22. paleoenvironmental results from north atlantic sites 607 and 609

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22. PALEOENVIRONMENTAL RESULTS FROM NORTH ATLANTIC SITES 607 AND 609 1 William F. Ruddiman, Lamont-Doherty Geological Observatory Andrew Mclntyre, Lamont-Doherty Geological Observatory, and Queens College of the City University of New York and Maureen Raymo, Lamont-Doherty Geological Observatory 2 ABSTRACT Detailed CaCO 3 analyses from Leg 94 Sites 607 and 609 confirm earlier findings from Leg 81 that large-scale North- ern Hemisphere glaciation began near the Gauss/Matuyama boundary. At Site 609, the first ice-rafted sand occurs be- tween samples at 2.55 and 2.45 Ma, or effectively coincident with the Gauss/Matuyama paleomagnetic boundary. Al- though small to moderate decreases in the CaCO 3 percentage from maxima in the lower Pliocene began at 3.15 Ma, the lack of ice-rafted debris until 2.55 Ma suggests that this decline must be explained by other factors, particularly dissolu- tion. The records at Sites 607 and 609 show an increase in the amplitude of CaCO 3 variations in the last million years. Counts of planktonic foraminifers reveal complex changes in estimated sea-surface temperature (SST) through the last 1.90 m.y., including long-term trends with wavelengths of several hundred thousand years and rhythmic changes with wavelengths of several tens of thousands of years. Relatively warm conditions prevailed until 1.05 Ma, and the low- est SST values of the Pleistocene in this area occurred near 0.8 and 0.7 Ma. In several instances, unusually low glacial temperatures were immediately followed by unusually high temperatures in the succeeding interglaciation. INTRODUCTION Leg 94 was designed primarily as a north-south tran- sect for paleoenvironmental study of the North Atlantic from the northern part of the modern subtropical gyre to the east-central portion of the subpolar gyre. We have focused initial efforts in this study on two of the six sites cored: 607 and 609 (Fig. 1). Analysis of upper Quater- nary piston cores at the locations of these two sites has shown a strong development of the basic orbital rhythms at 23,000, 41,000, and 100,000 yr. in records of North Atlantic sea-surface temperature (SST) change (Ruddi- man and Mclntyre, 1984). We thus chose these two sites to trace the rhythms of sea-surface change into earlier periods, as well as to examine the long-term history of CaCO 3 deposition in the North Atlantic, and the inferred glacial history on the surrounding continents. We report detailed 3.5-m.y. records of CaCO 3 from both sites, as well as a 1.90-m.y. record of oxygen and carbon isotopic values, planktonic foraminiferal counts, and estimated sea-surface temperatures from Site 607. CaCO 3 VARIATIONS AT SITES 607 AND 609 (3.5-0 Ma) CaCO 3 analyses of Site 609 samples were carried out at 30-cm intervals, equivalent to a mean sample interval of about 4000 yr. Analyses of Site 607 samples were per- formed at 15-cm intervals, equivalent to a time interval Ruddiman, W. R, Kidd, R. B., and Thomas, E., et al., Init. Repts. DSDP, 94: Wash- ington (U.S. Govt. Printing Office). 2 Addresses: (Ruddiman and Raymo) Lamont-Doherty Geological Observatory and De- partment of Geological Sciences of Columbia University, Palisades, New York 10964; (Mcln- tyre) Lamont-Doherty Geological Observatory and Department of Geological Sciences of Co- lumbia University, Palisades, New York 10964, and Queens College of the City University of New York, Flushing, New York 11367. of about 3500 yr. The data are shown in Figure 2 and listed in Appendix A (Site 609) and B (Site 607). All measurements were made using the gasometric technique of Hulsemann (1966). Replicate analyses indicate a pre- cision of 1-2%. As indicated in Figure 2, the record at Site 609 was compiled by splicing analyses from Holes 609 and 609B. This was necessary to overcome large gaps caused by complications in the coring process (Ruddi- man et al., this volume). Both CaCO 3 records are plotted versus time in Figure 3. The time scales at Sites 609 and 607 are based on linear interpolation between available paleomagnetic datum lev- els (Clement and Robinson, this volume). These time scales are preliminary and will be adjusted in future work. Also shown plotted versus time in Figure 3 is the CaCO 3 record from Hole 552A (Shackleton et al., 1984; Zim- merman et al., 1985). All three records show the most marked change in CaCO 3 near the boundary between the Gauss and Ma- tuyama magnetic chrons at 2.47 Ma, with large-ampli- tude variations in carbonate percentage beginning at this level. This represents the first major development of gla- cial conditions in the subpolar gyre, including the initial delivery of ice-rafted detritus (Shackleton et al., 1984). However, the relative importance of this change in Ca- CO 3 percentage varies from site to site. At Hole 552A, negligible CaCO 3 variations occurred through most of the Gauss (as reported in Shackleton et al., 1984), followed by a pair of short CaCO 3 minima at about 2.55 Ma, and then at 2.4 Ma by a much more pro- nounced minimum that marks the beginning of large- scale CaCO 3 fluctuations. At Site 607, small variations (5°7o or less) were char- acteristic for a long interval prior to 3.15 Ma. A drift to- ward slightly lower CaCO 3 values began around 3.15 Ma, 855

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Page 1: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

22. PALEOENVIRONMENTAL RESULTS FROM NORTH ATLANTIC SITES 607 AND 6091

William F. Ruddiman, Lamont-Doherty Geological ObservatoryAndrew Mclntyre, Lamont-Doherty Geological Observatory, and Queens College of the City

University of New Yorkand

Maureen Raymo, Lamont-Doherty Geological Observatory2

ABSTRACT

Detailed CaCO3 analyses from Leg 94 Sites 607 and 609 confirm earlier findings from Leg 81 that large-scale North-ern Hemisphere glaciation began near the Gauss/Matuyama boundary. At Site 609, the first ice-rafted sand occurs be-tween samples at 2.55 and 2.45 Ma, or effectively coincident with the Gauss/Matuyama paleomagnetic boundary. Al-though small to moderate decreases in the CaCO3 percentage from maxima in the lower Pliocene began at 3.15 Ma, thelack of ice-rafted debris until 2.55 Ma suggests that this decline must be explained by other factors, particularly dissolu-tion. The records at Sites 607 and 609 show an increase in the amplitude of CaCO3 variations in the last million years.

Counts of planktonic foraminifers reveal complex changes in estimated sea-surface temperature (SST) through thelast 1.90 m.y., including long-term trends with wavelengths of several hundred thousand years and rhythmic changeswith wavelengths of several tens of thousands of years. Relatively warm conditions prevailed until 1.05 Ma, and the low-est SST values of the Pleistocene in this area occurred near 0.8 and 0.7 Ma. In several instances, unusually low glacialtemperatures were immediately followed by unusually high temperatures in the succeeding interglaciation.

INTRODUCTION

Leg 94 was designed primarily as a north-south tran-sect for paleoenvironmental study of the North Atlanticfrom the northern part of the modern subtropical gyreto the east-central portion of the subpolar gyre. We havefocused initial efforts in this study on two of the six sitescored: 607 and 609 (Fig. 1). Analysis of upper Quater-nary piston cores at the locations of these two sites hasshown a strong development of the basic orbital rhythmsat 23,000, 41,000, and 100,000 yr. in records of NorthAtlantic sea-surface temperature (SST) change (Ruddi-man and Mclntyre, 1984). We thus chose these two sitesto trace the rhythms of sea-surface change into earlierperiods, as well as to examine the long-term history ofCaCO3 deposition in the North Atlantic, and the inferredglacial history on the surrounding continents.

We report detailed 3.5-m.y. records of CaCO3 fromboth sites, as well as a 1.90-m.y. record of oxygen andcarbon isotopic values, planktonic foraminiferal counts,and estimated sea-surface temperatures from Site 607.

CaCO3 VARIATIONS AT SITES 607 AND 609(3.5-0 Ma)

CaCO3 analyses of Site 609 samples were carried outat 30-cm intervals, equivalent to a mean sample intervalof about 4000 yr. Analyses of Site 607 samples were per-formed at 15-cm intervals, equivalent to a time interval

Ruddiman, W. R, Kidd, R. B., and Thomas, E., et al., Init. Repts. DSDP, 94: Wash-ington (U.S. Govt. Printing Office).

2 Addresses: (Ruddiman and Raymo) Lamont-Doherty Geological Observatory and De-partment of Geological Sciences of Columbia University, Palisades, New York 10964; (Mcln-tyre) Lamont-Doherty Geological Observatory and Department of Geological Sciences of Co-lumbia University, Palisades, New York 10964, and Queens College of the City University ofNew York, Flushing, New York 11367.

of about 3500 yr. The data are shown in Figure 2 andlisted in Appendix A (Site 609) and B (Site 607). Allmeasurements were made using the gasometric techniqueof Hulsemann (1966). Replicate analyses indicate a pre-cision of 1-2%. As indicated in Figure 2, the record atSite 609 was compiled by splicing analyses from Holes609 and 609B. This was necessary to overcome large gapscaused by complications in the coring process (Ruddi-man et al., this volume).

Both CaCO3 records are plotted versus time in Figure 3.The time scales at Sites 609 and 607 are based on linearinterpolation between available paleomagnetic datum lev-els (Clement and Robinson, this volume). These timescales are preliminary and will be adjusted in future work.Also shown plotted versus time in Figure 3 is the CaCO3

record from Hole 552A (Shackleton et al., 1984; Zim-merman et al., 1985).

All three records show the most marked change inCaCO3 near the boundary between the Gauss and Ma-tuyama magnetic chrons at 2.47 Ma, with large-ampli-tude variations in carbonate percentage beginning at thislevel. This represents the first major development of gla-cial conditions in the subpolar gyre, including the initialdelivery of ice-rafted detritus (Shackleton et al., 1984).However, the relative importance of this change in Ca-CO3 percentage varies from site to site.

At Hole 552A, negligible CaCO3 variations occurredthrough most of the Gauss (as reported in Shackleton etal., 1984), followed by a pair of short CaCO3 minima atabout 2.55 Ma, and then at 2.4 Ma by a much more pro-nounced minimum that marks the beginning of large-scale CaCO3 fluctuations.

At Site 607, small variations (5°7o or less) were char-acteristic for a long interval prior to 3.15 Ma. A drift to-ward slightly lower CaCO3 values began around 3.15 Ma,

855

Page 2: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

70° 60° 50° 40° 30°

40"

60° 10c

Figure 1. Locations of cores cited in text. Site 607 and Piston Core V30-97 are located at 41°00'N, 32°58'W (3427 m). Site 609 is located at49°53'N, 24°14'W (3883 m). Site 552 is located at 56°03'N, 23°14'W. Piston Core K708-7 is located at 53°56'N, 24°05'W.

with a doubling in the amplitude of variation to about10% at 2.7 Ma. The first major carbonate minimum oc-curred at 2.45 Ma, with a series of comparably strongCaCO3 oscillations (25%) continuing until 1.95 Ma. Theamplitude of CaCO3 variations then decreased somewhat,varying erratically between 15 and 25% from 1.9 to1.35 Ma before returning to intermediate (25%) ampli-tudes from 1.35 to 0.8 Ma. Large-amplitude changes(40-50%) began at 0.8 Ma and continued through therest of the Pleistocene.

At Site 609, a similar late Pliocene increase in the am-plitude of CaCO3 variations occurred, with variationsof less than 5% prior to 3.15 Ma, increasing to 15% to20% by 2.6 Ma. This was, however, superimposed upon adrift toward lower mean CaCO3 values during this inter-val. More striking CaCO3 oscillations of 30% occurredat and after 2.55 Ma, followed by somewhat erratic butlarge-amplitude variations (50% or more) until about0.85 Ma. The last 0.85 m.y. have been characterized bylarge-amplitude CaCO3 variations (exceeding 70%).

Several features of these records require comment. Wewill focus this discussion on three intervals during whichimportant changes are evident in one or more of the Ca-CO3 records: (1) the interval from 3.15 to 2.55 Ma, dur-ing which two of the three records show declining Ca-CO3 values; (2) the abrupt beginning of strong, periodicCaC03 variations, and particularly the deeper CaCO3

minima, around 2.55 to 2.47 Ma; and (3) the increase inamplitude of CaCO3 oscillations in the last 0.85 m.y.

CaCO3 changes in this area during the late Pleisto-cene were mainly caused by variable suppression of bio-genic productivity due to salinity stratification and seaice (Ruddiman and Mclntyre, 1976), and by variable de-position of ice-rafted detritus (Ruddiman, 1977). In or-der to explain the very large late Quaternary changes inCaCO3 content without comparably large changes in sed-imentation rate in most North Atlantic cores, the effectsof these two factors on the flux of sediment to the sea-floor must generally be opposed and nearly balancedthrough time.

Dissolution of CaCO3 is generally regarded as a sec-ond-order factor in the high-amplitude CaCO3 changesof the late Pleistocene North Atlantic. However, for thesmaller-amplitude CaCO3 variations in the earlier partsof the Pleistocene and late Pliocene, dissolution may playa first-order role and must be considered.

The three sites have different CaCO3 responses acrossthe interval from 3.15 to 2.55 Ma. The strongest responseis the marked drift to lower values at deep Site 609(3883 m). The drift to lower values is more subtle at theintermediate Site 607 (3427 m) and there is no drift atthe shallow Site 552 (2311 m). This progression suggeststhat the trend toward lower CaCO3 from 3.15 to 2.55 Mais largely a result of depth-dependent dissolution.

856

Page 3: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

Site 607

PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

Site 609CaCO^

100

609B

609B

150 -

175 "-

270 "–

Figure 2. Variations in CaCO3 percentage at Sites 607 and 609 plotted versus sub-bottom depth. Note the expandedamplitude scale for the CaCO3 values at Site 607.

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Page 4: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

Site 607CaCOg (%)

Site 609CaCO

100 0

Site 552(Hole 552A)

CaCO3 (%)50 100

3.5 -

4.0 L

Figure 3. Variations in CaCO3 percentage at Sites 607, 609, and 552 plotted against time. Hole 552A data are from Shack-leton et al. (1984) and Zimmerman et al. (1985).

858

Page 5: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

We examined the sand fraction (coarser than 0.062 mm)of those samples at Sites 609 and 607 with the lowestCaCO3 values in the interval from 3.15 to 2.55 Ma. Wefound no ice-rafted grains in any sample below the2.55-Ma level. The only noncarbonate detritus presentin the coarse fraction was pyrite. This eliminates dilu-tion by ice rafting as a causal factor of the gradual Ca-CO3 drift. At this point it is not possible to eliminateproductivity suppression as an explanation, but the depth-dependent trends argue that dissolution is the primaryfactor. It is also possible that an increased local influx toSite 609 of fine detritus derived from nearby Maury Chan-nel (Ruddiman, 1972) reduced the carbonate percent-ages at this site during the Gauss chron.

Thus our results confirm the observation first madeby Shackleton et al. (1984) that the initiation of majorNorthern Hemisphere glaciation occurred near the Gauss/Matuyama boundary. The first substantial reductions inCaCO3 and minor influxes of ice-rafted sand occurredjust below the paleomagnetic boundary between 2.57 and2.55 Ma in all three records, but it is only at or justabove the Gauss/Matuyama boundary at 2.47 Ma thatabundant ice-rafted sand appears. All three sites recorddeep CaCO3 minima with abundant ice-rafted sand grainsjust after 2.47 Ma. This change affected the entire east-central North Atlantic from 56°N southward to 41 °N,the effective southern limit of abundant ice rafting dur-ing the Pleistocene (Ruddiman, 1977).

The three sites also show interesting differences inCaCO3 trends during the later Pleistocene (late Matuya-ma and early Brunhes chrons). There is an increased am-plitude of variation during the last 0.8 m.y. at Site 607(especially in the late Matuyama and early Brunhes), asimilar but somewhat less obvious increase in CaCO3

variations during the last 0.85 m.y. at Site 609, and, incontrast, a decrease in range of CaCO3 changes at Site552 during the last 0.6 m.y. This pattern suggests thatthe very large-scale ice-volume oscillations that occurredin the Brunhes epoch (Shackleton and Opdyke, 1973)tended to send ice-rafted debris farther south than thosein the Matuyama, thus shifting the largest relative im-pact to the south (Site 607) and depressing the relativeimpact farther north (Site 552). Kent et al. (1971) alsofound higher percentages of ice-rafted sand in the NorthPacific during the last million years than in the earlierMatuyama. This trend during the last million years couldalso reflect a relatively increased role of the Laurentideice sheet, which would probably have the largest impactat westernmost Site 607 and the smallest effect at east-ernmost Site 552.

OXYGEN ISOTOPIC VARIATIONS AT SITE 607(1.80-0 Ma)

Benthic foraminifers were picked for oxygen isotopeanalysis from the same suite of samples run for CaCO3

percentage at 4500-yr. intervals (on the average) over thetime span from 1.80 Ma to the present. The two speciesused were Uvigerina peregrina and Cibicides (also knownas Planulina) wuellerstorfi. Uvigerina is assumed to bein oxygen isotopic equilibrium with ambient sea water;Cibicides is adjusted by +O.64%o to bring it into pre-

sumed equilibrium (Shackleton, 1977). The unadjustedvalues are listed in Appendix C. Figures 4, 5, and 6show adjusted values. For the upper part of the records(above the oxygen isotopic stage 8/7 boundary in Figs. 5and 6), we plotted previously published oxygen isotopicvalues measured in Piston Core V30-97 at the same lo-cation as Site 607 (Ruddiman and Mclntyre, 1981).

The isotopic data from Site 607 are plotted versus sub-bottom depth in Figure 4. All major oxygen isotopicstages from stages 8 to 22 are clearly visible. In general,their relative amplitudes are comparable to those in thestacked isotopic record published in Imbrie et al. (1984).For example, glacial stages 12 and 16 have the heaviestδ 1 8θ values. Stages 11 and 12 appear to occur twice inthe section because of double coring (Ruddiman, Ca-meron, and Clement, this volume).

The absolute amplitude of the isotopic signal fromSite 607 is very large (~2.5%o). This may result in partfrom splicing together data from two core sites. How-ever, the fact that the amplitudes are still unusually largewithin each of the two parts of the record indicates thatchanges in bottom-water temperature have significantlyoverprinted the ice-volume fluctuations at this site.

A preliminary time scale for the spliced record of CoreV30-97 and Site 607 was derived from oxygen isotopicand paleomagnetic data. For the upper 0.25 m.y. (spannedby Core V30-97), we used the time scale published byRuddiman and Mclntyre (1984). For the interval below0.25 Ma in the record from Site 607, we interpolatedages between the isotopically defined 0.25-Ma level andthe paleomagnetic boundaries from Clement and Rob-inson (this volume). Oxygen isotopic data plotted to thistime scale and spanning the last 1.0 Ma are shown inFigures 5 and 6.

PLANKTONIC FORAMINIFERAL VARIATIONSAT SITE 607 (1.90-0 Ma)

Figure 4 shows percentage abundance fluctuations offour key species of planktonic foraminifers over the up-per 85 m of record at Site 607. The counts are based onaliquots averaging slightly over 300 individuals larger than0.149 mm from samples taken every 15 cm, equivalentto a time interval of about 3500 yr. All counts are listedin Appendix C. The same data are plotted in Figure 5 tothe time scale described in the last section. The Site 607counts extend from 0.25 to 1.90 Ma (Fig. 5). For theportion of the record above 0.25 Ma in Figure 5, weshow counts from Core V30-97 (Ruddiman and Mcln-tyre, 1981).

Particularly noteworthy among the trends shown inFigure 5 are: (1) the pulses of increased abundance ofthe cold, polar-water indicator Neogloboquadrina pachy-derma (sinistral, or left-coiling) between 1.05 and 0.8 Ma,and at 0.68 Ma, 0.45 Ma, and 0.35 Ma, with intervals ofnear-zero abundance between 1.9 and 1.7 Ma and be-tween 1.25 and 1.1 Ma and generally lower percentagesbetween 0.65 and 0.47 Ma and between 0.34 and 0.07 Ma;(2) a progressive increase in the abundance of the coolsubpolar species Globigerina bulloides throughout thelength of the record; (3) large variations of the temper-ate North Atlantic Drift indicator, Globorotalia inßata,

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Page 6: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

1 Q „ Neogloboquadrina Globigerina Globorotalia Globigerinoidesδlöθ(°/oo) pachyderma s. (%) bulloides (%) inflate (%) ruber (%) Other (/o)

,5.00 2.50 0 80 0 40 0 40 0 25 0 80

Page 7: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

Figure 4. Percentage abundance of four species of planktonic foraminifers and percentage abundance of all other species combined, plotted versus sub-bottom depth at Site 607 over the last 1.9m.y. Also shown are oxygen isotopic data from Site 607 based on values derived from benthic foraminifers Uvigerina (•) and Cibicides (A); values in parentheses were not included in the con-tinuous record (the solid line). Numbers are δ 1 8θ stage designations.

Page 8: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

V30-97/Site 607

1 R Neogloboquadrina Globigerina Globorotalia Globigerinoidesδ'öO(°/oo) pachyderma s. (%) bulloides (%) inflata (%) ruber {%) Other (%)

5.50 2.50 0 80 0 60 0 40 0 25 10 80n nn • • * • _ • • . _ * . . , . . _ _ ^ _ _ ^ ^ _ ^ _ ^ ^ _

Page 9: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

Figure 5. Percentage species abundance and oxygen isotopic data from Site 607 and Core V30-97 spliced at 0.25 Ma and plotted against time.

Page 10: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

with generally somewhat reduced values after 1.1 Ma,and a suggestion of lower values prior to 1.8 Ma; and(4) a reduction in the mean abundance and range of var-iation of the warm subtropical species Globigerinoidesruber (white) after 0.95 Ma, except for a few very largemaxima in the Brunhes chron.

No-analog abundances do not occur in the speciespercentage data from the samples in this record (Figs. 4,5). Ruddiman, Shackleton, et al. (in press) have foundno-analog faunas in the > 1.2 to 1.1 Ma interval fromHole 552A about 1700 km to the north-northeast ofSite 607 (Fig. 1). During portions of this interval, G. in-flata percentages at Hole 552A exceeded by 5 to 10%the 40% maximum range found in North Atlantic coretops (Kipp, 1976). Throughout the same interval, N.pachy derma (s.) values dropped to nearly zero at Hole552A. Because of a record gap between 1.4 and 1.2 Maat Hole 552A, it was not possible to define the begin-ning of this anomalous interval at that site, other thanto constrain it as older than 1.2 Ma and younger than1.4 Ma. In the record at Site 607, G. inflata values stayedwithin the 40% limit from 1.2 to 1.1 Ma, so that a no-analog condition was not attained. N. pachyderma (s.)percentages from Site 607 indicate that the interval ofnear-zero abundance lasted from 1.25 to 1.1 Ma. A simi-lar interval occurred prior to 1.7 Ma (see also Raymo,Ruddiman, and Clement this volume).

SEA-SURFACE TEMPERATURE VARIATIONS ATSITE 607 (1.90-0 Ma)

Estimated winter sea-surface temperature over the last1.90 m.y. at Site 607 based on the counts shown in Fig-ures 4 and 5 are shown plotted versus time in Figure 6.These estimates (listed in Appendix C) are based on re-cently developed transfer function F13×5 (Ruddimanand Esmay, this volume). This transfer function was de-vised specifically to deal with the large number of sam-ples required to analyze HPC records in detail. It re-quires the recognition of just the four species shown inFigures 4 and 5, and all remaining species are lumpedinto a fifth category—"Other".

Although the statistical measures of equation perform-ance are inevitably degraded somewhat from those ofthe widely used North Atlantic equation F13 of Kipp(1976), the standard errors of estimate (2.2°C in sum-mer and 1.9°C in winter) are still relatively small for anarea where the total range of Quaternary SST variationis in excess of 15°C. The new equation captures the ma-jor trends and basic rhythms of cyclical SST change inthe late Pleistocene as well as the full F13 equation inthis area (Ruddiman and Esmay, this volume).

For the upper 0.25 m.y. of record shown in Figure 6,the sea surface temperature in winter (SSTw) estimatesare based on the counts in Core V30-97 published byRuddiman and Mclntyre (1981, 1984). In order to makethese data consistent with the Site 607 counts, they werereprocessed through transfer function F13×5, whichrecognizes only the reduced number of species mentioned.Only the winter-season (SSTw) estimates are shown, be-cause this was the best-simulated season and because thetrends in both seasons are quite similar.

The SSTw curves at Site 607 (Fig. 6) are complex, withsignificant variations apparent at both very long and rel-atively short wavelengths. A prolonged warm intervaloccurred prior to 1.05 Ma, but with significant varia-tions at both long and short wavelengths. A trend is ap-parent at the longer (500,000-600,000 yr.) wavelengthfrom intermediate temperatures at the bottom of the re-cord (1.90 Ma) to an SST maximum at around 1.65-1.60 Ma, an SST minimum at about 1.40-1.30 Ma, andan SST maximum centered at about 1.15-1.10 Ma, pri-or to a prominent step-function cooling at around 1.0 Ma.

The part of the long-wavelength structure showingwarmth before 1.7 Ma and between 1.25 and 1.1 Mamay be due to bias in the transfer function: these are theintervals in which Neogloboquadrina pachyderma (s.) isabsent. Farther north, this absence creates severe no-an-alog conditions at Site 552 (Ruddiman et al., in press).Because N. pachyderma (s.) is less abundant at Site 607even in most peak-glacial intervals, its absence appearsonly to impart a small warm bias to the SST estimateswithout totally invalidating the use of the transfer func-tion.

Shorter-period variations around 40,000 yr. during theMatuyama are superimposed on these longer-term SSTwchanges and are also evident in the CaCO3 record. Re-cent analysis of both SSTw and CaCO3 percentage forthe Site 607 record between 2.47 and 0.735 Ma shows avery powerful concentration of variance at the orbitalobliquity period of 41,000 yr. (Ruddiman, Raymo, et al.,in press).

The abrupt shift to colder conditions after 1.0 Maand the positioning of the coldest estimates in the 0.8-0.7 Ma section of Figure 6 do not reflect bias in thetransfer function. The CaCO3 record from Site 607 in-dependently shows nearly identical trends, indicating thatthis is a valid local climatic signal. Pulses of increasinglylow SSTw values occurred from 1.05 to 0.8 Ma, and againat 0.68 Ma, with relative warmth from 0.67 to 0.5 Ma,and periodic coolings after 0.5 Ma.

The strongest cold pulses in the record younger than1.05 Ma are coincident with maxima in the polar speciesN. pachyderma (s.) (Figs. 4, 5). Some of the more mod-erate cold pulses are correlated with maxima in Globi-gerina bulloides, although the link between this speciesand the SST estimates is otherwise not very strong.

The general prevalence of warmth prior to 0.95 Ma,as well as the scattered pulses of extreme warmth in thegenerally colder interval after that date, are both linkedto high abundances of the subtropical species G. ruber(Figs. 4, 5). Values of that species in excess of 15% andranging up to 25% produce SST estimates in excess of24°C and ranging up to 26.5°C.

One interesting trend in the SST curve is the tendencyfor the lowest SST estimates late in several of the glacialisotopic stages to be immediately followed by the high-est SST estimates early in the succeeding interglacial iso-topic stages (Fig. 6). This occurs most notably at the fol-lowing isotopic stage boundaries: 10/9 (0.337 Ma); 12/11 (0.421 Ma); 18/17 (0.687 Ma); and 22/21 (0.788 Ma),but it is also evident at the 6/5 boundary (0.127 Ma).Although a small part of this pattern is related to inade-

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PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

quacies in the transfer function used to make the SSTwestimates (Ruddiman and Esmay, this volume), the strik-ing percentage changes in the cold-indicator species N.pachyderma (s.) and warm indicator G. ruber (Figs. 5, 6)confirm that extremes of warmth immediately followedextremes of cold.

Finally, the SSTw curve at Site 607 differs rather strik-ingly from that at Hole 552A, also shown in Figure 6.Except for the previously mentioned no-analog condi-tions from 1.2 to 1.1 Ma at Hole 552A, the curve atHole 552A tends to oscillate repetitiously between simi-lar extremes of warmth and cold. The range of SST os-cillation at Hole 552A increased progressively from thesmaller variations typical a million years ago to the larg-er variations of the last 0.45 m.y., but this increase inamplitude was slow and gradual.

In contrast, the SST record at Site 607 is abruptlypunctuated by unusually cold and warm pulses; it showsoscillations at very long wavelengths; and it is subject tolarger base-line shifts from one range of variation to an-other. All of these effects create a more complex patternthan the more rhythmic trends evident at Hole 552A.

Several features in the CaCO3 curve at Site 607 aresimilar to those in the SSTw curve (Fig. 6). The unusu-ally deep CaCO3 minima in oxygen isotopic stages 22,18, 12, and 10 match the unusually cold SST estimatesat those levels, although the CaCO3 minimum in stage10 lacks the full intensity of the SSTw minimum. Thesestrong carbonate minima thus validate the unusually coldSSTw values.

CORING PROBLEMS

Although the data reported here for Sites 607 and 609are valid when plotted against sub-bottom depth in eachhole at each site, the time series plots are not final. Sev-eral problem areas must be examined more closely be-fore the records of CaCO3, δ 1 8 θ , foraminiferal speciespercentages, and estimated SST can be accepted as ac-curate time series and analyzed with the standard signal-processing techniques (spectral analysis, filtering, coher-ency and cross-correlation analysis).

The major problem is the existence of gaps in the rec-ord at breaks between cores. Correlation lines shown inRuddiman et al. (this volume) suggest that 75 cm or moreof material may be missing across some core breaks atthese sites. At the mean Pleistocene sedimentation ratesof 45 and 75 m./m.y. at Sites 607 and 609, this wouldequate to maximum time gaps at the core breaks of about17,000 yr. at Site 607 and 10,000 yr. at Site 609. Thesegaps are being rectified by sampling comparable sec-tions in the alternate holes at these sites.

DISCUSSION

Site 607 is located beneath surface waters with thelargest temperature changes (glacial to interglacial rang-es of 12 to 15 °C) in the world during the late Pleistocene(CLIMAP, 1981; Ruddiman and Mclntyre, 1984). The1.90-m.y. SSTw record of the entire Pleistocene shownin Figure 6 indicates even larger changes of up to 20°C.The relative warmth indicated for most of the Matuya-ma chron is not surprising; oxygen isotopic evidence sug-

gests smaller ice volume (both mean and glacial-maxi-mum values) at that time (Shackleton and Opdyke, 1973).

Although the faunal and SST time series in Figures 5and 6 are not final, the pulses of very cold SSTw at roughly0.8 Ma (isotopic stage 22) and 0.68 Ma (stage 18) meritadditional comment, because they far exceed the lowestglacial SST values observed in the two large-scale glacialcycles of the last 250,000 yr. The cold pulses at 0.45 Ma(stage 12) and 0.35 Ma (stage 10) are also slightly largerthan the late Pleistocene glacial values.

We do not believe that these SST estimates are erro-neous. The raw species data in Figure 5 are consistentwith the estimated SSTw values, with very high N. pachy-derma (s.) percentages (as much as 90%) requiring verylow temperatures. In addition, the cold SST pulses arecorroborated by correlative lows in the CaCO3 percent-age (Fig. 6). Similarly, the high G. ruber percentages (asmuch as 25%) following some of the succeeding degla-ciations (Fig. 5) require high interglacial SST values.

Following the line of reasoning used by Ruddiman andMclntyre (1981, 1984) to explain the climatic responseof North Atlantic surface waters over the last 250,000 yr.,the origin of these cold-warm pulses probably lies inone of two factors: (1) changes in forcing of the high-latitude ocean by nearby ice sheets or (2) changes in north-ward advection of warm tropical and subtropical sur-face waters due to climatic interactions that are physi-cally remote from the ice sheets.

From evidence in Ruddiman and Mclntyre (1984), ice-sheets can force the North Atlantic response in two ways:(1) at latitudes north of 50°N, via the immediate effectsof the ice on the atmosphere, and of the cold lower-at-mospheric winds on the surface ocean (Manabe and Broc-coli, 1985), with little or no lag of the SST response, be-hind ice volume; and (2) at slightly lower latitudes (35-50°N), via the iceberg-meltwater flow, with a lag of severalthousand years of the surface-ocean temperatures behindice volume. To explain the anomalously low SST pulsesobserved in Figures 5 and 6, the first explanation wouldrequire unusually large ice sheets; the second would re-quire unusually rapid deglaciations.

We see no strong evidence in support of the first ice-sheet explanation. There is no obvious correlation be-tween the lowest SST values at Site 607 and the heaviestδ 1 8 θ values in the stacked isotopic record used as an ice-volume proxy by Imbrie et al. (1984). The lowest SST es-timates in the Site 607 record fall in stages 22 and 18,with less prominent low values in stages 10, 12, and 6.In the oxygen isotopic record of Imbrie et al. (1984), theheaviest δ 1 8 θ values occur in stages 16, 2, 6, and 12.Thus the lowest SST values do not fall at the times oflargest ice volume; stages 6 and 12 are the only intervalscommon to both sets.

A second possibility is that during isotopic stages 22,18, 12, and 10 there was an unusually large Laurentideice sheet, which presumably is more important than oth-er ice sheets in controlling the local temperature/salinityresponse of this part of the North Atlantic. But this wouldrequire that all other ice sheets be much smaller to com-pensate for the enhanced Laurentide effect in the globaloxygen isotopic record at these times, which seems un-likely.

865

Page 12: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

V30-97/Site 607 K708-7/Hole 552ANeogloboquadrina

δ 1 8 θ (°/oo) CaCO3 (%) pachyderms s. (%) SSTw (°C) SSTw (°C)

5.50 2.50 30 100 0 80 0 2 0 - 1 17n c\r\ . . . — . . •—_ •

Page 13: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

Figure 6. Oxygen isotopic, CaCO3, and N. pachyderma (s.) percent data from the spliced Site 607/Core V30-97 record plotted versus time, along with winter sea-surface temperature (SSTw)in this record and in the spliced Hole 552A/Core K708-7 record.

Page 14: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

Evidence in support of the second of the two ice-re-lated explanations—faster rates of deglaciation, causinga more concentrated influx of icebergs and meltwaterinto the North Atlantic—is also weak. Faster deglacia-tion could occur as a response to a larger rate of insola-tion forcing of the ice sheets. However, data in Berger(1977) indicate that none of the insolation parametersthought to be causal in forcing deglaciations (eccentrici-ty maxima, obliquity minima, or precessional terms) showunusual values uniquely correlative with the cold pulsesnoted above. Nor are actual values of incoming insola-tion at the latitudes of the ice sheets (45-65°N) unusualin any way at or near the times of these SST anomalies.Thus no anomalous insolation forcing of ice toward de-glaciation exists at these times.

A second possibility linked to the rate of deglaciationis that there was a maximum response at these times ofone or more of the feedback factors within the climatesystem that contribute to rapid deglaciations. The mostlikely feedback factors are: bedrock rebound, marine calv-ing, increased CO2, and moisture starvation. It is, how-ever, difficult to imagine why these factors would oper-ate more vigorously during the particular deglaciationsin question, particularly at isotopic stages 22/21 and 18/17. Moreover, the rate of operation of all of these feed-backs is ultimately tied directly to ice volume, which, asalready noted, was not unusually large in global termsat these times.

It is impossible to evaluate at this time the other likelyexplanation (changes in northward advection of warm,low-latitude waters) because of the scarcity of long-termSST records in critical low-latitude locations. The onlyavailable time series covering the last million years in thelow-latitude Atlantic are coarse-resolution SST estimates(average sampling interval 17,000 yr.) from Briskin andBerggren (1975) and pretransfer function data from Rud-diman (1971). Neither of these studies pinpoints any-thing unusual about the intervals in question.

Still, the contrast between the SST signals at Sites 552and 607 (Fig. 6) is instructive. The SST record at Hole552A can be attributed to relatively direct control by theNorthern Hemisphere ice-volume signal evident in oxy-gen isotopic curves, with larger ice volume forcing lowertemperatures (Ruddiman et al., in press). In contrast,the preliminary SST record from Site 607 is not totallyexplainable in terms of Northern Hemisphere ice vol-ume. And it is difficult to imagine Laurentide ice decou-pling entirely from the other high-latitude ice sheets.Therefore, the explanation for the trends at Site 607 maylie in forcing from low latitudes. Future ODP drillingon Leg 108 should help address this problem.

ACKNOWLEDGMENTS

We acknowledge the assistance of Joanne Munkelt and Denise Os-wald in laboratory analyses, Ann Esmay in data processing, and Bea-trice Rasmussen in manuscript preparation. We thank Joe Morley, Wil-liam Showers, and Bill Curry for critical reviews. This research wassupported by NSF grant OCE82-19862 from the Submarine Geologyand Geophysics Program of the Ocean Science Section of the NationalScience Foundation. We acknowledge the DSDP core curator for as-sistance in obtaining samples. This is Lamont-Doherty Geological Ob-servatory Contribution No. 3989.

REFERENCES

Berger, A. L., 1977. Long-term variations of caloric insolation result-ing from the earth's orbital elements. Quat. Res., 9:139-167.

Briskin, M., and Berggren, W. A., 1975. Pleistocene stratigraphy andquantitative paleo-oceanography of tropical North Atlantic coreV16-205. In Saito, T , and Burckle, L. (Eds.), LateNeogeneEpochBoundaries: New York (Micropaleontology Press), pp. 167-198.

CLIMAP Project Members, 1981. Seasonal reconstruction of theearth's surface at the last glacial maximum. Geol. Soc. Am. Mapand Chart Series MC-36.

Hulsemann, J., 1966. Notes: on the routine analysis of carbonate inunconsolidated sediments. J. Sed. Petrol., 36:622-625.

Imbrie, J., Hays, J. D., Martinson, D. G., Mclntyre, A., Mix, A. C ,Morley, J. J., Pisias, N. G., Prell, W. L., and Shackleton, N. J.,1984. The orbital theory of Pleistocene climate: support from a re-vised chronology of the marine 18O record. In Berger, A., Hays, J.,Imbrie, J., et al. (Eds.), Milankovitch and Climate (Vol. II): Bos-ton (D. Reidel Pub. Co.), 269-305.

Kent, D., Opdyke, N. D., and Ewing, M., 1971. Climate change in theNorth Pacific using ice-rafted detritus as a climate indicator. Geol.Soc. Am. Bull., 82:2741-2754.

Kipp, N. D., 1976. New transfer function for estimating past sea-sur-face conditions from sea-bed distribution of planktonic foraminif-eral assemblages in the North Atlantic. In Cline, R. M., and Hays,J. D. (Eds.), Investigation of Late Quaternary Paleoceanographyand Paleoclimatology. Geol. Soc. Am. Mem., 145:3-42.

Manabe, S., and Broccoli, A. J., 1985. The influence of continentalice sheets on the climate of an ice age. J. Geophys. Res., 90:2167-2190.

Ruddiman, W. F., 1971. Pleistocene sedimentation in the equatorialAtlantic: stratigraphy and faunal paleoclimatology. Geol. Soc. Am.Bull., 82:283-301.

, 1972. Sediment redistribution on the eastern ReykjanesRidge flank: seismic evidence. Geol. Soc. Am. Bull., 83:2039-2062.

., 1977. Late Quaternary deposition of ice-rafted sand in theSubpolar North Atlantic (lat. 40° to 65°N). Geol. Soc. Am. Bull.,88:1813-1827.

Ruddiman, W. F., and Mclntyre, A., 1976. Northeast Atlantic paleo-climatic changes over the past 600,000 years. In Cline, R. M., andHays, J. D. (Eds.), Investigation of Late Quaternary Paleoceanog-raphy and Paleoclimatology, Geol. Soc. Am. Mem., 145:111-146.

, 1981. Oceanic mechanisms for amplification of the 23,000-year ice volume cycle. Science, 212:617-627.

_, 1984. Ice-age thermal response and climatic role of the sur-face Atlantic Ocean, 40° to 63° N. Geol. Soc. Am. Bull., 95:381-396.

Ruddiman, W. F., Raymo, M., and Mclntyre, A., in press. Matuyama41,000-year cycles: North Atlantic Ocean and Northern Hemi-sphere ice sheets. Earth Planet. Sci. Lett.

Ruddiman, W. F , Shackleton, N. J., and Mclntyre, A., in press. NorthAtlantic Sea-Surface Temperatures for the Last I.I m.y. In Sum-merhayes, C. P., and Shackleton, N. J. (Eds.), Geol. Soc. LondonSpec. Publ.

Shackleton, N. J., 1977. The oxygen isotope stratigraphic record ofthe Late Pleistocene. R. Soc. London Phil. Trans. B, 280:169-178.

Shackleton, N. J., Backman, J., Zimmerman, H., Kent, D. V., Hall,M. A., Roberts, D. G., Schnitker, D., Baldauf, J. G., Desprairies,A., Homrighausen, R., Huddlestun, P., Keene, J. B., Kaltenback,A. J., Krumsiek, K. A. O., Morton, A. C , Murray, J. W., andWestberg-Smith, J., 1984. Oxygen isotope calibration of the onsetof ice rafting in DSDP Site 552A: history of glaciation in the NorthAtlantic region. Nature (London), 307:620-623.

Shackleton, N. J., and Opdyke, N. D., 1973. Oxygen isotope and pa-leomagnetic stratigraphy of equatorial Pacific core V28-238: oxy-gen isotope temperatures and ice volumes on a 105 and 106 yearscale. Quat. Res., 3:39-55.

Zimmerman, H. B., Shackleton, N. J., Backman, J., Kent, D. V.,Baldauf, J. G., Kaltenback, A. J., and Morton, A. C , 1985. His-tory of Plio-Pleistocene Climate in the Northeastern Atlantic, DeepSea Drilling Project Hole 552A. In Roberts, D. G., Schnitker, D.,et al., Init. Repts. DSDP, 81: Washington (U.S. Govt. Printing Of-fice), 861-876.

Date of Initial Receipt: 18 December 1984Date of Acceptance: 25 October 1985

868

Page 15: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

APPENDIX ADSDP Site 609: Calcium Carbonate Values

Sub-bottomdepth

(m)

0.060.310.610.911.211.411.812.112.412.713.013.313.613.914.214.514.815.115.415.716.016.316.616.797.317.617.918.218.518.819.119.419.71

10.0110.3110.6110.9111.2111.5111.8112.1112.4112.7113.0113.3113.6113.9114.2114.5114.8115.1115.4115.7116.0116.3117.5117.8117.9518.1118.2518.4118.5618.7118.8519.0119.1519.3119.4519.6119.7519.9120.0620.2120.3520.5120.81

CaCO3

(%)

79.1071.4440.6232.7022.7010.5416.2428.9823.1835.4931.4356.1143.1019.8037.1164.2378.8554.7676.1379.2666.2361.1566.8578.6115.8336.5558.0228.3834.6647.8264.6372.1166.6475.1460.9512.9435.5368.8480.1343.2123.5939.4023.6151.9838.6542.9917.0813.1467.6977.3958.8853.7778.5254.2964.6780.0678.3377.7313.948.13

27.4321.0913.1322.1914.2653.4057.256.47

69.4679.2960.2946.1772.3874.8080.9685.54

Sub-bottomdepth(m)

21.1121.4121.7122.0122.3122.6122.9123.0623.2123.3523.5123.6523.8123.9524.1124.2524.4124.5624.7124.8525.0125.1525.3125.4526.5126.8127.1127.4127.7128.0128.3128.6128.9129.2129.5129.8130.1130.4130.7131.0131.3131.6131.9132.2132.5132.8133.1133.4133.7134.0134.2134.5134.8135.1135.4135.7136.0136.3136.6136.9137.2137.5137.8138.1138.4138.8139.1139.4139.7140.0140.3140.6140.9141.2141.5141.81

CaCO3

85.8084.2781.7780.1515.4331.5933.3713.9712.6317.7337.4628.0546.3711.9116.6245.9046.6431.5117.7724.2751.1370.7158.9484.0984.0585.7883.5487.4773.2770.8780.6683.6579.4234.3956.1957.5344.8870.5873.6040.5163.4156.0865.0465.9264.9272.6551.4939.8915.6218.5750.81 B38.94 B18.28 B31.75 B30.85 B20.12 B27.46 B29.42 B30.32 B29.83 B47.16 B16.72 B63.11 B77.93 B67.80 B71.0359.7667.3463.8651.853.814.58

36.5557.3641.9870.47

Sub-bottomdepth(m)

42.1142.4142.7143.0143.3143.6143.9144.2145.4145.7146.0146.3146.6146.9147.2147.5147.8148.1148.4148.7149.0149.3149.6149.9150.2150.5150.8151.1151.4151.7152.0152.3152.6152.9153.2153.5153.8154.1154.4154.7154.9155.3155.6155.9156.2156.5156.8157.1157.4157.7158.0158.3158.6158.9159.2159.5159.8160.1160.4160.7161.0161.3161.6161.9162.2162.5162.8163.1163.4163.7164.0164.9165.2165.5165.8166.11

CaCC>3(%)

71.5029.3315.0867.3977.6956.5116.9221.9551.8376.7362.4757.7163.9064.9755.4976.4163.6539.8128.9118.7311.165.966.20

10.0535.3251.9056.4745.4750.4911.3633.7524.23

8.1548.4255.7574.4978.5375.5061.4545.0434.0454.2760.0262.0056.0159.1038.8841.9415.3670.4971.5153.7123.1259.2215.5558.6648.3275.9858.0762.9455.1664.4048.1661.7859.5925.9232.3872.1886.2581.1161.6647.1159.4260.3062.9062.38

Sub-bottomdepth(m)

66.4166.7167.0167.3167.6167.9168.2168.5168.8169.1169.4169.7170.0170.3170.6170.9171.2171.5171.8172.1172.4172.7173.0173.3173.6174.5174.8175.1175.4175.7176.0176.3176.6176.9177.2177.5177.8178.1178.4178.7179.0179.3179.6179.9180.2180.5180.5380.8181.1181.4181.7182.0182.3182.6182.9184.1184.4184.7185.0185.3185.6185.9186.2186.5186.8187.1187.4187.7188.0188.3188.6188.9189.2189.5189.8190.11

CaCO3

(%)

58.5864.5861.5450.747.15

18.0338.9662.7745.8049.1755.8649.7147.6517.839.97

35.1940.0613.7235.6542.0156.6463.3972.2269.6353.5271.7556.9239.8124.3257.0827.9542.5427.5048.2977.0174.8068.9645.3122.9428.8731.5818.7445.2782.6070.4775.2571.5023.1534.2119.4522.7462.9845.9872.8167.4351.4658.1362.2662.1348.1223.3964.3688.7958.1161.4161.0758.9754.9552.5159.5252.6439.9755.3749.4471.2574.13

Sub-bottomdepth(m)

90.4190.7191.0191.3191.6191.9192.2192.5195.2195.5195.8196.1196.4196.7197.0197.3197.6197.9198.2198.5198.8199.1199.4199.71

100.01100.31100.61100.91101.14103.11103.31103.61103.91104.21104.51104.81105.11105.41105.71106.01106.31106.61106.91107.21107.51107.81108.11108.41108.71109.01109.31109.61109.91110.21110.51110.81111.11114.71115.01115.31115.61115.91116.21116.51116.81117.11117.41117.71118.01118.31118.61118.91119.21119.51119.81120.11

CaCO3

(%)

79.5971.0969.3572.8567.3260.7938.4831.4076.5974.0972.5641.9921.6950.2849.4745.8769.1672.5670.3166.9771.8366.7074.8136.5032.8567.8158.4180.3751.4466.1658.4359.8959.2469.0268.4933.5085.6484.9471.5376.1663.1972.2265.0247.3365.5071.6085.8569.8973.9576.6970.8873.5950.7830.9354.8052.2952.1628.9544.8636.5758.2479.0227.1437.9848.8438.2265.4267.3962.9462.9258.4760.5669.6966.9068.6567.61

869

Page 16: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

Appendix A (continued).

Sub-bottomdepth

(m)

120.41120.71121.01122.25122.51122.81123.11123.41123.71124.01124.31124.61124.91125.21125.51125.81126.11126.41126.71127.01127.31127.61127.91128.21128.51128.81129.11129.41129.71130.01130.31130.61130.91131.21131.47131.81132.11132.41132.71133.01133.31133.61133.91134.21134.51134.81135.11135.41135.71136.01136.31136.61136.91137.21137.51137.81138.11138.41138.71139.01139.31139.61139.91140.25140.51140.81141.11141.41141.71142.01142.31142.61142.91143.21143.51143.81144.12

CaCO3

(%)

30.9539.7550.6571.2266.1347.0848.7465.6684.0067.3774.8950.6949.2767.3374.9169.7866.1068.5768.0662.3464.2365.3667.6166.2262.7668.5851.2826.0084.6883.6875.3733.5383.5484.4777.6768.9970.7372.8860.8146.9267.7657.2948.0845.8548.2014.8075.8551.2783.1780.3278.1067.8879.2812.3776.7574.8272.3853.4370.3977.9874.4569.4864.1174.8368.7271.9670.4473.6973.0166.8077.0151.9750.5541.0645.1061.4087.79

Sub-bottomdepth(m)

144.41144.71145.01145.31145.61145.91146.21146.51146.81147.11147.41147.71148.01148.31148.61148.91149.21150.11150.41150.71151.01151.31151.61151.91152.19152.21152.51152.81153.11153.41153.71154.01154.31154.61154.91155.21155.51155.81156.11156.41156.71157.01157.31157.61157.91158.21158.51158.81159.11159.71160.01160.31160.61160.95161.21161.36162.71163.01163.31163.61163.91164.21164.51164.81165.11165.41165.71166.01166.31166.61166.91167.21167.51167.81168.11168.41168.71

CaCO3

(%)

66.0973.7082.4541.0250.3177.7283.2778.3764.0360.1970.2550.0231.0230.2241.2280.8384.5470.2269.6168.3875.0367.1149.5020.0651.6147.6724.4781.7472.3068.6867.9158.4459.8350.6459.1056.9461.1547.8970.3470.9875.5870.1668.1465.5963.8459.5861.7670.3866.1664.6060.4560.3963.8267.6569.1370.1270.35 B68.40 B60.70 B64.44 B75.56 B73.96 B69.42 B68.91 B64.59 B57.02 B56.63 B49.84 B49.59 B53.00 B60.48 B59.31 B63.58 B69.85 B70.41 B63.21 B67.41 B

Sub-bottomdepth

(m)

169.01169.31169.61169.91170.21170.51170.81171.11171.41171.71172.01172.19172.31172.61172.91173.21173.51173.81174.11174.41174.71175.01175.31175.61175.91176.21176.51176.81177.11177.41177.71178.01178.31181.91182.21182.51182.81183.11183.41183.71184.01184.31184.61184.91185.21185.51185.81186.11186.41186.71187.01187.31187.61187.91188.21188.51188.81189.11189.41189.71190.01190.31190.61190.91191.21191.44191.51191.81192.11192.41192.71193.01193.31193.61193.91194.21194.51

CaCO3

(%)

67.29 B31.60 B75.93 B73.73 B67.91 B66.94 B66.85 B61.52 B43.79 B52.26 B80.84 B77.44 B52.33 B63.67 B61.15 B53.16 B60.54 B67.36 B72.02 B67.62 B65.44 B70.70 B68.50 B67.45 B72.66 B50.47 B44.98 B70.65 B67.58 B70.03 B59.61 B75.33 B72.22 B75.94 B78.55 B72.98 B73.37 B68.78 B75.83 B66.88 B58.39 B58.68 B57.69 B63.30 B63.03 B69.60 B70.18 B70.16 B68.07 B67.28 B72.62 B71.52 B71.93 B72.33 B69.64 B71.52 B73.28 B70.82 B68.35 B68.55 B69.25 B71.29 B70.60 B74.67 B76.47 B78.46 B68.66 B69.42 B66.22 B60.91 B60.28 B63.48 B71.04 B72.22 B74.26 B76.32 B73.04 B

Sub-bottomdepth(m)

194.81195.11195.41195.71196.01196.31196.61196.91197.21197.51197.81198.11198.41198.71199.01199.31199.61199.91200.21200.51200.81201.11201.41201.71202.01202.31202.61202.91203.21203.51203.81204.11204.41204.71205.01205.31205.61205.91206.21206.51206.81207.11207.41207.71208.01208.31208.61208.91209.21209.51209.81210.11210.41210.64210.79211.01211.31211.61211.91212.21212.51212.81213.11213.41213.71214.01214.31214.61214.91215.21215.51215.81216.11216.41216.71217.01217.31

CaCO3

(%)

75.02 B75.43 B72.29 B73.03 B74.76 B81.34 B82.77 B75.76 B67.65 B63.80 B64.53 B71.42 B71.70 B69.12 B67.33 B71.68 B71.37 B72.79 B66.57 B62.50 B68.58 B71.58 B76.61 B84.67 B80.09 B72.98 B69.59 B71.48 B70.65 B74.29 B76.82 B79.48 B78.15 B79.28 B74.30 B65.03 B71.65 B70.73 B68.31 B67.17 B62.99 B74.76 B76.23 B71.72 B65.35 B64.67 B70.88 B70.35 B67.21 B70.65 B74.46 B79.24 B73.04 B77.05 B75.48 B73.60 B69.31 B71.43 B65.44 B65.87 B64.63 B76.13 B85.73 B84.44 B66.57 B82.04 B82.93 B81.62 B79.04 B78.09 B76.32 B79.10 B77.89 B77.85 B76.02 B75.54 B79.00 B

Sub-bottomdepth(m)

217.61217.91218.21218.51218.81219.11219.41219.71219.96220.31220.61220.91221.21221.51221.81222.11222.41222.71223.01223.31223.61223.91224.21224.51224.81225.11225.41225.71226.01226.31226.61226.91227.21227.51227.81228.11228.41228.71229.01229.31229.61229.83229.98230.21230.51230.81231.11231.48231.71232.01232.31232.61232.91233.21233.51233.81234.11234.41234.71235.01235.31235.61235.91236.21236.51236.81237.11237.41237.71238.01238.31238.61238.91239.21239.51239.81240.11

CaCO3

(%)

81.24 B78.70 B78.30 B77.40 B89.20 B78.09 B76.11 B69.11 B78.03 B85.09 B80.57 B83.27 B84.09 B80.84 B78.01 B81.43 B84.93 B81.81 B80.47 B77.45 B75.03 B73.74 B75.12 B75.51 B78.69 B82.14 B79.41 B81.61 B80.19 B80.08 B76.65 B75.80 B78.21 B81.93 B82.51 B82.41 B81.68 B82.70 B83.16 B80.58 B81.73 B75.71 B82.77 B78.50 B82.03 B82.31 B77.07 B80.46 B77.38 B79.79 B85.32 B85.17 B85.43 B82.81 B83.41 B84.85 B80.87 B81.38 B82.37 B75.93 B83.61 B89.92 B89.25 B90.27 B88.92 B89.56 B88.93 B95.42 B89.17 B92.13 B89.93 B88.80 B85.80 B87.19 B91.55 B92.23 B89.83 B

870

Page 17: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

Appendix A (continued).

Sub-bottomdepth

(m)

240.41240.71241.01241.31241.61241.91242.21242.51242.81243.11243.41243.71244.01244.31244.61244.91245.21245.51245.81

CaCO3

(%)

90.37 B92.61 B93.80 B93.00 B92.18 B93.12 B90.66 B91.57 B91.80 B92.30 B91.94 B91.59 B92.21 B91.90 B92.47 B93.25 B89.80 B87.05 B90.66 B

Sub-bottomdepth(m)

246.11246.41246.71247.01247.31247.61247.91248.21248.51248.81249.07249.11249.41249.71250.01250.31250.61250.91251.21

CaCO3

(%)

90.58 B89.85 B93.02 B90.71 B93.88 B93.77 B91.39 B88.83 B93.15 B90.29 B92.85 B91.49 B90.77 B93.70 B94.05 B94.23 B86.29 B86.09 B89.83 B

Sub-bottomdepth(m)

251.49251.81252.11252.41252.71253.01253.31253.61253.91254.21254.51254.81255.11255.41255.71256.01256.31256.61256.91

CaCO3

(%)

93.18 B94.10 B91.89 B89.87 B93.88 B95.33 B92.24 B92.67 B90.85 B92.51 B88.08 B90.64 B92.41 B91.49 B90.38 B92.23 B94.76 B93.48 B92.46 B

Sub-bottomdepth(m)

257.21257.51257.81258.77259.01259.31259.61259.91260.23260.51260.81261.11261.41261.71262.01262.31262.61262.91263.21

CaCO3

(%)

89.75 B90.10 B91.91 B92.95 B93.06 B92.46 B94.43 B92.77 B94.81 B93.53 B96.55 B92.26 B90.23 B92.73 B92.98 B93.89 B94.82 B94.13 B95.03 B

Sub-bottomdepth(m)

263.51263.81264.11264.41264.71265.01265.31265.61265.91266.21266.51266.81267.11267.41267.71268.01

CaCO3

(%)

91.87 B91.82 B92.83 B91.61 B92.25 B91.62 B89.37 B93.12 B89.47 B92.99 B92.38 B93.83 B93.60 B86.27 B90.83 B90.30 B

Note: A " B " indicates values from Hole 609B, others are from Hole 609.

APPENDIX BDSDP Site 607: Calcium Carbonate Values

Sub-bottomdepth

(m)

0.010.160.310.530.610.780.911.061.211.361.511.661.812.032.112.282.412.562.712.863.013.163.313.533.613.783.914.064.214.364.514.664.815.035.115.205.285.415.565.715.866.016.166.316.536.616.78

CaCO3

(%)

84.8882.2559.7653.0549.8750.2157.2753.7063.6462.0259.2567.5167.2559.6971.1275.4472.9468.5256.3060.4068.5074.8280.3284.5783.5682.7884.7687.0587.0186.4981.3282.6183.4574.9986.9187.2979.1261.8169.8569.6773.3770.7368.8456.2164.4763.5277.39

Sub-bottomdepth(m)

6.917.067.217.367.517.517.817.888.118.138.418.568.718.869.019.16

10.1510.3810.6610.9611.1111.2611.4111.6311.7111.8812.0112.1612.3112.4612.6112.7612.9113.1313.2113.3813.5113.6613.8113.9614.1114.2614.4114.6314.7114.8815.01

CaCO3

(%)

76.3969.2063.1376.5266.8274.1874.2080.8478.5281.5783.5869.8370.4081.5181.6273.1668.6164.6990.8191.1990.1079.4569.7086.2086.3386.1891.2689.4188.1891.1991.0688.2854.5663.0666.7270.5977.0679.0868.2759.1578.4777.7180.7886.1485.6691.8691.07

Sub-bottomdepth(m)

15.1615.3115.4615.6115.7615.9116.1316.2116.3816.5116.6616.8116.9617.1117.1717.2617.4117.6317.7117.8818.0118.1618.3118.4618.6118.7618.8419.2119.3619.5119.7319.8119.9820.1120.2620.4120.5620.7120.8621.0121.2321.3121.4821.6121.7621.9122.06

CaCO3

( * )

94.4892.2588.4691.0091.3696.3793.6793.6585.0293.5493.5090.2680.4352.6755.7865.8255.6158.3567.5174.6376.8277.4371.5667.1875.9475.0580.9992.8292.6884.8245.7164.3250.8764.6361.9671.7280.7378.4972.0962.5077.7173.5382.2280.0578.9686.5490.31

Sub-bottomdepth(m)

22.2122.3622.5122.7322.8122.9823.1123.2623.4123.5623.7123.8624.0124.2324.3124.4824.6125.5225.7325.8225.9826.1326.2626.4226.5626.7226.8627.0227.2327.3227.4827.6327.7627.9228.0628.2328.3628.5228.7328.8328.9829.1429.2629.4229.5629.7329.86

CaCO3

(%)

90.2191.0490.4385.0080.3080.1187.6082.8179.2584.6082.1182.8077.2968.3174.7178.7883.4378.7376.3678.9784.3684.9881.9080.5479.3278.9277.6773.9572.6969.5863.3955.0652.6746.5258.5464.9656.0061.4956.3457.4565.0465.7164.3370.2059.1569.0763.11

Sub-bottomdepth(m)

30.0330.2330.3330.4830.6330.7630.8931.0631.2331.3631.4931.7331.8031.9832.0932.2632.4032.5632.7432.8632.9933.2333.2933.4833.6333.7633.9034.0634.2634.3634.4434.8334.9635.0935.3335.4135.4235.5835.6935.8635.9735.9936.1836.3436.4636.6136.83

CaCO3

(%)

61.3263.6664.1670.3377.3375.0573.7285.6386.4884.8386.0980.6680.6563.5738.5552.0355.3866.2072.9477.4777.6975.6477.7963.5754.6560.5061.6764.8459.1971.0165.7377.8175.9179.1184.2583.7483.7190.1389.1986.8186.3186.0388.2489.7382.4086.4977.41

871

Page 18: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

Appendix B (continued).

Sub-bottomdepth(m)

36.8837.0837.1937.3637.4937.6637.8337.9638.0938.3338.3838.4138.5838.7438.8638.9939.1639.3339.4639.5939.8339.8939.9040.0840.1940.3640.4940.5240.6140.8340.9641.0941.1741.3341.4141.5841.7141.8641.9942.1642.2442.3342.4642.5942.8342.8843.0843.1843.2043.3643.5043.6643.8343.9644.0144.5644.7244.9345.0345.1845.3345.4645.5845.7645.9446.0646.2046.4346.4546.4946.6846.7746.7946.9647.1047.26AIM47.56

CaCO3

(%)

66.7457.3160.7458.8360.8251.7939.3649.0759.0776.5979.0679.0684.2677.6383.8080.2064.6065.6462.6667.4566.0273.2676.3686.9187.4391.4993.2793.2492.2291.0790.6285.3279.7168.7881.1485.2786.2786.0983.0976.2085.5184.8487.4087.9587.8689.0877.9083.8782.0884.8782.8587.8891.6892.0089.9072.9374.6885.2490.7892.4091.3990.8092.3087.5589.1788.4185.3968.7972.6677.8686.8086.6881.8384.1179.2772.4664.9173.31

Sub-bottomdepth

(m)

47.7047.9347.9948.0348.1848.3148.4648.5948.7648.9449.0649.1949.2049.4349.5049.6849.8149.9650.0950.1150.2550.4350.5650.7050.9350.9951.1851.3151.4651.6051.7651.9352.0652.2252.4352.4952.6852.7952.9653.0953.2653.4353.5954.0554.1654.2954.5354.6154.7854.9155.0655.2155.3655.3655.5355.6655.8156.0356.2856.4156.5656.7156.8657.0157.1657.2957.5357.6357.7857.9158.0658.2158.3658.4158.6658.7959.0359.09

CaCO3

(%)

73.1177.1785.1375.7283.7090.3791.3691.9389.8691.8991.3889.2489.8288.9991.1089.1988.6578.5683.3889.2570.1479.1481.2875.9978.8577.8574.5886.2991.3390.3591.6986.0273.1165.0763.6363.4574.6969.8385.7287.9290.9582.3290.1380.3486.9687.1888.1488.9788.0385.3385.1280.5166.0367.1768.2776.7376.3785.2191.1489.6490.4688.8189.5089.2786.1582.0775.8079.6574.7085.2580.5792.5991.5386.2788.2785.6080.5282.10

Sub-bottomdepth(m)

59.2859.4159.5659.7159.8660.0160.1660.3060.3760.5360.6160.7860.9161.0661.2161.3661.5161.6661.8162.0362.1162.2862.4162.5662.7162.8663.0163.1663.2463.6563.7663.9164.1364.2164.3864.4964.6664.8164.9665.1365.2665.3965.6365.7165.8866.0166.1666.2966.4666.6166.7666.9167.1367.2367.3867.4967.6667.7967.9668.1168.2668.4168.6368.7168.8869.0169.1669.3169.4669.6169.7669.9170.1370.2170.3870.5170.6670.81

CaCO3

(%)

86.0487.7195.0292.5392.6690.8182.6259.8064.1468.3072.4079.3384.3589.4989.5092.0790.9892.1786.4873.4874.4977.8776.3882.5387.3991.2791.0692.1689.9280.3976.3173.9678.2482.1186.7590.8581.5986.4592.0792.8893.7191.9487.1285.6286.2388.0288.6688.1688.7984.2277.0188.1588.6690.3888.6393.3590.3088.0589.0289.5386.1787.6790.1891.5687.6685.7182.5979.7681.7380.8472.5875.9985.5387.6090.3288.5890.2289.27

Sub-bottomdepth(m)

70.9671.1171.2671.3971.6371.7171.8871.9972.1672.3172.4672.6172.7673.2173.3673.7373.8173.9874.2674.4174.5674.7174.8675.0175.2375.3175.4875.6175.7675.9176.0676.2176.3676.5176.7376.8176.9877.1177.2677.4377.5677.7377.8678.0178.2378.3178.4878.6178.7678.9179.0679.2179.3679.5179.7379.8179.9880.1180.2680.4180.5680.7180.8680.9981.2381.3181.4881.5981.7681.9182.0682.2182.3682.5182.8782.9682.9683.11

CaCO3

(%)

87.0183.7173.9663.1470.3875.4686.0081.3082.0485.5286.3881.2280.4292.6193.7790.7289.9888.8871.1371.8176.2978.3885.2088.5288.3787.6687.0489.1091.0488.7687.9078.9879.9085.2486.7988.8786.4989.1390.0191.9989.4092.1785.2190.2989.9792.0591.3790.6194.9094.3993.5090.7790.8081.2181.1480.2282.0983.2582.5784.7485.6587.0789.6890.0788.3789.6889.6389.3786.3084.3882.6981.0187.1683.3584.0293.9890.3787.80

Sub-bottomdepth(m)

83.3383.4183.5883.7183.8684.0384.1684.1784.3184.4684.6184.8384.8985.0885.1985.3685.4985.6685.8385.9686.1186.3386.4386.5886.7186.8687.0187.1687.3387.4687.6187.8387.8988.0888.1988.2888.3688.4688.5388.6688.8388.9689.1589.3389.4189.5889.7189.8690.0190.1690.3190.4690.6190.8390.8991.0891.1991.3691.4991.6691.8391.9692.0792.4592.5692.7192.9393.0193.1893.3193.4693.6193.7693.9194.0694.2194.4394.51

CaCO3

(%)

86.1382.7988.8483.8690.6589.4574.4075.4088.4292.0693.0392.0496.0292.9594.1890.5691.2788.4490.0994.4091.9391.0993.3392.0887.7278.1875.7876.1573.1374.8869.3880.3683.4689.7190.6284.6576.3555.5683.8187.1090.6590.0589.6485.6883.1584.5688.7190.4891.3489.9489.9891.7584.6577.0377.0276.0471.1069.5678.1381.7891.4392.7992.0289.8291.0287.6087.0389.1390.9590.7991.5687.0282.4974.9475.8775.7782.9286.65

872

Page 19: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

Appendix B (continued).

Sub-bottomdepth(m)

94.6894.8194.9695.0995.2695.2695.4195.5695.7195.9396.0396.1896.3196.4696.6196.7696.9197.0697.2197.4397.5197.6897.8197.9698.1198.1198.2698.4398.5898.7198.9399.0199.1899.3199.4699.6199.7699.91

100.06100.21100.43100.51100.69100.81100.96101.11101.26101.45101.48102.05102.16102.31102.53102.61102.78102.91103.06103.21103.36103.51103.66103.81104.03104.11104.28104.41104.56104.71104.86105.01105.16105.31105.53105.61105.78105.89106.06106.21

CaCO3

(%)

91.3693.3392.3089.8580.4483.4689.4291.0385.9574.0879.0374.0874.9980.8687.3189.0589.4291.6787.5387.8788.4689.1085.1585.6976.7276.5584.6585.4489.1691.7091.5389.8486.2083.6887.3382.5877.2674.6186.3889.7290.1988.9289.8888.0490.7885.7291.2786.0890.0291.5687.9880.2979.3778.2065.5076.6169.9175.9775.8782.6075.8789.6690.7091.3390.7690.5787.4283.7162.5972.2379.1478.9988.2390.2290.6389.2088.3177.56

Sub-bottomdepth(m)

106.36106.51106.66106.79107.03107.11107.28107.39107.56107.71107.86108.01108.16108.32108.53108.61108.78108.91109.06109.21109.36109.51109.66109.81110.03110.11110.28110.41110.56110.71110.86111.07111.67111.76111.91112.13112.21112.38112.51112.66112.79112.96113.11113.26113.41113.63113.71113.88114.01114.16114.31114.46114.61114.76114.91115.02115.13115.14115.21115.38115.51115.66115.78115.96116.11116.26116.41116.63116.69116.88117.01117.16117.31117.46117.61117.76117.91118.13

CaCO3

(%)

74.8967.9070.4367.3477.9377.6985.5189.7093.3892.8991.8591.7992.8793.0488.8790.8289.7291.1491.3190.3391.2990.8687.2987.7877.9867.6874.1075.0284.0489.0291.3994.8894.1191.9786.4091.8786.4592.1792.3792.3291.0986.6886.2084.0288.7687.5187.2388.7884.5485.1683.6581.1579.4181.4688.3382.4580.4683.5192.7089.3789.5791.5090.8691.1791.7389.4380.5887.8290.4890.9192.1991.2790.7390.7886.3084.5087.0583.63

Sub-bottomdepth(m)

118.21118.38118.51118.66118.81118.96119.11119.26119.39119.63119.71119.88120.01120.16120.31120.46120.61120.76120.81121.25121.36121.51121.73121.81121.98122.11122.26122.41122.56122.71122.86122.99123.23123.29123.48123.61123.76123.91124.06124.21124.36124.49124.73124.81124.90125.11125.26125.41125.56125.73125.86126.01126.23126.31126.48126.59126.76126.91127.06127.24127.36127.51127.73127.81127.89128.11128.26128.39128.56128.71128.86128.99129.23129.31129.48129.59129.78129.91

(*Vo)

87.0888.0894.0193.0692.3393.1390.8493.1392.2687.4492.9288.7589.9392.9592.8293.2190.5492.5090.8793.3888.5892.2791.1492.7091.7297.1392.4988.6685.4491.4087.6989.2690.7491.2491.5891.0592.6492.0491.5989.6392.2290.0987.0987.3987.2189.6989.8388.2289.9488.4690.3988.2887.1086.0385.9785.3785.5587.5189.6289.6489.9788.4987.9988.5188.3990.7190.5091.4592.2490.3293.2296.2392.0493.6190.0392.2392.6591.31

Sub-bottomdepth(m)

130.08130.23130.38130.81130.96131.11131.33131.41131.71131.86132.01132.16132.31132.46132.61132.83132.89133.08133.19133.36133.49133.66133.81133.96134.11134.33134.44134.58134.71134.86135.01135.16135.31135.46135.61135.83135.91136.08136.21136.36136.53136.66136.81136.96137.11137.33137.41137.58137.71137.86138.01138.16138.31138.46138.83138.91139.08139.21139.36139.51139.66139.81139.96140.11140.41140.56140.71140.93141.01141.18141.31141.46141.61141.76141.91142.06142.17142.43

CaCO3

(%)

92.5494.9794.2687.3387.7088.9090.7089.9394.5694.8991.4492.1691.3493.3389.8891.4693.0492.8395.6095.4496.1198.8492.7694.0492.5892.9693.1592.8691.9793.9393.6393.3988.4692.6091.3191.6194.8990.8791.5491.1387.6190.7590.0990.0987.5888.7888.0291.1692.4494.2692.5694.9594.6094.5893.3493.2494.4693.6094.7291.5992.8398.2294.8894.3594.9193.3592.1092.8093.1195.4193.1692.2193.1493.5895.7593.8898.0396.02

Sub-bottomdepth

(m)

142.51142.68142.81142.96143.11143.26143.41143.56143.71143.93144.03144.03144.18144.33144.33144.46144.61144.76144.91145.06145.21145.31145.51145.59145.81145.87146.13146.13146.26148.66150.16151.66152.01153.16153.39154.76155.11159.61159.91160.21160.51160.81161.11161.41161.71162.01162.31162.61162.91163.16163.16163.21163.51163.81164.11164.41164.71165.01165.31165.61165.91166.21166.51166.81167.11167.41167.71167.99182.36191.96201.56211.16220.76230.33239.93

CaCO3

(%)

94.0296.1894.0498.7294.3791.8392.7794.4995.4696.5894.6296.3695.9487.3588.8393.4193.9096.3794.5092.9292.2895.6894.6493.1992.7590.4288.8091.5093.7093.1292.2793.4294.1593.7991.4692.5592.7292.2791.3992.3290.6392.7593.6091.7689.5893.4393.9493.1592.7392.6792.6993.7091.4194.3696.5592.9392.7192.8689.8694.0191.0493.1993.5694.4592.8792.6893.8993.0292.5393.7192.8890.9894.2495.1795.18

873

Page 20: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

APPENDIX C

DSDP Site 607: Oxygen Isotope and Faunal Data Appendix C (continued).

Sub-bottomdepth

(m)

9.619.769.769.91

10.1510.1510.2110.3810.3810.5110.6610.6610.6610.8110.9611.1111.2611.4111.6311.6311.7111.8812.0112.1612.3112.3812.4612.4612.6112.6112.7612.9113.1313.1313.1313.2113.2113.3813.5113.5113.6613.6613.8113.9614.1114.1114.2614.3314.4114.4914.6314.6314.7114.7114.8814.8814.8814.8815.0115.0115.1615.1615.1615.3115.4615.4615.6115.6115.7615.7615.8315.9115.9116.1316.2116.2116.2816.3816.3816.51

δ 1 8 o(‰)

4.35 U3.84 U4.33 C

3.94 C4.35 U3.21 U4.24 U2.74 C3.81 U3.25 C4.33 U3.65 C2.87 C2.25 C3.28 C2.88 C

3.46 C3.21 C3.12 C2.99 C3.06 C2.52 C2.37 C

2.78 C2.45 C2.13 C2.30 C2.58 C2.57 C3.17 C4.46 U2.87 C3.81 C4.98 U3.88 C5.02 U3.78 C2.82 C4.38 U3.80 C3.48 C4.55 U2.68 C3.06 C4.39 U2.87 C3.63 C3.45 U3.30 C3.45 C3.72 U3.16 C4.53 U3.59 C4.27 U3.13 C3.05 U3.96 U3.37 C3.82 U3.88 U1.80 C3.43 U2.24 C2.34 U3.22 U2.55 C

2.55 C2.65 C2.40 C2.17 C2.07 C

2.54 C2.23 C2.69 C

G.

ruber(%)

0.7

4.74.0

8.81.9

2.2

2.7

3.0

4.06.22.24.42.5

1.14.14.32.8

2.12.0

2.2

10.5

10.03.01.4

1.2

1.61.2

1.1

0.7

0.0

0.4

1.32.12.42.3

3.1

3.9

2.2

5.7

2.8

2.62.4

5.1

5.6

11.712.5

22.216.6

14.617.2

24.6

G.bulloid.

(%)

14.1

15.715.0

10.714.2

21.19.7

12.213.213.115.514.611.3

13.517.48.7

16.019.518.98.0

8.4

10.416.930.9

8.3

23.510.8

13.9

32.239.915.4

19.922.414.013.413.5

10.2

10.3

7.9

9.9

14.511.6

6.6

12.6

10.67.7

8.96.7

8.98.3

7.2

N.

pachy. s.(%)

1.0

1.77.2

1.74.7

4.40.3

2.7

1.81.48.5

10.22.6

2.2

2.22.32.81.75.12.5

1.7

5.2

13.920.7

4.7

8.7

4.8

10.1

7.3

16.19.4

5.04.25.99.24.1

3.3

9.6

3.9

1.2

1.510.4

1.1

2.7

4.20.3

0.61.1

1.41.0

0.6

G.inflataW

8.2

22.37.6

28.39.4

15.618.2

21.623.513.1

9.613.521.1

11.316.518.316.5

9.69.5

21.4

19.6

20.48.67.9

22.4

9.115.2

8.2

5.00.5

5.6

9.38.8

11.910.712.6

14.0

16.8

22.1

18.5

17.519.0

39.6

32.9

29.927.9

24.225.8

21.022.1

15.3

AllotherW

75.9

55.666.2

50.669.8

56.769.0

60.557.466.264.257.362.4

72.059.866.461.967.164.565.9

59.8

54.157.539.0

63.4

57.168.0

66.7

54.843.469.2

64.562.565.764.466.7

68.7

61.1

60.4

67.6

63.956.7

47.6

46.2

43.651.5

44.149.8

54.151.4

52.3

SSTVv

(°C)

12.1

13.5

11.6

16.411.6

10.413.8

13.013.614.210.611.212.9

12.012.614.012.111.410.713.4

16.4

15.29.65.4

12.3

8.7

11.8

10.2

7.04.19.9

10.210.211.510.812.3

13.3

11.2

14.4

13.6

12.610.8

16.9

15.2

17.118.3

20.219.1

17.818.7

19.5

Sub-bottomdepth

(m)

16.5116.5116.6616.8116.9617.0317.1117.2617.2617.3317.4117.5017.6117.6317.7117.7817.8817.8818.0118.1618.3118.3118.4618.4618.6118.6118.7618.8419.2119.3619.5119.7319.7319.8119.9820.1120.2620.2620.4120.5620.5620.5620.7120.7120.8620.8621.0121.0121.0121.0121.2320.2321.2321.3121.4821.4821.6121.6121.6121.7621.7621.7621.8921.9121.9122.0622.0622.0622.2122.3622.5122.5122.7322.8122.8122.8822.9822.9823.1123.26

δ 1 8 θ(‰)

4.51 U2.36 C2.12 C2.65 C2.99 C3.17 C3.89 C4.10 C4.17 C4.18 C

3.78 C

3.60 C

3.37 C4.74 U3.00 C4.74 U4.53 U3.24 C4.18 U3.99 C4.47 U3.75 C4.46 U3.63 U2.09 C2.57 C3.01 C3.37 C4.59 U3.64 C2.95 C3.15 C4.60 U3.72 C4.27 C4.80 U2.99 C4.24 U4.59 U3.39 C3.53 C4.56 U4.61 U3.94 C3.62 C4.53 U4.60 U3.46 C4.50 U4.35 U4.55 U3.12 C3.39 C4.22 U3.55 C4.35 U2.92 C4.37 U4.43 U4.10 U4.20 U2.84 C4.01 U4.01 U3.76 U3.52 U3.81 U3.20 C2.30 C3.41 C3.88 U

3.34 C4.58 U4.53 U3.78 C

G.ruber(%)

19.411.96.51.0

1.9

1.81.01.0

0.0

0.91.11.1

1.12.12.3

0.8

2.2

1.20.0

21.719.65.60.3

1.50.31.50.6

0.61.9

2.1

3.2

2.3

2.4

0.2

1.6

3.1

0.7

6.32.5

4.1

3.3

6.83.5

5.0

4.9

1.42.5

4.04.2

G.bulloid.

W

18.721.110.77.3

19.0

19.613.921.6

17.325.925.619.9

13.410.115.6

14.3

14.3

15.119.015.513.316.513.8

20.417.918.329.4

23.119.1

12.4

16.3

18.5

15.6

16.98.5

8.7

8.1

10.510.2

9.0

12.78.6

10.6

14.416.2

13.88.7

14.410.0

N.pachy. s.

(%)

0.41.4

14.349.7

10.3

7.8

18.427.7

41.816.419.313.4

6.75.19.9

19.2

6.9

12.94.80.61.57.4

39.9

7.917.317.920.2

19.17.4

5.5

11.1

16.6

7.9

14.37.2

13.0

16.1

8.64.9

4.5

2.0

1.11.6

2.7

9.2

19.79.4

1.43.3

G.inflataW

18.324.220.2

4.9

28.7

11.117.1

9.9

5.2

8.69.6

19.6

28.620.311.4

12.0

25.1

12.211.218.121.122.9

4.5

19.415.3

8.47.1

8.5

20.1

18.6

9.2

11.6

20.1

9.412.7

12.4

16.5

8.2

13.0

23.2

17.118.416.3

12.113.7

15.223.9

21.620.3

All

other0%)

43.241.448.237.1

40.2

59.649.739.7

35.748.144.446.0

50.262.460.8

53.8

51.5

58.665.044.044.447.541.5

50.849.253.842.6

48.751.5

61.4

60.3

51.0

54.0

59.4

70.0

62.8

58.6

66.469.4

59.2

64.965.0

67.9

65.8

56.1

50.0

55.4

58.562.1

SSTW( ° Q

18.916.711.85.8

9.8

9.78.46.3

5.66.56.38.1

11.2

12.310.3

8.2

11.3

9.39.8

19.3

19.012.3

6.5

9.47.5

8.15.3

6.610.0

11.7

10.3

8.6

10.8

8.411.9

11.1

9.6

12.812.4

13.5

13.115.2

13.6

13.211.3

8.411.6

13.413.6

874

Page 21: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

Appendix C (continued).

PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

Appendix C (continued).

Sub-bottom

depth(m)

23.2623.4123.4123.4823.5623.7123.7123.8623.8624.0124.0124.1224.2324.3124.3124.3924.4824.6125.2125.3625.5125.6325.7325.8125.9025.9825.9826.1126.1826.2626.3126.4126.4126.4426.5626.7126.8626.9327.0127.1227.2327.3127.4827.6127.7627.9128.0628.2128.3628.5128.7328.8128.9829.1129.2629.4129.5629.7129.8630.0130.2330.3130.3330.4830.6130.7630.9131.0631.2131.3631.5131.5131.6231.7331.8131.9831.9832.1132.1132.2632.4132.41

1 C

δ 1 8 θ(‰)

4.63 U3.43 C4.50 U

2.92 C2.76 C3.33 C3.09 C2.95 C3.20 C2.91 C

2.81 C2.65 C4.38 U

2.44 C2.04 C2.81 C2.68 C2.70 C

2.59 C2.94 C

2.95 C2.87 C2.59 C

2.90 C2.49 C

2.81 C2.64 C

2.90 C

2.81 C

3.09 C

4.03 C

4.11 C

4.16 C4.22 C3.59 C3.78 C3.65 C3.76 C

3.21 C

4.44 U3.27 C3.24 C3.29 C3.41 C3.23 C2.37 C2.73 C3.11 C2.78 C2.79 C

2.96 C2.86 C3.93 U2.79 C4.38 U3.53 C4.53 U3.16 C4.57 U

G.

ruber(ft)

2.4

2.2

0.7

3.5

3.3

7.6

5.87.7

2.8

7.6

4.58.9

7.0

4.57.5

4.6

5.2

6.7

9.7

11.312.112.4

8.9

9.9

12.59.8

11.68.3

11.49.7

7.9

5.3

4.8

2.3

1.83.70.7

3.3

1.91.1

2.1

1.0

1.32.4

4.7

2.7

4.3

1.5

1.8

2.2

2.2

3.6

4.8

3.3

4.9

11.717.514.911.1

20.417.215.1

5.3

0.0

2.3

0.9

G.

bulloid.

(ft)

8.8

13.613.29.6

11.6

13.2

9.6

17.714.2

12.612.018.5

10.09.6

13.59.9

14.710.9

13.412.712.113.6

11.013.212.517.513.514.213.913.015.114.411.914.117.115.915.218.514.721.013.916.712.920.020.514.26.4

7.5

7.5

18.29.3

13.016.18.1

17.917.511.711.716.9

11.812.811.114.7

4.7

7.4

8.9

N.pachy. s.

(ft)

2.1

4.03.7

5.4

3.3

6.6

12.912.64.5

2.7

3.40.6

3.2

1.60.0

1.31.4

1.2

0.9

1.31.2

2.9

4.2

3.6

5.9

5.87.6

10.55.7

8.8

9.2

10.118.211.520.0

3.42.82.7

4.5

5.5

7.86.2

4.8

4.8

2.5

7.59.8

12.312.616.028.5

15.110.619.5

8.50.4

4.4

0.0

2.0

1.1

0.9

2.7

37.9

72.4

26.127.0

G.inflata

(ft)

25.5

17.920.722.1

13.1

12.8

8.316.114.2

13.612.49.2

10.214.18.6

10.210.111.9

4.09.0

9.0

9.1

10.111.212.512.715.312.513.012.711.013.610.816.924.730.231.135.830.916.920.227.940.229.025.220.721.316.412.921.216.1

17.211.97.2

13.523.013.919.216.9

10.510.317.112.6

11.5

27.621.7

Allother(ft)

61.1

62.361.7

59.3

68.6

59.7

63.4

45.864.2

63.5

67.862.7

69.7

70.270.4

74.0

68.6

69.3

72.2

65.7

65.6

61.9

65.8

62.2

56.654.252.054.4

56.0

55.8

56.856.6

54.3

55.336.4

46.850.239.7

47.9

55.5

56.048.2

40.8

43.847.1

54.958.2

62.3

65.3

42.5

44.0

51.1

56.6

61.9

55.247.4

52.654.2

53.1

56.358.7

54.0

29.5

11.5

36.6

41.5

SSTVv

( ° Q

13.6

12.0

11.5

12.9

12.9

13.4

12.011.7

11.9

14.4

13.214.5

14.4

14.014.814.1

13.5

14.6

15.3

15.8

16.1

15.6

14.6

14.815.1

13.814.5

12.614.7

13.612.6

11.610.5

10.2

7.9

13.312.1

14.1

12.39.7

10.910.713.411.512.911.212.510.810.9

8.5

8.2

10.211.010.311.216.816.918.015.5

18.217.517.1

8.0

0.4

8.0

7.5

Sub-bottomdepth

(m)

32.5632.7132.7132.8632.8633.0133.2333.3133.3133.4833.4833.6133.6133.7633.7633.9134.0634.2134.3634.4434.8134.9635.0235.1135.3335.4135.5835.7335.8635.9936.1636.3136.4636.4636.6136.6736.7636.8336.9137.0837.2137.3737.5137.6637.8137.9838.1138.1738.3338.4138.5838.7338.8639.0139.1639.2339.3139.3939.4639.6139.6739.7639.8339.8339.8939.9840.0340.0840.2140.3640.5140.6140.8340.9641.0941.1741.2641.3341.4141.5841.5841.71

δ 1 8 θ(‰)

4.44 U3.57 C4.42 U3.51 C4.05 U3.11 C3.35 C1.16U3.26 C4.51 U3.02 C2.75 C4.47 U3.66 C4.55 U4.53 U4.48 U4.37 U4.32 U4.20 U

3.18 C3.68 C3.22 C3.60 C3.55 C2.72 C3.09 C3.10 C2.71 C2.97 C2.52 C2.57 C3.63 U3.23 C

3.16C2.92 C1.96 C

3.55 C3.78 C

3.16C

3.05 C2.58 C3.14 C3.30 C3.37 C

4.48 U

3.35 C2.98 C3.29 C3.18 C

2.34 C2.68 C2.69 C2.55 C2.55 C1.98 C1.96 C4.48 U

4.42 U

3.45 C4.09 U3.84 U

G.

ruber

2.2

1.4

2.4

4.3

8.34.1

4.2

2.6

2.5

0.30.6

1.5

3.13.41.6

1.52.4

2.5

5.73.4

3.3

3.8

5.9

7.15.8

7.04.4

11.213.08.5

4.00.4

1.50.30.4

1.8

0.6

0.00.60.7

2.2

1.6

2.22.2

2.6

1.9

5.2

1.90.0

0.0

0.0

0.6

3.63.0

4.2

3.8

6.33.3

5.34.7

2.5

7.8

7.6

6.1

12.313.1

8.6

2.5

3.8

0.9

7.8

1.8

5.4

G.bulloid.

(ft)

9.5

9.8

15.6

18.113.313.5

15.2

9.6

14.4

6.813.57.9

9.316.78.4

13.624.413.210.916.712.09.5

10.214.916.013.314.5

8.4

10.98.8

12.63.3

5.54.1

10.811.6

5.4

4.84.0

6.8

6.2

8.8

9.98.7

7.1

9.611.96.94.91.7

3.4

7.0

6.4

10.116.68.2

8.910.319.810.38.8

6.6

10.911.614.111.422.419.99.0

9.116.713.1

14.0

N.

pachy. s.

(ft)

12.010.3

4.6

5.7

4.1

3.8

14.2

10.7

19.5

10.57.46.2

11.18.2

11.312.111.7

5.1

12.017.34.3

21.013.87.56.1

11.111.6

3.7

8.324.435.675.949.150.739.245.159.582.960.330.023.7

4.5

8.79.9

19.46.4

13.349.161.944.928.431.921.039.829.038.6

30.020.017.210.017.53.6

1.8

2.64.6

7.3

23.428.428.338.4

3.7

3.5

6.0

G.inflata

(ft)

29.524.6

18.7

8.212.716.2

17.7

20.2

14.4

18.326.416.434.923.420.422.416.212.420.316.127.712.111.518.814.19.2

11.3

15.914.27.9

9.8

3.3

16.819.516.29.4

11.40.6

12.919.815.314.620.419.29.7

9.2

14.17.28.1

21.119.813.120.216.910.311.4

15.113.611.215.316.617.712.019.016.315.214.54.3

14.78.4

10.714.9

18.7

Allother(ft)

46.953.9

58.7

63.761.662.4

48.6

57.0

49.0

64.152.168.041.548.358.350.345.466.951.046.452.753.758.651.658.059.558.2

60.853.750.338.017.227.125.433.532.123.111.622.142.752.670.558.860.161.272.955.635.025.132.348.547.348.830.339.938.0

39.752.746.559.754.564.467.660.652.852.931.045.044.243.161.266.7

55.9

SSTW

(°C)

10.910.8

11.6

11.614.112.8

10.3

11.2

8.9

10.810.612.112.011.110.89.8

8.2

11.912.09.2

13.110.011.712.912.412.210.9

15.914.911.38.2

1.34.23.0

5.66.0

2.7

0.9

2.3

7.39.2

12.411.411.310.112.011.35.92.7

4.2

7.6

7.5

10.06.5

8.6

7.8

9.6

9.89.6

12.010.015.114.814.215.415.210.47.69.0

7.0

13.612.0

12.7

875

Page 22: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

Appendix C (continued). Appendix C (continued).

Sub-bottomdepth(m)

41.8641.8641.9942.0742.1642.1642.3142.3142.4642.6142.6642.8342.9143.0843.1843.3643.5143.6643.8143.9644.0144.4144.5644.7144.9345.0145.1045.1045.1845.1845.1845.3145.4645.6145.7645.9146.0646.0646.2146.2946.4346.5146.6846.7946.9646.9647.1147.2647.4147.4447.4847.5647.6347.7147.8047.9348.0348.1848.3148.4148.4348.4648.6148.6948.7648.9149.0649.1949.3049.4349.5149.6849.8149.8549.%50.0950.1150.2650.4150.4150.4850.56

δ 1 8 θ(%o)

3.74 U2.69 C

2.94 C4.04 U3.31 C4.14 U

3.16 C2.97 C2.97 C2.92 C3.47 C3.31 C1.85 C3.08 C

3.03 C2.57 C

2.71 C3.47 C3.38 C2.45 C4.41 U3.22 U2.42 C2.53 C3.12 U2.64 C2.25 C2.48 C2.54 C2.36 C2.54 C2.70 C3.05 C2.93 C3.11 C3.59 U2.62 C2.82 C2.79 C3.19 C2.88 C3.25 C

3.51 C3.10C3.34 C3.36 C3.19 C2.97 C3.14 C3.67 U2.76 C

2.58 C2.81 C2.73 C2.73 C2.75 C2.77 C2.85 C

2.67 C2.72 C2.79 C3.45 C2.90 C

4.16 U4.19 U4.43 U3.86 C4.36 U4.31 U3.41 C

G.ruber( * )

5.2

2.3

6.11.8

3.3

2.6

5.95.52.9

3.91.46.0

6.3

5.58.55.8

12.313.83.64.43.13.3

1.514.1

9.6

17.721.422.320.822.914.5

10.38.55.66.8

12.112.713.3

7.14.01.94.73.42.55.22.9

6.34.79.58.5

11.613.616.614.211.718.312.818.415.511.320.1

9.117.115.414.414.96.4

5.96.0

5.5

4.28.0

G.bulloid.

( * )

12.6

13.811.210.7

3.3

6.7

9.411.013.110.58.19.18.56.1

11.88.8

8.312.410.510.314.511.212.510.6

13.3

4.87.45.08.19.1

16.5

10.317.39.44.5

11.812.610.4

10.211.25.36.8

6.8

5.59.55.2

10.19.48.47.7

6.8

11.612.89.1

11.414.314.110.214.514.115.0

17.8

11.615.110.8

13.37.3

6.8

5.33.4

7.7

8.7

N.pachy. s.

(%)

4.8

16.415.122.7

13.9

5.43.85.88.7

25.850.734.928.839.9

9.9

18.84.33.2

36.536.329.032.0

4.90.5

1.1

2.30.01.70.0

3.11.2

16.126.6

4.923.4

2.46.52.9

8.124.5

9.7

9.411.516.823.639.820.620.310.210.77.17.9

7.3

4.73.92.7

4.23.0

0.3

10.80.82.2

2.6

0.64.96.5

14.9

7.410.37.9

4.53.1

G.

inflata

11.3

6.412.5

8.7

16.2

26.615.715.020.2

5.85.5

11.011.011.718.715.417.412.95.3

10.613.48.26.1

22.3

14.8

12.914.49.07.8

18.617.3

19.714.622.320.120.510.910.7

18.314.930.528.828.323.425.914.618.615.231.915.615.3

8.3

6.210.78.89.1

11.26.3

13.217.22.8

14.110.76.8

4.24.94.7

13.912.67.6

26.813.9

Allother(%)

66.1

61.155.156.1

63.2

58.765.262.755.154.034.239.045.536.851.151.357.657.644.138.440.045.374.952.4

61.3

62.356.862.063.446.350.6

43.633.057.845.153.257.462.8

56.345.552.550.350.051.835.737.544.350.440.057.559.258.657.161.264.255.557.762.056.646.761.456.958.162.165.760.366.7

66.165.975.5

56.866.2

SSTV(°C)

13.0

9.611.4

8.9

11.7

13.114.013.111.29.55.69.1

10.08.2

13.311.016.116.28.48.48.18.6

11.818.0

15.4

17.919.218.718.718.617.0

12.810.413.910.816.515.016.3

13.49.3

12.013.011.910.49.67.1

10.710.314.813.515.215.015.716.115.417.115.417.317.313.817.814.417.116.815.915.412.2

13.513.113.7

13.914.9

Sub-bottomdepth(m)

50.5850.7150.7850.9351.0051.0151.0151.1851.1851.3151.4651.6151.7651.9152.0652.2152.2852.4352.5152.6052.6852.8152.9653.0953.2653.4153.4954.0554.1654.2954.3754.5354.6154.7854.9155.0655.2155.3655.5155.6655.7455.8155.8756.0356.0356.1356.2856.4156.5656.7156.8657.0157.1657.2957.3757.5357.6357.7857.9158.0658.2158.3558.3658.5158.6658.7958.8358.8759.0359.0959.1959.2859.4159.5059.5659.7159.8660.0160.1660.3060.3760.53

δ 1 8 θ(‰)

3.62 C

4.15 U

4.06 U3.19 C3.88 U

3.03 C2.16 C2.40 C2.55 C

2.66 C4.36 U4.43 U4.51 U4.48 U

2.95 C3.41 C

2.91 C2.73 C2.67 C

3.64 U3.65 U2.86 C

2.68 C3.30 C3.88 U4.00 U

3.14 C

4.26 U4.09 U3.42 U2.92 C3.57 U2.63 C2.08 C2.73 C

3.07 C3.20 C3.45 C

3.55 C

3.75 U3.54 U

2.80 C

2.95 C3.41 C

3.51 C

2.10 C

4.38 U

G.ruber

W

8.95.9

10.313.511.813.7

8.4

7.2

22.114.818.710.27.0

5.68.50.9

1.43.55.86.5

16.910.621.815.314.24.6

10.07.5

12.615.615.612.75.77.06.57.3

10.22.52.75.06.4

19.4

16.413.118.319.8

6.7

7.84.98.22.7

3.6

6.13.7

4.52.7

7.1

10.2

6.9

10.66.8

6.2

1.67.14.65.38.7

4.7

11.010.012.615.315.64.42.8

1.13.1

G.bulloid.

w8.66.7

10.75.38.94.3

7.2

7.6

13.111.714.010.210.44.09.7

7.2

2.8

8.97.26.2

7.18.8

16.111.711.911.110.314.212.110.112.611.313.013.416.410.110.210.112.29.2

11.67.7

9.410.5

8.3

10.78.1

15.012.710.57.87.7

4.07.18.6

6.5

14.719.0

12.912.312.813.1

12.311.819.715.214.58.3

15.215.212.08.4

12.011.315.314.28.7

N.pachy. s.

(%)

5.12.60.72.31.0

2.2

0.0

2.0

0.00.8

0.30.7

1.21.60.3

1.20.00.7

0.34.90.3

0.30.40.31.60.9

0.7

1.10.00.01.70.0

0.40.00.3

0.6

1.21.21.00.41.50.7

1.01.30.7

1.51.40.63.65.1

12.213.120.218.316.30.40.9

0.3

1.41.44.19.9

16.814.512.45.35.50.7

3.11.60.51.12.7

11.617.919.59.0

G.inflata(*)

16.823.410.322.023.620.5

16.4

16.123.219.115.721.119.526.713.916.231.216.118.615.415.427.318.817.329.025.618.928.122.716.711.68.0

24.024.315.019.00.3

28.725.838.327.114.3

14.015.614.69.9

31.613.811.615.217.214.29.8

19.521.122.118.711.2

23.812.319.69.1

8.5

16.815.928.820.416.021.414.816.610.218.320.415.323.83 1 . 3

Allother(%)

60.661.368.056.954.659.3

68.0

67.141.5

53.551.3

57.861.962.267.674.564.570.968.167.060.353.042.955.343.257.760.049.152.657.658.568.056.955.361.863.078.157.558.347.153.457.9

59.159.658.158.052.362.867.261.060.161.359.951.549.568.458.659.3

55.063.456.761.7

60.849.847.445.550.970.349.358.458.365.051.552.448.641.447.9

SS1\v

( ° Q

14.815.015.917.517.317.5

16.1

15.220.417.718.416.515.115.715.713.315.014.115.314.418.317.619.517.818.614.616.315.717.618.017.016.714.915.514.115.415.713.913.616.815.318.6

17.816.818.418.016.214.713.214.311.211.411.510.510.914.414.615.0

15.015.714.012.2

9.4

11.810.013.514.114.615.715.216.817.417.211.59.18.0

12.3

876

Page 23: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

Appendix C (continued).

PALEOCEANOGRAPHY FROM NORTH ATLANTIC SITES 607 AND 609

Appendix C (continued).

Sub-bottomdepth

(m)

60.6160.7860.9161.0661.2161.3661.5161.6661.8161.8762.0362.1162.1962.2862.4162.5662.6462.7162.8663.0163.1663.2463.6563.7663.9163.9864.1364.2164.3864.4964.6664.7364.8164.8964.9665.1365.2665.2665.3965.4165.4865.6365.7165.8866.0166.1666.2966.4666.6166.7666.8166.9166.9867.1367.2367.3867.4967.6667.7967.9668.1168.2668.3168.4168.4768.6368.7168.8869.0169.1669.3169.4669.6169.7669.8069.9170.1370.2170.3670.3870.5170.66

5 1 8O

(‰)

4.34 U4.11 U3.25 C2.92 C2.76 C2.67 C

2.70 C2.74 C

3.63 C

3.80 C

3.00 C

3.02 C

3.57 C

3.44 C3.27 C

3.70 U3.54 U3.44 U3.00 C3.37 U2.89 C

4.16 U4.39 U4.34 U4.20 U4.03 U3.30 C

3.94 U

2.88 C2.69 C

2.89 C

3.15 C

3.40 C3.74 C3.59 C

3.68 C

3.70 C3.15 C

3.09 C

2.86 C

G.

ruber(%)

3.4

2.1

1.58.2

14.418.812.217.812.52.7

2.7

4.4

6.2

5.2

2.04.1

8.7

12.215.714.318.016.6

3.1

2.81.01.7

1.2

3.6

4.16.9

4.0

3.34.9

5.65.1

14.611.0

6.7

4.1

11.35.4

5.66.6

6.3

4.8

9.0

8.44.0

3.2

4.0

4.4

8.912.313.39.9

11.88.1

11.711.67.9

6.0

6.89.5

20.616.114.59.2

10.39.5

9.3

10.510.58.8

11.214.213.7

10.715.917.0

G.

bulloid.

( * )

7.5

12.56.6

12.015.211.49.3

10.010.39.9

13.910.99.2

8.7

8.2

11.113.014.112.316.016.114.511.38.89.9

7.9

11.78.9

10.88.0

10.312.1

8.6

5.6

10.615.713.0

10.77.9

3.3

8.3

13.511.07.8

7.5

4.1

10.08.38.6

9.4

8.2

9.9

11.010.7

7.4

5.67.1

4.56.4

12.913.8

6.86.1

9.8

8.98.0

7.58.8

8.9

6.9

8.6

6.8

4.64.1

8.2

9.7

11.015.219.5

N.

pachy. s.(%)

9.1

3.9

3.8

1.31.1

0.0

1.4

3.1

4.5

16.019.68.0

9.2

11.714.119.09.4

8.0

1.41.4

0.9

1.1

6.87.7

13.412.712.813.913.27.2

25.826.9

8.6

4.04.0

3.02.7

5.4

7.2

7.68.0

6.96.68.1

9.2

8.214.119.915.2

5.4

5.1

2.41.7

2.6

3.4

2.8

4.22.6

3.5

11.418.0

2.71.4

0.0

1.1

2.1

2.911.9

3.9

1.2

2.8

8.4

17.39.5

0.7

4.3

1.1

0.0

0.4

G.inflata

(*)

27.523.825.325.117.014.822.915.218.619.413.518.527.823.619.722.218.719.217.213.320.223.131.330.336.741.136.423.824.933.116.213.813.824.627.020.615.0

17.422.617.617.416.512.122.729.023.218.419.921.816.420.813.411.316.512.322.021.819.914.214.513.819.522.019.321.817.311.316.520.319.819.824.024.015.617.521.3

23.529.123.8

All

other(%)

52.557.762.753.552.355.054.153.954.252.050.358.247.650.755.943.750.246.653.555.144.744.847.650.439.036.637.949.847.144.843.843.864.260.153.346.158.5

59.858.260.260.957.463.655.249.555.449.148.051.364.861.465.463.757.067.057.858.861.364.553.348.564.261.050.352.158.169.152.557.462.858.350.345.359.759.451.0

53.739.839.4

SS1\v(°C)

12.412.313.115.817.018.617.217.516.010.19.1

12.313.412.210.410.013.314.817.516.518.618.612.712.510.311.610.411.011.214.79.2

8.7

12.614.714.116.915.6

13.812.915.413.012.613.313.513.014.812.610.110.613.013.515.216.316.615.516.915.216.816.112.510.715.116.519.418.417.315.413.715.516.316.115.012.514.817.616.7

16.719.919.2

Sub-bottomdepth

(m)

70.8170.9671.1171.2671.3971.4871.6371.7171.8871.8871.9971.9972.1672.3172.4672.6172.6573.2173.3673.5173.7373.8173.9874.1174.2674.4174.5674.7174.8675.0175.2375.3175.4875.6175.7675.9176.0676.2176.2876.3676.5176.7376.7376.8176.9876.9877.1177.2677.4377.5677.7377.8678.0178.2378.3178.4878.6178.7678.9179.0679.2179.3679.5179.7379.8179.9880.2680.4180.5680.6180.7180.7180.8680.9981.2381.3181.4881.5981.7681.9182.0682.21

δ 1 8 θ(‰)

3.10 C

3.94 U

3.50 C

3.10 C

2.86 C3.58 U3.21 C3.60 U4.08 U3.05 C4.20 C

2.73 C

2.90 C2.91 C3.12 C

3.35 C

4.03 U3.89 U3.64 U2.68 C

2.95 C

2.81 C

4.33 U

3.01 C3.55 U3.66 U3.62 U3.01 C2.82 C2.94 C

3.56 U2.83 C

3.11 C3.80 U

2.82 C

3.40 C

G.

ruber(%)

13.715.44.99.4

1.0

0.9

6.2

18.35.4

10.6

4.9

4.8

6.5

10.68.7

20.525.224.123.420.918.78.96.2

4.1

5.53.6

5.1

7.59.4

11.311.112.011.49.38.74.0

2.6

2.96.3

6.3

8.7

7.4

13.89.95.4

6.513.910.018.816.715.415.718.316.125.616.711.410.55.3

7.0

5.6

5.1

6.53.1

1.4

2.5

4.5

9.6

5.5

11.210.19.9

6.05.1

8.7

8.6

3.0

G.bulloid.

( * )

12.34.18.5

8.3

14.55.9

9.37.3

11.7

8.3

7.27.9

10.511.011.610.1

8.3

13.36.1

7.49.0

10.914.79.5

8.211.19.5

9.66.2

7.06.9

7.5

6.1

11.09.18.3

4.512.97.0

10.7

16.49.1

9.4

7.312.710.714.712.911.1

7.6

12.99.5

6.96.86.9

8.8

9.5

14.57.5

10.510.211.07.77.9

13.610.617.4

11.511.512.210.714.418.015.912.19.8

7.0

N.

pachy. s.(%)

1.4

1.516.114.417.720.114.16.4

9.5

13.1

9.2

12.07.8

11.09.41.4

1.1

1.82.4

1.29.4

13.716.814.614.13.0

1.2

1.80.7

1.80.5

1.2

0.7

1.7

0.71.91.4

1.91.4

1.7

1.7

1.8

2.00.0

1.0

1.8

1.1

0.92.3

2.3

1.7

0.9

1.01.3

2.3

2.63.2

0.7

1.70.7

3.63.3

1.52.4

2.92.7

3.0

2.1

2.6

1.6

2.9

4.93.20.7

1.7

2.0

1.8

G.inflata

w21.622.916.116.313.822.020.316.215.6

19.6

21.323.413,113,514.216.916,520.814,920.724.5

7.2

12.419.012.023.023.630.525.118.320.918.418.619.618.911.318.622.216.924.0

23.218.5

16.222.120.717.315.410.010.016.711.28.0

2.4

1.68.4

11.824.422.121.722.021.922.118.922.821.126.024.2

21.713.211.515.917.113.814.112.1

7.8

13.7

All

other

W

51.056.054.451.753.151.150.251.757.8

48.4

57.451.962.153.956.151.148.940.153.249.838.459.449.952.960.159.360.750.658.661.660.760.863.258.462.674.572.860.168.357.3

50.063.2

58.660.760.263.754.966.257.956.758.766.071.474.356.860.151.652.263.859.858.758.565.363.861.158.250.9

55.067.263.560.353.659.064.165.471.874.4

SSTW

(°C)

17.418.411.113.08.4

9.1

11.916.812.2

13.6

12.812.013.113.713.418.719.419.718.719.316.612.710.811.011.813.414.816.217.016.617.117.017.115.716.014.014.213.115.115.0

15.315.2

17.017.014.314.616.815.517.617.716.917.418.017.518.617.316.616.414.815.414.113.915.113.812.013.313.0

15.813.815.815.514.612.913.515.015.213.9

877

Page 24: 22. Paleoenvironmental Results from North Atlantic Sites 607 and 609

W. F. RUDDIMAN, A. McINTYRE, AND M. RAYMO

Appendix C (continued).

G.ruber

G.bulloid.

(<Vo)

N.pachy. s.

(°7o)

G.inflata

(<Vo)

Allother(%)

Sub-bottomdepth δ 1 8 θ ruòer bulloid. pachy. s. irç/7αto other SSTw(m) (‰)

82.36 7.8 10.6 1.4 12.8 67.4 15.082.51 3.31 C 3.0 10.7 1.7 13.7 71.0 13.3

Note: Oxygen isotope values are unadjusted and are relative to PDB standard. A" U " indicates Uvigerina, and a " C " indicates Cibicides. The planktonic fora-minifer species name abbreviations stand for: G. ruber—Globigerinoides ruberwhite; G. bulloid.—Globigerina bulloides; N. pachy. s.—Neogloboquadrinapachyderma sinistral; G. inflata—Globorotalia inflata; All other—all other spe-cies combined. SSTW stands for estimated winter sea-surface temperature.

878