A-70X-4, 10807A-70X-5, 10807A-70X-CC, 10807A-71X-1, 45807A-71X-2.45807A-71X-3,45807A-71X-4, 45807A-71X-CC45807A-72X-1, 42807A-72X-2, 42807A-72X-3, 42807A-72X-4, 42807A-73X-1, 70807A-73X-2, 70807A-73X-3, 70807A-73X-4, 70807A-73X-5, 72807A-73X-6, 70807 A-74X-1,92807A-74X-2, 92807A-74X-3, 92807A-75X-1, 60807A-75X-2, 60807A-75X-3, 60807A-75X-4, 60807A-75X-5, 60807A-76X-1, 70807A-76X-2, 70807A-76X-3, 70807A-76X-4, 70807A-76X-5, 70807A-76X-6, 50807A-77X-1.56807A-77X-2, 56807A-77X-3, 56807A-77X-4, 56807A-77X-5, 56807A-77X-6, 30807A-78X-1, 56807A-78X-2, 568O7A-78X-3, 56807A-78X-4, 56807A-78X-5, 56807A-79X-1, 55807A-80X-1, 53807A-80X-2, 55807A-80X-3, 55807 A-8IX-1,61807A-82X-1.75807A-82X-2, 75807A-82X-3, 77807A-82X-3, 79807A-82X-4, 79807 A-83X-1,60807A-83X-2, 60807A-83X-3, 60807A-83X-4, 60807C-2R-1, 73807C-2R-2, 73807A-84X-1, 60807A-84X-2, 60807A-84X-3, 60807A-84X-4, 60807A-84X-5, 60807A-84X-6, 60807A-85X-1, 60807A-85X-2, 60807C-4R-l,73

1.311.381.311.061.181.411.381.511.301.671.441.641.472.172.131.921.662.002.011.731.521.871.371.281.471.661.331.521.621.751.951.711.331.401.381.531.771.661.571.571.271.141.451.511.451.431.741.521.811.791.571.705.441.591.291.611.811.861.871.981.581.591.831.821.731.691.842.102.092.292.322.242.262.012.201.53

-0.09-0.17-0.10-0.18-0.07-0.56-0.17-0.15-0.24-0.04

0.070.08

-0.130.190.200.050.050.280.090.010.01

-0.490.12

-0.010.16

-0.08-0.05-0.02

0.10-0.01

0.100.07

-0.07-0.06-0.12-0.16

0.070.08

-0.090.01

-0.08-0.15-0.17

0.33-0.05-0.03

0.570.09

-0.040.360.070.10

-0.210.070.08

-0.250.160.070.040.040.150.110.23

-0.030.140.04

-0.10-0.11-0.16-0.07

0.00-0.01

0.11-0.09

0.10-0.06

641.28642.18643.51646.27650.35659.30660.80662.30663.80665.30667.36669.35670.85672.35673.85676.85678.62680.12681.62683.12688.50690.00691.50693.00694.52696.00698.42699.92701.42707.80709.30710.80712.30713.80717.60719.10720.60722.10723.60724.90727.06728.56730.06731.56733.06734.30736.76738.26739.76741.26742.76746.05755.73757.25758.75765.51775.25776.75778.27778.29779.79784.80786.30787.80789.30790.43791.93794.50796.00797.50799.00800.50802.00804.20805.70809.73

A90/2773A90/2774A90/2878A90/2775A90/2776A90/2777A90/2778A90/2779A90/2780A90/2781A90/2782A90/2783A90/2784A90/2785A90/2786A90/2787A90/2788A90/2789A90/2790A90/2791A90/2792A90/2793A90/2794A90/2795A90/2796A90/2797A90/2798A90/2866A90/2867A90/2868A90/2869A90/2870A90/2871A90/2872A90/2873A90/2874A90/2875A90/2876A90/2877A90/2811A90/2812A90/2813A90/2814A90/2815A90/2816A90/2817A90/2818A90/2819A90/2820A90/2821A90/2822A90/2823A90/2824A90/2825A90/2826A90/2827A90/2828A90/2829A90/2830A90/2831A90/2832A90/2833A90/2834A90/1936A90/1937A90/1938A90/1939A90/1940A90/1941A90/1942A90/1943A90/1944A90/1945A90/1946A90/1947A90/1948

807C-4R-2, 73807A-86X-1, 60807A-86-2, 60807C-6R-1.73807C-6R-2,73807C-6R-3, 73807C-6R-4, 73807C-6R-5, 73807C-12R-1, 35807C-15R-1, 57807C-16R-1.78807C-17R-l,76807C-17R-2, 73807C-18R-CC, 2807C-19R-1.55807C-20R-1, 1807C-21R-1, 12807C-22R-1, 12807C-23R-1.64807C-23R-2, 64807C-23R-3, 64807C-23R-4, 16807C-24R-1, 73807C-24R-2, 74807C-25R-1, 70807C-26R-1, 73807C-29R-1, 16807C-30R-2, 27807C-31R-1, 8807C-32R-1, 16807C-33R-l,2807C-34R-1.3807C-35R-1.34807C-37R-l,7807C-38R-1.4807C-39R-l,25807C-40R-1.45807C-41R-1.32807C-42R-1.74807C-43R-1.71807C-44R-1.76807C-45R-1.65807C-45R-2, 64807C-46R-1, 73807C-46R-2, 74807C-46R-3, 62807C-47R-1, 70807C-47R-2, 88807C-48R-1.20807C-48R-2, 19807C-49R-1.22807C-50R-1.21807C-51R-1.21807C-51R-2, 23807C-51R-3, 119807C-51R-4, 39807C-52R-1, 20807C-52R-2, 20807C-52R-3, 19807C-53R-1.20807C-53R-2, 20807C-53R-3, 20807C-53R-4, 20807C-54R-1, 0807C-54R-1, 15807C-54R-1.26807C-54R-1.35807C-54R-1.47807C-54R-1.56807C-54R-1.68807C-54R-1, 85807C-54R-1, 104807C-54R-1, 117807C-54R-1, 133807C-54R-1, 146807C-54R-2, 10

1.591.841.761.601.551.541.661.741.761.991.921.551.561.631.751.862.071.982.062.112.262.222.292.132.222.522.131.982.132.632.202.371.951.912.122.081.691.901.991.721.812.471.271.501.441.241.491.741.832.332.062.423.043.313.133.423.523.253.142.541.741.741.791.371.341.281.311.361.441.311.741.351.301.301.601.47

-0.24-0.02

0.03-0.12-0.15-0.10

0.04-0.08-0.10-0.66-0.80-0.73-0.62-0.71-0.74-0.80-0.67-0.99-0.96-0.80-0.76-0.91-0.67-0.61-0.83-0.52-0.49-0.64-0.73-1.02-1.22-1.15-0.92-0.97-1.11-1.03-1.13-1.25-1.23-1.77-1.36-1.58-1.39-1.39-1.31-0.89-1.97-1.96-1.99-1.93-2.10-2.23-1.95-1.99-1.82-2.04-2.18-1.97-1.81-1.71-1.54-1.77-1.37-1.73-1.76-1.73-2.01-1.95-1.60-1.78-1.51-1.69-1.76-1.80-1.13-1.75

811.23813.80815.30829.03830.53832.03833.53835.03876.95894.47899.68904.66906.13908.92914.45918.91924.02933.82939.34940.84942.34943.36944.43945.94949.10958.83987.26997.83

1006.581016.261025.421034.631044.641063.771073.641082.651092.451098.021103.141107.111116.761126.251127.741135.931137.441138.821140.901142.581145.401146.891150.421155.411160.411161.931164.391165.091170.001171.501172.991179.601181.101182.601184.071188.801188.951189.061189.151189.271189.361189.481189.651189.841189.971190.131190.261190.40

———————————————————————————————————————————————————————————————

65.7365.7465.7565.7665.7765.7765.7865.8065.8165.8265.8365.8465.86

267

R.M. CORFIELD, J.E. CARTLIDGE

Appendix (continued).

Lab no.Hole, core, section,

interval (cm) δ1 3C δ 1 8 θDepth(mbsf) (Ma) Lab no.

Hole, core, section,interval (cm) δ

1 3C δ 1 8 θDepth(mbsf)

Age(Ma)

A90/1949A90/1950A90/1951A90/1952A90/1953A90/1954A90/1955A90/1956A90/1957A90/1958A90/1959A90/1960A90/1961A90/1962A90/1963A90/1964A90/1965A90/1966A90/1967A90/1968A90/1969A90/1970A90/1971A90/1972A90/1973A90/2014A90/2015A90/2016A90/2017A90/2018A90/2019A90/2020A90/2021A90/2022A90/2023A90/2024A90/2025A90/2026A90/2027A90/2028A90/2029A90/2030A90/2031A90/2032A90/2033A90/2034A90/2035A90/2036A90/2037A90/2039A90/2041A90/2042A90/2043A90/2045A90/2046A90/2047A90/2048A90/2049A90/2050A90/2342A90/2343A90/2344A90/2346A90/2345A90/2347

807C-54R-2, 18807C-54R-2, 32807C-54R-2, 42807C-54R-2, 55807C-54R-2,62 '.807C-54R-2, 73807C-54R-2, 81807C-54R-2, 86807C-54R-2, 101807C-54R-2, 107807C-54R-2, 117807C-54R-2, 126807C-54R-2, 138807C-54R-2, 149807C-54R-3, 12807C-54R-3, 22807C-54R-3, 32807C-54R-3, 44807C-54R-3, 53807C-54R-3, 67807C-54R-3, 75807C-54R-3, 88807C-54R-3, 97807C-54R-3, 106807C-54R-3, 116807C-54R-3, 122807C-54R-3, 132807C-54R-3, 139807C-54R-3, 149807C-54R-4, 9807C-54R-4, 20807C-54R-4, 31807C-54R-4, 40807C-54R-4, 50807C-54R-4, 62807C-54R-4, 80807C-54R-4, 90807C-54R-4, 100807C-54R-4, 113807C-54R-4, 125807C-54R-4, 135807C-54R-4, 148807C-55R-1, 7807C-55R-1, 178O7C-55R-1, 26

.56

.65

.86

.701.02.70.62.65.51.56.44.42.71.78.75.34.25.21.14.29.49.51.59.37.47.03.33.36.33.64.60.60.22.75.64.81.70.52.69.83.84.76.89

1.051.20

807C-55R-1,35 2.06807C-55R-1.49 :807C-55R-1,65 :807C-55R-1,76 :807C-55R-1,97 :807C-55R-1, 118807C-55R-2, 12807C-55R-2, 22807C-55R-2, 34807C-55R-2, 43807C-55R-2, 50807C-55R-2, 56807C-55R-2, 64807C-55R-2, 77807C-55R-3, 12807C-55R-3, 30807C-55R-3, 38807C-55R-3, 51807C-55R-3, 59807C-55R-3, 71

2.08

1.102.00

1.041.032.042.012.272.102.172.202.232.202.252.312.242.332.362.46

- .26-1.35-1.51-1.63-0.78-1.69-1.52-1.49-

-

_

___

.75

.69

.32

.45

.71

.72

.87

.66

.68

.84-1.55-1.68-1.64-1.69-1.83-1.72-1.14-1.74-1.61- .93

r 1.86-1.68-1.72

____;_;

.95

.81

.72

.87

.74

.85

.46

.76

.86

.10

.65

.60-1.81-1.51-1.89-1.80-1.62-1.75-1.78-1.81-1.91-1.74-1.69-1.57-1.80-1.67-1.66-1.47___

__

.68

.60

.68

.83

.73

.56

1190.481190.621190.721190.851190.921191.031191.111191.161191.311191.371191.471191.561191.681191.791191.921192.021192.121192.241192.331192.471192.551192.681192.771192.861192.961193.021193.121193.191193.291193.391193.501193.611193.701193.801193.921194.101194.201194.301194.431194.551194.651194.781196.971197.071197.161197.251197.391197.551197.661197.871198.081198.521198.621198.741198.831198.901198.961199.041199.171200.021200.201200.281200.411200.491200.61

65.8665.8765.8865.8965.9065.9065.9165.9165.9365.9365.9465.9565.9665.9665.9765.9865.9966.0066.0166.0266.0266.0366.0466.0566.0666.0666.0766.0766.0866.0966.1066.1166.1166.1266.1366.1566.1566.1666.1766.1866.1966.2066.3766.3866.3966.3966.4166.4266.4366.4466.4666.4966.5066.5166.5266.5266.5366.5466.5566.6166.6366.6366.6466.6566.66

A90/2348A90/2349A90/2350A90/2351A90/2352A90/2353A90/2354A90/2355A90/2356A90/2357A90/2358A90/2359A90/2360A90/2361A90/2380A90/2381A90/2382A90/2383A90/2835A90/2836A90/2837A90/2838A90/2839A90/2840A90/2841A90/2842A90/2844A90/2865A90/2384A90/2385A90/2386A90/2387A90/2388A90/2389A90/2390A90/2391A90/2392A90/2393A90/2394A90/2395A90/2396A90/2397A90/2398A90/2399A90/2400A90/2401A90/2402A90/2403A90/2404A90/2405A90/2406A90/2407A90/2408A90/2409A90/2487A90/2488A90/2489A90/2490A90/2491A90/2492A90/2493A90/2494A90/2495A90/2496

807C-55R-3, 85807C-55R-3, 103807C-55R-3, 112807C-55R-3, 124807C-55R-3, 133807C-55R-3, 143807C-55R-4, 11807C-55R-4, 21807C-55R-4, 37807C-55R-4, 49807C-55R-4, 63807C-55R-4, 73807C-55R-4, 85807C-55R-4, 98807C-55R-4, 110807C-55R-4, 120807C-55R-4, 130807C-55R-4, 141807C-56R-1.20807C-56R-2, 20807C-56R-3, 20807C-57R-1, 21807C-57R-2, 21807C-58R-1, 20807C-59R-1, 34807C-59R-2, 46807C-61R-1, 110807C-61R-2, 112807C-62R-1, 35807C-62R-2, 34807C-62R-3, 41807C-63R-1, 81807C-63R-2, 81807C-63R-3, 81807C-63R-4, 85807C-64R-1, 121807C-64R-2, 121807C-64R-3, 39807C-65R-l,58807C-65R-2, 60807C-66R-l,55807C-66R-2, 55807C-66R-3, 55807C-67R-1, 132807C-67R-2, 132807C-67R-3, 132807C-67R-4, 125807C-67R-5, 47807C-68R-1.77807C-68R-2, 50807C-68R-3, 26807C-69R-l,58807C-69R-2, 56807C-69R-3, 57807C-69R-4, 65807C-69R-5, 70807C-70R-1, 46807C-70R-2, 89807C-70R-3, 9,807C-70R-4, 75807C-70R-5, 28807C-71R-1, 67807C-71R-2, 36807C-71R-3, 28

2.352.452.502.522.542.262.392.542.722.662.672.692.852.752.452.542.642.672.752.872.793.013.033.092.852.922.962.952.872.922.903.043.012.983.013.012.972.883.013.103.173.143.082.922.982.973.042.942.923.043.073.053.043.073.073.173.153.253.213.223.193.173.103.12

- .67-1.72-1.68-1.57-1.52-2.26-1.83-1.67-1.67-1.64-1.76-1.59-1.58-1.72-2.03-1.86-1.91-1.72-1.81-1.64-1.75-1.60-1.77-1.69-1.61-1.65-1.73-1.70-1.68-1.51-1.77-1.47-1.51-1.76-1.44-1.67-1.72-1.74-1.80-1.67

--

-

---

.71

.74

.83

.86

.76

.82

.72

.83

.79

.68

.66

.71

.76-1.70-1.97-1.85-2.03-1.89-1.95-1.94-1.77-1.85-2.02_ .84

1200.751200.931201.021201.141201.231201.331201.511201.611201.771201.891202.031202.131202.251202.381202.501202.601202.701202.811206.801208.301209.801216.511218.011222.701232.541234.161252.601254.121261.551263.041264.611271.611273.111274.611276.151281.711283.211283.891290.681292.201300.351301.851303.351310.821312.261313.761315.191315.911319.871321.101322.361329.381330.861332.371333.951335.501338.861340.791341.491343.651344.681348.671349.861351.28

66.6766.6866.6966.7066.7166.7266.7366.7466.7566.7666.7766.7866.7966.8066.8166.8266.8266.8367.1567.2667.3867.91

—————————————————————————————————————————

268