AN ABSTRACT OF THE THESIS OF
Ann Louise Sabin for the degree of Master of Science in Oceanography presented on
October 4. 1994. Title: Holocene and Latest Pleistocene Paleoceanography of the
Northeast Pacific and its
in the Pacific Northwest
Redacted for privacy
Abstract approved:..
Nicklas G. Pisias
Northeast Pacific Ocean sediments were analyzed to determine the past
relationship between northeast Pacific sea surface conditions and the climate on the
adjacent continent, the Pacific Northwest of North America. Studies of modern
ocean-atmosphere interactions demonstrate the significant effect sea surface conditions
and atmospheric circulation in the Northeast Pacific Ocean has on the climate of the
west coast of North America. Thus, it is likely that past continental climate change
can be correlated to changes in sea surface temperature in the northeast Pacific Ocean.
We analyzed radiolaria from twelve sediment cores, ranging from 33.62°N to
54.42°N latitude along the west coast of North America to reconstruct past sea surface
conditions. Relationships between modern radiolaria and mean annual sea surface
temperature calibrate equations used to estimate sea surface conditions for the past
20,000 years. Chronology is controlled by radiocarbon ages from planktonic
foraminifera and bulk organic carbon.
The reconstructions of sea surface conditions from changes in radiolaria
assemblages indicate that the upwelling center off the west coast of North America
was further south 15,000 years ago than it is today, and reached its present location
13,000 years ago. We infer that the West Wind Drift and Transition Zone were
further south in the latest Pleistocene as a result of a more southerly North Pacific
High pressure cell prior to 13,000 years ago.
Two Pacific Northwest continental records of paleotemperature are well
correlated to the sea surface temperature record the northeast Pacific around 48N
latitude, with temperatures increasing over the past 20,000 years. Significant
temperature minima and glacial expansions occurred at 13,000 and 4,000 years ago in
the records examined, as did a minor minimum at 16,000 years ago. We conclude
that changes in the past latitudinal position of the West Wind Drift played a significant
role in controlling continental climate immediately to its east, as it does in the present
day environment.
Holocene and Latest Pleistocene Paleoceanography
of the Northeast Pacific and its Relationship
to Climate Change in the Pacific Northwest
by
Ann Louise Sabin
A THESIS
submitted to
Oregon State University
in partial fulfillment of
the requirements for the
degree of
Master of Science
Completed October 4, 1994
Commencement June 1995
Master of Science thesis of Ann Louise Sabin presented on October 4. 1994
APPROVED:
Redacted for privacy
Major Professor, representing Oceanography
Redacted for privacy
Dean of the College of Oceanic
d Xtmospheric Sciences
Redacted for privacy
Dean of Graduate
yol
I understand that my thesis will become part of the permanent collection of Oregon
State University libraries. My signature below authorizes release of my thesis to any
reader upon request.
Redacted for privacy
Ann Louise Sabin, Author
ACKNOWLEDGMENTS
I would like to thank my advisor, Nick Pisias for his support during the past
three years. I have enjoyed the opportunity of working with him, and his guidance
and advice were very important to this work. Alan Mix played the role of unofficial
advisor and his assistance was invaluable as well.
Linda and Calvin Heusser supplied the continental temperature and
precipitation records, without which this work would not be as significant.
Joe and Leigh have given me endless encouragement as well as an audience
for bouncing ideas. I have enjoyed being your officemates, and your insights,
academic and otherwise, have kept me going.
Sara and Carolyn, thank you for your unending support and well of
confidence when mine was running low. Jim, Ann, Mysti, and all the rest in the
Foram and Rad labs provided comic relief (and other forms of companionship),
especially during those highly stressful moments. Donna Witter and Eileen Hemphill-
Haley have each in their own way given me courage to get to where I am. And thank
you to everyone else who played a role but I have not mentioned.
Thank you to those who really kept me sane -- Kelly, Ann, Mom, Dad,
Jessie, Rube, Phineas, Gus, and, yes, the Corvallis Belly Dance Performance Guild.
And thank you, my Matthew, for not going insane during this adventure. I
wouldn't have made it without you.
This research was supported by the U.S. Geological Survey under Contract
1434-92C-50016, and by the Northwest College and University Association for
Science (Washington State University) under Grant DEFGO6-89ER-75522 with the
US. Department of Energy.
TABLE OF CONTENTS
INTRODUCTION
1
REGIONAL SETTING
3
Water Masses and Currents
Continental Background
3
10
13
METHODS
Chronology
Paleotemperature Equation
15
18
26
RESULTS
Factor Analysis of Core Top Data
Down Core Analysis
Factor Analysis of Down Core Data
Sea Surface Temperature
DISCUSSION
Summary of Past Oceanographic Conditions
Comparison to the Continental Record
26
37
38
61
68
68
69
CONCLUSIONS
74
BIBLIOGRAPHY
76
APPENDICES
79
APPENDIX A
APPENDIX B
APPENDIX C
80
86
90
LIST OF FIGURES
Page
Figure
1.
North Pacific surface circulation patterns and upper ocean domains.
3
2.
Seasonality of the California Current for a) winter; b) early spring;
c) summer.
5
3.
Long-term mean atmospheric pressure at sea level for a) January
and b) July.
6
4.
Long-term mean wind stress (dynes*cm2) in the California Current
for a) January, b) April, c) July, and d) October.
7
5.
Geography of the Pacific Northwest.
10
6.
Location of marine sediment cores and continental data sites used in this
study.
13
7.
Sedimentation rates of the marine cores used in this study.
19
8.
Map of residuals for the northeast Pacific from the sea surface
temperature equation.
24
9.
Comparison of the radiolaria based temperature equation to the
alkenone based temperature equation at site W8709a-PC,TC8.
24
10..
Present day communalities of the Pisias et al (in prep) factor analysis
for the northeast Pacific.
26
11.
Present day distribution of factor 1, the Subtropical factor.
28
12.
Present day distribution of factor 2, the Transitional factor.
30
13.
Present day distribution of factor 4, the Eastern Boundary Current
factor.
32
14.
Present day distribution of factor 5, the Arctic factor.
35
15.
Present day mean annual sea surface temperature from the
northeast Pacific Ocean.
37
16.
Communality of the radiolaria factors, 20 ka to present.
39
LIST OF FIGURES (continued)
Page
Figure
17a.
17b
Distribution of the Subtropical factor, 20 ka to present;
an interpolated graph of latitude vs. age.
17m.
Time series of the Subtropical factor at each core site.
40
41
45
1 8a.
Distribution of the Transitional factor, 20 ka to present;
an interpolated graph of latitude vs. age.
1 8b.
1 8m.
Time series of the Transitional factor at each core site.
46
1 9a.
Distribution of the Eastern Boundary Current factor, 20 ka to present;
an interpolated graph of latitude vs. age.
51
19b - 19m.
Time series of the Eastern Boundary Current factor
at each core site.
52
20a.
56
Distribution of the Arctic factor, 20 ka to present;
an interpolated graph of latitude vs. age.
20b - 20m.
21 a.
Distribution of sea surface temperature, 20 ka to present;
an interpolated graph of latitude vs. age.
2 lb - 2 im.
22.
Time series of the Arctic factor at each core site.
Time series of sea surface temperature at each core site
a) and b): Hoh Bog records from Heusser, Heusser and Streeter, 1980;
57
62
63
70
c) Sea surface temperature estimates from cores TT39-PC12,
Tr39-PC 17
23.
a) and b): Marion Lake records from Mathewes and Heusser,
71
1981; c) Sea surface temperature estimates from cores TT39PC12, TT39-PC17.
24.
Comparison of the SST record at U39-PC12, TT39-PC17 to
continental temperature records at a) Hoh Bog and b) Marion Lake.
75
LIST OF TABLES
Page
Table
1.
Location of marine cores used in this study.
14
2.
Radiolaria species used in factor analysis.
16
3.
Regression equation used on radiolaria factors to obtain estimated
mean annual sea surface temperature.
23
A.1.
Depths and dates of cores. Raw ages are from planktonic foraminifera
using 14C AMS techniques, unless otherwise noted.
80
A.2.
Dates of continental pollen sites. Raw ages are from bulk organic
carbon.
84
A. 3.
Dates of continental glacial events. Raw ages are from bulk organic
carbon.
85
B. 1
A summary of factor loadings from core tops used in the Pisias et al
factor analysis.
86
C. 1
Pseudofactor matrices of the twelve marine cores used in this study.
90
LIST OF APPENDICES
Appendix
Page
A. 1.
Depths and dates of cores. Raw ages are from planktonic foraminifera
using 14C AMS techniques, unless otherwise noted.
80
A.2.
Dates of continental pollen sites. Raw ages are from bulk organic
carbon.
84
A.3.
Dates of continental glacial events. Raw ages are from bulk organic
carbon.
85
B.
A summary of factor loadings from core tops used in the Pisias et al
factor analysis.
86
C.
Pseudofactor matrices of the twelve marine cores used in this study.
90
Holocene and Latest Pleistocene Paleoceanography
of the Northeast Pacific and its Relationship
to Climate Change in the Pacific Northwest
INTRODUCTION
The continental Pacific Northwest has experienced significant climate
variations since the last glacial advance (around 18 ka, ka = one thousand years ago),
with major changes in temperature, precipitation and vegetation. At the beginning of
the Holocene (10 ka), temperature was warmer and precipitation was lower than
present (Heusser et al, 1980; Mathewes and Heusser, 1981). A fundamental problem
in understanding these variations in regional climate is the absence of a known forcing
of climate change on time scales less than 10,000 years.
In the modem climate, sea surface conditions and continental climate are
linked through atmospheric teleconnection (Namias, 1959). Thus, we hypothesize
that past climate change in the Pacific Northwest must, in part, be controlled by
changes in sea surface conditions (primarily sea surface temperature, SST) in the
neighboring ocean, the northeast Pacific, and associated changes in atmospheric
circulation. We would expect the climate patterns found in the continental Pacific
Northwest and SST patterns found in the northeast Pacific Ocean during the
Pleistocene-Holocene transition (11 to 8 ka) should show similar patterns. The goal
of this study is to document changes in sea surface temperatures in the Northeast
Pacific during the past 20,000 years and to relate these changes in oceanic conditions
to continental climate change of the Pacific Northwest.
2
This study is presented in four parts. First, a summary of the regional setting
is given for both marine and continental environments. The second section outlines
experimental methods used. Third we present the results obtained by these methods.
In the fourth section, the discussion is divided into two parts. First, the
environmental implications of the data analysis are discussed, integrating factor
analysis and temperature estimates. Second, we compare these findings to the
continental record. A Conclusions section outlines the key results from this research.
3
REGIONAL SETTING
Water Masses and Currents
The northeastern Pacific can be divided into three major oceanographic
regions; the Transition Zone, the California Current and the Alaskan Stream (Figure
1). These three regions along the west coast of North America are influenced by
continental runoff, upwelling, and by the West Wind Drift. In the southern part of the
California Current, equatorial currents are also important. The West Wind Drift, the
surface current which forms the northern limb of the North Pacific Gyre, crosses the
Pacific Ocean between approximately 400 and 50°N latitude. Its northern edge defines
the Subarctic Front. The Alaskan Gyre, defined by a cyclonic flowing current, is
north of the West Wind Drift. The region where the West Wind Drift intersects the
coast of North America is referred to as the Transition Zone, and marks
120°
160°W
60°
/._..f.?J
N
SiJBARCflC 1RONT
NORTH PACIfIC GYRE
CAUFORN
IXTENSION
160°E
180°
160°W
140°
Figure 1. North Pacific surface circulation patterns and upper ocean domains.
Adapted from Hickey, 1979
the beginning of both the southward flowing California Current and the northward
flowing Alaskan Stream. Both flow along the coast of North America. The
California Current defines the eastern boundary of the North Pacific Gyre and the
Alaskan Stream defines the eastern and northern boundaries of the Alaskan Gyre.
The geographic location of the Transition Zone is highly variable. Pickard and
Emery (1990) state that the northern boundary of the California Current is 45°N in the
summer and 40°N in the winter. Hickey (1989) places the northernmost extent of the
California Current at 50°N and does not discuss seasonal variability. Mysak (1977)
extends the current as far north as 52°N. As the West Wind Drift migrates seasonally,
most authors treat the region as a wide domain with unstable boundaries which
migrate up and down the coast between 40° and 50° N latitude.
The California Current System is the most completely studied of the three
oceanographic regions. The core of the current is located approximately 300 km west
of the coastline and is found over a depth range of approximately 150m. Underneath
the California Current, the California Undercurrent flows poleward and over the
continental slope with a jetlike structure to its flow (Hickey, 1989). The Southern
California Countercurrent also flows poleward, and is located south of Point
Conception, California (Figure 2).
Seasonal changes in the California Current are due to the migration of the
North Pacific High atmospheric pressure cell. The pressure cell migrates 10°
southward in the winter from its summer position at 38°N latitude (Huyer, 1983;
Figure 3). This migration causes a change in coastal wind patterns (Figure 4) and in
turn affects the local currents. South of Point Conception, the California
Undercurrent reaches its maximum strength during the summer; to the north it is
strongest and most continuous in the winter, when it shoals off Washington and
Oregon. It is then
5
B.
A.
130
1OW
130
iZOW
4O
3O
N
130
iD'w
130
120W
C.
CC = California Current
DC = Davidson Current
SCC = Southern California
Current
SCE = Southern California
Summer
Eddy
120W
Figure 2. Seasonality of the California Current for a) winter,
b) early spring, c) summer. From Huyer, 1983
referred to as the Davidson Current and displaces the California Current offshore
(Figure 2).
The seasonal migration of the North Pacific High pressure cell is associated
with a strong seasonal cycle of upwelling in northern parts of the California Current.
Upwelling is the result of offshore Ekman transport of surface waters, due to
northeasterly winds when the North Pacific High migrates northward in the summer.
Upwelled waters are a mixture of low latitude waters advected north by the California
Undercurrent and subarctic waters. The upwelled waters are cold and nutrient rich,
Figure 3. Long-term mean atmospheric pressure at sea
level for a) January and b) July. From
Huyer, 1983.
leading to very high productivity in the California Current. South of San Francisco,
upwelling occurs year-round, and is strongest in spring. North of San Francisco,
upwelling is strongest in July. It is relatively weak off central Oregon, and a
distinctly seasonal phenomenon (Huyer, 1983).
The Alaskan Stream flows northward along the west coast of Canada and
south coast of Alaska. This narrow, high velocity stream enters the Bering Strait at
the Aleutian Islands and defines the north and east boundaries of the Alaskan Gyre.
The Alaskan Stream is composed of many closed eddy circulations, which reflect
7
Figure 4. Long-term mean wind stress (dynes*cm2) in the
California Current for a) January, b) April, c) July, and d)
October. Contours correspond to constant magnitudes of
0.5, 1.0 and 1.5 dynes *cm..2; areas in excess of 1.0
dynes*cm2 are shaded. From Huyer, 1983.
A
I32WI3O
I28
26
124
)22
)2O
D.
C.
B.
J18
I)6
4anuory
1140
1120
1200
1180
lI6
114°
April
Figure 4.
112°
20° 1180
1160
JuIy
114°
112°
1200
1180
1160
October
114°
112°
bottom topography (Mysak, 1977). As a result, the current is not a strong eastern
boundary current, and does not follow a predictable path.
Upwelling has not been observed along the Alaska coast and only weak
summer upwelling has been observed off the Canadian coast (Freeland et al, 1984).
The Alaskan Low atmospheric pressure cell exists over the Gulf of Alaska most of the
year. Winds blow from east to west along the southern coast of Alaska, creating
downwelling conditions almost year round. Along the Canadian coast, the current is
northward for most of the year, with a change in the surface waters (<300m deep) in
summer. Summer currents are southward, a response to the North Pacific High
seasonal migration, and weak upwelling has been observed. This coastal current is
also partially driven by the freshwater outflow from the Juan de Fuca Strait (Freeman
etal, 1984).
Superimposed on the Northeast Pacific's seasonal variability is interannual
variability, partially the result of changes in the dynamic topography of the North
Pacific Gyre. Intensity of flow in the California Current varies interannually largely
due to remote forcing by the tropical Pacific and is most pronounced in the southern
California Current. This change in intensity of flow is tied to the El Niflo-Southern
Oscillation (ENSO), which occurs in the tropical Pacific on an irregular basis (ParesSierra and O'Brien, 1989). Effects are communicated to the Northeast Pacific by both
oceanic and atmospheric processes.
Poleward propagating waves generated in the tropical ocean during an ENSO
event take on the form of coastal Kelvin waves. These waves account for much of the
low frequency variability in the California Current during an ENSO event, and are
thought to be the primary mechanism for the simultaneous occurrence of tropical and
mid-latitude ENSO events (Pares-Sierra and O'Brien, 1989).
10
Atmospheric communication of ENSO effects occur through the troposphere
in a Hadley Cell circulation. While the atmosphere appears to be secondary for
forcing interannual variability, its minor variations may greatly enhance those of the
Kelvin waves. The anomalous waves and SST can result in anomalously warm or
cold years, which in turn affects productivity in the area (Thomas and Strub, 1989).
Continental Background
The Pacific Northwest can be
divided into two lowland provinces, the
knds
coast region and the Columbia Basin
(Barnosky et al, 1987).
Separating
çw1ands
these provinces is the Cascade
Mountain Range. This study focuses
on the region to the west of the Cascade
Mountain Range. This region is made
up of the Puget Lowland and the
Coastal Mountain Ranges (Figure 5).
H
Figure 5. Geography of the Pacific
Northwest.
Presently, the northwest coast of North
America is a temperate climate. Mean
annual precipitation averages around 2200-2400 mm/yr and temperatures average
16°C in the summer. Douglas Fir and Alder are the dominant vegetation types today,
with Western Hemlock on the coast and Oak further inland (Bamosky et al, 1987).
Winds come from the west during the winter, and are strong from the northwest
during the summer.
11
What connects the two climate regimes of ocean and continent? Namias
demonstrated in numerous papers (1959, 1963, 1966, 1969, 1974) that modem sea
surface temperature and the atmospheric conditions which affect continental climate
are highly correlated. Changes in the mid- and upper-level troposphere affect the
continental climate the most. Over the Northeast Pacific, the position of the
anticyclonic North Pacific High pressure cell normally dominates the weather; the
cyclonic Alaskan Low pressure cell plays a secondary role. The results of Namias
(1959, 1963) suggest that there is a correlation of sea surface temperature anomalies
to anomalies in atmospheric circulation. In 1963, Namias presented statistical
evidence that anomalies in atmospheric circulation were partially the result of
anomalous water temperatures and coupled ocean- atmosphere interaction.
A warm pooi of water in the North Pacific Ocean can cause greater diabatic
heating and vertical instability. This heat and vertical instability warms and
strengthens Asiatic cyclones as they move across the Pacific Ocean. The strength and
warmth of the Asiatic cyclones are communicated to the Northeast Pacific circulation
at migratory fronts. Adiabatic rise from the sea and horizontal dispersion of warm air
increases the strength of the Alaskan Low pressure cell, resulting in more movement
of air. A strengthened cyclone in the Northeast Pacific can lead to the Alaskan Low
pressure cell moving to a lower latitude than normal, which then causes cold Arctic air
to pass over the Pacific Northwest and ultimately affects the eastern two-thirds of the
United States. This happened in each fall between 1962 and 1964, when a warm pool
of water existed in the central Pacific (Namias, 1966). The warm water pool
disappeared by the fall of 1965 and the lower latitude migration of the Alaskan Low
pressure cell disappeared.
A different effect occurs when the anticyclones in the Troposphere are
changed. Warm waters under the North Pacific high which generate strong diabatic
12
rise can create abnormally strong anticyclones which push the subtropical highs north
of their normal position. Wanner air is then found at higher latitudes. Namias (1969)
described four cases where abnormally strong anticyclones developed. In all four
circumstances, the unusually strong mid-tropospheric phenomena off California
created heavy precipitation in the area. The shift of the North Pacific High pressure
also cell affected the location of upwelling centers, drawing them further north when
the pressure cell was north.
Changes in SST are also important to generating and strengthening storms.
Between September 1972 and August 1973, there were heavy rains in California as a
result of migrating atmospheric pressure cells (Namias, 1974). In this circumstance,
an atmospheric trough associated with underlying SST contrasts developed, providing
a baroclinic source of energy to the atmosphere. Namias suggests that around the
North Pacific Gyre a zone of SST contrast advected far enough to account for the
development of the trough. Anomalous oceanic warmth was enhanced by the
increased atmospheric activity. The two processes, SST and atmospheric circulation,
both drive and respond to the other's actions. In light of this interrelationship,
variable SST in large regions could be the key to whether the Aleutian Low or the
North Pacific High pressure cells will dominate weather (Namias, 1969).
13
70.
I.r,fr4,rl
--
To document changes in
sea surface conditions of the
northeast Pacific Ocean during
the past 20,000 years we have
used radiolarian microfossils to
reconstruct past sea surface
PAR87a-OI and 1O
SC.
t0.
I IJy-rIz.
B
TF39-PC174
c
temperatures using the approach
of Imbrie and Kipp (1971) and
W8709a-PC13
W87O9a-TC,PC8
L13-81-G138, V1-8O-P3.
F8-90-G21 and G25-.-
other
late
Pleistocene
paleoceanographic
F2-92-P3---
studies
V1-81-G15-
(Moore, 1973, 1978; Pisias,
30.
1978).
20.
Radiolaria are diverse
and have a wide geographic
-
10.
range.
They are found in all
major oceans (Anderson, 1983),
0.
which make them well suited for
19
paleoceanographic studies.
Figure 6. Location of marine sediment
cores and continental data sites used
in this study.
Marine cores are
labeled; A Hoh Bog, Washington;
B = Marion Lake, British Columbia;
C = Dome Peak and Glacier Peak,
Washington.
Unlike calcareous species,
siliceous radiolaria
are
moderately well preserved in
north Pacific sediments and are
therefore ideal for study of this
14
region. Stratigraphic control for these sediments is provided by both conventional
14C and accelerator mass spectrometer (AMS) 14C dates.
We studied twelve marine sediment cores from the northeast Pacific and
compared our data to previously published continental records: two pollen records
and glacial records from the Pacific Northwest (Figure 6). The twelve cores were
selected based on the availability of radiocarbon dates and span the major
oceanographic regions of the northeast Pacific. The cores range in latitude from 33.6°
N to 54.41° N and, except for two cores in the Alaskan Gyre, follow a transect
parallel to the coast of North America (Figure 6; Table 1) and are from the shelf
environment. A total of 232 sediment samples were taken at approximately 10 cm
intervals in each core. Samples were chemically treated with hydrogen peroxide to
remove organic material and hydrogen chloride to remove carbonates, then sieved
Table 1.
Location of marine cores used in this study. Listed for
each core are its name, latitude and longitude, water depth
and distance offshore. Distance offshore was measured
perpendicular to closest coasthne.
Core
V1-81-G15
F2-92-P3
F8-90-G21
F8-90-G25
V1-80-P3
L13-81-G138
W8709a-PC13
W8709a-PC,TC8
TT39-PC17
rr39-PC12
PAR87a-01
PAR87a-01
Latitude/Longitude
Water Depth,
meters
33.60° N, 120.42° W
35.62° N, 121.60° W
37.22° N, 123.24° W
37.45° N, 123.45° W
38.43° N, 123.80° W
38.41° N, 123.97° W
42.12° N, 125.75° W
42.26° N, 127.68° W
48.23° N, 130.01° W
49.41° N, 128.19° W
54.36° N, 148.47° W
54.42° N, 149.44° W
1000
799
1605
1720
1600
2531
714
3137
2795
2369
3664
3480
Distance
Offshore,
km
160
60
80
80
30
30
120
270
250
400
520
480
15
with a 63 p.m sieve to remove silt, fragments and smaller unidentifiable specimens.
The greater than 63 p.m fraction was then prepared following the technique of Roelofs
and Pisias (1986) to obtain radiolaria slides: after rinsing and the chemical treatment,
the samples were allowed to settle for 24 hours in a beaker of water onto coverslips.
These coverslips were then secured to glass slides and cured
for permanency.
Forty-one species, listed in Table 2, were identified following the taxonomy of
Nigrini and Moore (1979). For each sample, a total count of 500 specimens was
preferred but a minimum of 100 radiolaria specimens was accepted as sufficient in
order to obtain a more complete geographic distribution. Four cores had a significant
number of samples containing less than 500: L13-81-G138, V1-80-P3, TT39PC17 and TT39-PC12. The first two cores are both near 38.4°N latitude, and the last
two are at 48.23° and 49.41°N latitude. This duplication of cores at same sites checks
for reproducibility of the record at the two sites which have low radiolaria counts.
The sediment off the coast of western North America contains a significant
fraction of fragmented radiolarians due to turbulence from rivers along the coast.
Thus, identified species account for only 30 to 60% of the total number of individuals
counted. Some species account for a large percentage of an individual sample (up to
70%). This is common in regions of high river input, where turbulence may break up
more fragile specimens, and in the colder latitudes, where there are fewer species
types present in the ocean.
Chronology
Stratigraphic control for this project was obtained by three techniques:
conventional 14C dating of bulk organic carbon, accelerator mass spectrometry
(AMS) dating of '4C on planktonic foraminifera and oxygen isotope stratigraphy
Table 2.
Radiolaria species used in factor analysis. Abbreviations are those used in
the O.S.U. radiolaria laboratory for counting purposes From Nigrini and
Moore, 1973.
S1
Si a
S7
S8
S10
S 12
Si 3
S14
S17
S18
S23
S24
S29
S30
S36a
S36c
S40
S43
S47
S48
S54
Ni
N2
N5
N7
N9
N14
N 15
N 18
N24
N25127
N29
N32
N33
N35
N35a
N38
N40
N42
N43
N46148
Spongurus sp.
Spongurus elliptica
Echinomma leptodermum
Prunopyle antarctica
Echinomma delicatum
Euchitonia elegans/E. furcata Ehrenberg
Polysolenia spinosa
Heliodiscus astericus
Hexacontium enthacanthum
Hymeniastrum euclidis
Didymocyrtis tetrathalamus
Lithelius minor
Larcopyle butschü
Stylochiamydium asteriscus
D. profunda
Euchitonia triangulum
Spongaster tetras
Spongopyle osculosa
Styloclictya validispina
Porodiscus sp.
Tetrapyle octacantha/Octopyle stenozoa
Liriospyris reticulata
Anthocyrtidium ophirense
Lamprocyrtis nigriniae
Pterocorys minithorax
Giraffospyris angulata
Tholospyris scaphipes
Lamprocyclas junonis
Botryostrobus auritus/australis
Pterocanium sp.
Pterocanium praetextumlP. praetextum eucolpum
Pterocorys hirundo
Phormostichoartus corbula
Botryostrobus aquilonaris
Theocalyptra davisiana
Theocalyptra davisiana cornutoides
Theocalyptra bicornis
Pterocorys zancleus
Theocoiytbium trachelium
Dendospyris borealis
Antarctissa denticulatalA. strelkovi
17
based on correlation to a 14C AMS dated core. Continental sites were dated using
conventional 14C dating of bulk organic carbon. Where possible in marine cores,
AMS dating on forarniniferal calcite was used. Because of the scarcity of foraminifera
in some deeper cores, 14C dates on bulk organic carbon were used. Seven cores in
the transect (V1-81-G15, F2-92-P3, F8-90-G21, F8-90-G25, W8709a-PC,TC8,
W8709a-PC13, PAR87a-10) have been dated using AMS dating on foraminifera; the
United States Geological Survey provided planktonic AMS dates for the southern
cores and dates for PAR87a-1O are from Zahn et a! (1992). Zahn et al (1992), also
report dates for neighboring core PAR87a-01, using AMS dates on PAR87a-10 and
correlating its oxygen isotope record to that of PAR87a-0l. The remaining cores
(L13-81-G138, Vl-80-P3, TT39-PC12 and TT39-PC17) were dated using bulk
organic carbon methods.
All 14C dates, including continental dates, were corrected to calendar ages as
follows:
1. Raw 14C AMS dates from marine samples were first corrected for ocean
carbon reservoir changes. Dates younger than 5000 years had 317 years subtracted
from the raw AMS date (Stuiver and Braziunas, 1993); dates equal to or older than
5000 years had 717 years subtracted from the raw AMS date (Bard, 1992). The
difference in corrections for the different ages reflect the use of different calibration
methods available for the age ranges.
2. No reservoir correction was made to the 14C dates from bulk organic
carbon.
3. All dates younger than 5000 yr were corrected to calendar age by applying
an equation from Stuiver and Braziunas (1993):
Calendar 14C age = (1.14*(conv. '4C age))-592;
II
with cony. 14C age meaning a reservoir correction has been applied, but not a
calendar correction.
4. All dates older than 5000 yr were then corrected to calendar age by
applying an equation from E. Bard (1992):
Calendar 14C age =
-5.85 x 106(conv. 14C age)2 + l.39(conv. 14C age) - 1087;
again, cony. '4C age means a reservoir correction has been applied, but not a
calendar correction. A summary of these radiometric ages is given in Appendix A.
Each core is listed with the depths at which the dating occurred, the raw date,
reservoir corrected dates (if applicable), and the final calendar corrected age.
Continental data also list the source of the dates.
Plots of depths vs. calendar age for each core are given in Figure 7. Cores
L13-81-G138 and V1-80-P3 are similar in location and show similar sedimentation
rates. This is also true for F8-90-G21 and F8-90-G25. While cores W8709aPC,TC8 and W8709a-PC13 are at the same latitude, they are separated by about 1.93'
of longitude. W8709a-PC13 is nearer to the coast; as a result, it has a higher
sedimentation rate. Ages of individual sediment samples were determined using a
linear interpolation between given dates for each core.
Paleotemperature Equation
Sea surface temperature estimates were made using the transfer function
technique of Imbrie and Kipp (1971). Q mode factor analysis simplified a radiolarian
19
Figure 7. Sedimentation rates of the marine cores used in this
study. Chronology is based on 14C AMS dates from
planktonic foraminifera for cores PAR87a-1O, W8709aPC,TC8, W8709a-PC13, F8-90-G25, F8-90-G21, F2-92P3 and V181-G15; based on bulk organic carbon for cores
TT39-PC12, TT39-PC17, V1-80-P3 and L13-8 1-G138.
Chronology for core PAR87a-01 is based on correlating its
oxygen isotope record to that of PAR87a-1O
20
Calendar Corrected Age,
kyr
5
10
20
15
Calendar Corrected Age,
kyr
25
0
50
0
60
50
70
80
90
200
250
100
1 ifi
fln
W8709A-PC,TC8
PAR87a-01
0
10
20
30
40
5
10
11
100
75 -
100
200
100 -
150
300
125 -
200
400
150-
250
cnn
0
C.)
3(
0
50-
5
10
15 20 25
0
oI.
50
100
10
5
'
12
'
14
16
'
I
18
175 -
W8709A-PCI3
0
.
15 20 25
10
F8-90-G25
0
PAR87a-1O
E
10 10.5 11 11.5 12 12.5
0
150
150
kyr
10 15 20 25 30
5
100
100
Calendar Corrected Age,
F8-90-G21
7.5 10 12.5 15 17.5 20
15
50
I
100
50
150
150
200
250
200
100
250
300
fin
T39PC12
10
15
20
0
F2-92-P3
v1-80-P3
25
30
0
10
20
30
40
0
10 20 30 40 50
0
100
1001
100
200
300
400
500
600
150200
200 -
300
250300-
400
TF39-PCI 7
L13-81-G138
Figure 7.
V1-8 1-G15
21
data set of 170 surface sediment samples from the Pacific Basin. A temperature
equation was calibrated by regressing annual mean SST (from atlas values in Levitus,
1977) against these factors. The factor analysis used a logarithmic transform of
species and described the 41 species used in this study as 7 factors. The factors
provide orthogonal assemblages and eliminate ecological redundancy within the
original data set (Imbrie and Kipp, 1971).
The factor analysis describes the original data in terms of two matrices,
referred to as the factor loading matrix and the factor score matrix. The factor loading
matrix shows the relative contribution of each factor in describing the surface
sediment radiolarian assemblage. A factor loading is the square root of the fraction of
information in a sample described by the specific factor. For example, a factor loading
of 0.5 for a specific sample indicates that the factor describes 25% of the information
in that sample. Summing the squared factor loadings from each sample gives the
communality, the total variance described by the factor in that sample. A communality
of 1.0 indicates that the factors describe 100% of the sample.
The factor score matrix shows the contribution of each variable to each factor.
Since the sum of squares of all scores in a factor add to one, the magnitude of
individual factor scores depends on the number of species used.
The relationship between the data matrix and the matrix from the factor
analysis is given by
U=B*F
where U = the row normalized data matrix, B = the factor loading matrix, and F =
the factor score matrix. Because the factor score matrix, F, is orthonormal, the
equation can be rewritten as:
U *1E't
This states that our row normalized data matrix, U, multiplied by the transpose of the
factor score matrix, Ft is equivalent to the factor loading matrix, B. Thus if we let U'
equal the data matrix (normalized) made up of all our down core samples, then
u?
* Ft = B?
gives the factor loading matrix for all down core samples. It is this factor loading
matrix, B', which is used in the down core analysis.
The paleotemperature transfer function was estimated by a non-linear
regression of the modern radiolaria factors against mean annual sea surface
temperature (Pisias et al, in prep). This produced an equation relating SST to
radiolarian assemblages (Table 3), which was then used to generate mean annual SST
estimates for the down core data. A map of the residuals (observed temperatures
estimated temperatures) (Figure 8) for the study area shows that residuals are <±10
C. The standard error of the equation is ±1.5°C. An independent study of past sea
surface temperatures, based on alkenones from coccoliths at W8709a-PC,TC8 (Prahl
et al, in prep) has been compared to the results from the radiolarian equation. The
two methods agree (Figure 9). This result suggests that the radiolaria based SST
equation provides reasonable estimates of past sea surface conditions.
23
Table 3. Regression Equation used on radiolaria factors to obtain estimated
mean annual sea surface temperature. From Pisias et al, in prep.
Key:
tro = Subtropicql factor
tm
Transitional factor
ant = Antarctic factor
ebc = Eastern Boundary
Current factor
art = Arctic factor
mix = Mixed factor
wpac = West Pacific factor
Mean Annual SST =
9.84003 + 19.38575(tro)
- lO.79275(ant)2
+ 13.88543(tro*art)
- 14.90222(trn*art)
- 9.86078(tro*trn)
+ 22.08979(ebc)2
5.54596(ebc)
+ 14.99509(ant*art)
- 18.08390(tro*mix)
+ l0.11748(mix)
+17.59832(mix*wpac)
l2.62261(art*mix);
S.E. = ±1.5°C
Figure 8. Map of residuals for the northeast Pacific from the sea
surface temperature equation. Contours are in °C.
Figure 9. Comparison of the radiolaria based temperature
equation to the alkenone based temperature equation
at site W8709a-PC,TC8
Temperature, °C
5
i.
-170,
I
.4b0.
I
-%.
5O.
1C'J'
-,
M\.'I
I
1.5
10
15
12.5
0I
5
o.
:-Z:YJi'I
/'\
.4// '\
.-Jso.
50.
1/ c1.
-..-....
ii
qo.
30.
bI(L)
20.
15
I .1
10.
0.
18
1/
,
I.
..n
4''
I
I i''I i'
_tn.
_,O.
D
.1!fl.
.120.
20
Radiolaria Equation SST Estimates
Alkenone Equation SST Estimates
Figure 8.
Figure 9.
Ui
26
RESULTS
Factor Analysis of Core Top Data
The factor analysis resulted in 7 factors, which account for 90% of the Pacific
Ocean core top sediment samples (Pisias et a!, in prep). Appendix B gives a
summary of the core top factor loadings. Communalities are very high; generally
.0.80, and range between 0.80 and 0.90 in the study area (Figure 10). Factors are
presented in order of importance to the Northeast Pacific.
Factor 1, which accounts for 63% of the variance in the surface sediment data
set, is dominated by the species group Tetrapvle octacantha/Octopvle stenozoa, with a
lesser contribution by Didymocyrtis tetrathalamus. Geographically this factor spans
Figure 10. Present day communalities of the
Pisias et al, in prep, factor analysis for
the northeast Pacific.,
27
the Pacific Ocean. Its highest factor loadings form a broad band at the equator;
between 30°N and 30°S latitude. Here, its factor loading is>0.70, equivalent to
explaining >49% of the tropical samples (Figure 1 la) and is therefore referred to as
the Subtropical factor. In the study area, the Subtropical factor loadings are low; they
reach a maximum of 0.35 at the area's southern boundary (Figure 1 ib). The factor
is highly correlated to temperature changes. Factor loadings are lower closer to the
polar regions and in the cool upwelling region along North America.
Factor 2 accounts for 15% of the total variance.
Three species,
Stvlochlamydium asteriscus, Botrvostrobus aquilonaris and Echinomma delicatum,
make up most of the assemblage. This factor is most prevalent at temperate latitudes,
40°N and 40°S, on the eastern side of the Pacific Ocean Basin (Figure 12a) and is
referred to here as the Transitional factor. Loadings in the study area range from 0.7
to >0.9 (Figure 12b). This geographic distribution is consistent with the intersection
of the West Wind Drift with North America. This assemblage is the dominant factor
in the
Transition
Zone.
Factor 4 from Pisias et al (in prep) explains 3% of the surface calibrated data
and is largely comprised of equal amounts by Tetrapyle octacanthalOctopvle stenozoa,
Ptervcorvs minithorax, Pterocorvs zancleus, Lamprocvrtis nigriniae and Theocalvptra
davisiana davisiana. Its highest factor loadings occur at the eastern edge of the Pacific
Basin. Thus, we refer to factor 4 as the Eastern Boundary Current factor (Figure
13a). These regions correspond with centers of strong upwelling at 40°N, 20°N and
10°S latitude. In the Northeast Pacific, the Eastern Boundary Current factor's highest
loadings occur at the coastline between 30° and 45°N latitude (Figure 13b), which
coincides with upwelling in the California Current. Factor loadings decrease into the
North Pacific Gyre and above the West Wind Drift and is not found in the Alaska
Figure 11. Present day distribution of factor 1, the Subtropical
factor. Points indicate locations of core top samples used in
the factor analysis. a) Pacific Basin, b) northeast Pacific.
Figure Ii.
t')
30
Figure 12. Present day distribution of factor 2, the Transitional
factor. Points indicate locations of core top samples used in
the factor analysis. a) Pacific Basin, b) northeast Pacific.
r
1W
-155
-15(3
-145
5
S
(40
30
°
-o
I
-145
-50
I
._-_L_1_
-7_
tOO
120
140
160
.
.
100
, -.
1OO
.
-140
°!5O
/N_ -5
,(2'.
-120
-10)
-40
Figure 12.
-140
-135
-130
-125
-1211
-115
11U
32
Figure 13. Present day distribution of factor 4, the Eastern
Boundary Current factor. Points indicate locations of core
top samples used in the factor analysis. a) Pacific Basin, b)
northeast Pacific.
FI
A.
'(1(1
-(0)
70
-155
-150
-(40
-(45
-830
-135
-125
-120
-115
-11k
.,I'
0
Ill JY
55
6G
r
1. III
-0.1o,
,///
J3r2/J
5O"._
50
.
/
"5
4
208'
I
-160
'
uI.(
1p
.
0
I
100
120
140
860
180
-140
-12(1
-1(2)
Figure 13.
(5
-150
145
-140
(35
-130
125
120
6
34
Gyre. The Eastern Boundary Current factor is a good indicator of the focus of
upwelling.
Factor 5 accounts for 3% of the variance in the surface sediment data set.
Dendospyris borealis, Theocalvptra davisiana davisiana and T. davisiana cornutoides
account for most of the factor. The factor has its highest factor loadings in the Sea of
Okhotsk and Bering Sea, where values reach up to 0.85 (Figure 14a). We refer to
factor 5 as the Arctic factor. In the Northeast Pacific its loadings are lower, between
0.3 and 0.5 in the Gulf of Alaska (Figure 14b). The factor is absent in the south of
and is indicative of high latitude and colder temperatures. The Arctic factor defines the
Subarctic Front by its southernmost extent and is the dominant factor in the Alaskan
Gyre and Alaskan Stream.
Factors 3, 6 and 7 from Pisias et al (in prep) are not important to the study
area. They are included because they were used in developing the Pacific wide
paleotemperature equation. The third factor explains 4% of the data and has its
highest factor loading is in the Antarctic Ocean and it is highly dominated by
Antarctissa denticulatalA. strelkovi, with a minor contribution by Tholospyris
scaphipes study area, Factor 6 explains 1% of the data and is dominated by the
species Lithelius minor, with minor contributions by Theocorvthium trachelium
trachelium and Spongopyle osculosa. This factor does not have one region of high
factor loading which can be correlated to a physical parameter or geographic location.
Factor 7, which contributes to 1% of the data set, has its highest loadings in
the western Pacific. Four species dominate the factor: Stylochlamydium astericus,
Theocalyptra davisiana davisiana, Pterocanium praetextum eucolpum and
Dendospyris borealis.
35
Figure 14. Present day distribution of factor 5, the Arctic factor.
Points indicate locations of core top samples used in the
factor analysis. a) Pacific Basin, b) northeast Pacific.
-155
-150
-145
-141)
-ISO
-135
-125
-110
,,.......,..
.-.
1b
0
t1K'\ !/
55P\
V
'T97'.)
.'.-.
,%
40
_.S
\
-.
\.
S -...
.
i.
-16O
120
140
160
-140
-120
-lOG
-OG
Figure 14.
-135
\
40
/
\
\
/
\
I
35
I
\
,i.i,,L.i.t,.
-ISO
-145
-140
-135
i3
-l5
30
-120
-115
-110
37
Present day mean annual sea surface temperatures for the northeast Pacific
Ocean are shown in figure 15 (from Levitus, 1977). The temperatures range from
8°C along the Alaskan coast and show an even warming to the southeast, with sea
surface temperatures at the Santa Barbara Basin of 15°C.
Down Core Analysis
To assess general faunal and SST changes for the past 20 kyr, we have
contoured the values of the variables (either factor loadings or SST) on an age vs.
latitude graph, adding values from the modem day ocean to represent 0 kyr. Grid
latitude, and the data was hand contoured. We have
box resolution is 1 kyr by
presented the time series of variables vs age. Communalities of the down core factor
6.160
150
140
130
120
115,.
Figure 15. Present day mean annual sea surface
temperature from the northeast Pacific
Ocean. Temperatures are from Levitus, 1977.
analysis are shown in Figure 16. Communalities are high, with the exceptions of
cores TT39-PC12 and TT39-PC17 (49.41°N and 48.23°N) and time period 20 ka to
17 ka. Distributions of factor loadings from 20 ka to the present are shown in Figures
17 to 20; pseudofactor matrices are in Appendix C. Mean annual sea surface
temperatures are shown in Figure 21. The most significant change over the past
20,000 years is the northward migration of radiolarian assemblages. All factors show
little change across the southern portion of the transect.
Factor Analysis of Down Core Data
Between 20 and 8 ka, the Subtropical factor was restricted largely to the
southern region of the study area (Figure 17). A regional trend in the Subtropical
factor is a northward expansion beginning at 8 ka, continuing to the present (Figure
17a). South of 36°N, a small northward expansion of the factor began at 15 ka. At
approximately 10 ka, the factor achieved its highest factor loadings for the Holocene
and latest Pleistocene between 33°N and 36°N latitude (Figures 17b,c). The
Subtropical factor retreated south until 8.5 ka, when it began expanding northward
again. No down core data exists between 3 and 0 ka, but modern values suggest the
factor maintained its position after a small northward migration. Between 36°N and
(Figures 17d - 17i) factor loadings remained relatively constant from 20 to 4 ka.
In the interval, factor loadings fluctuations as large as 0.15 are seen, but not in
any discernible pattern. North of 45°N, little variation in the Subtropical factor
occurred. A small decrease of the factor began at 8 ka to factor loadings near 0
between 6 and 4 ka at 49°N (Figure 17k), after which the factor loadings increased
slightly; but again, the changes were on the order of 0.15. At the northernmost sites
39
PAR87a-01.
PAR87a-1O
rr39-PCI2
Tr39-PC17
z
0
W8709a-PC.TCS
W8709a-I3PC
-J
V1-80-P3
L13-81-0138
F8-90-G25.
F8-90-G21
F2-92-P3
VI-18-G15
0.0
5.0
10.0
15.0
20.0
Age, kyr
I
0.50
0.60
0.70
communality
0.80
Figure 16. Communality of the radiolaria factors, 20 ka to present.
Pluses indicate location of radiolaria samples.
(54°N, Figures 1 71,m) the Subtropical factor increased slightly in factor loadings
from 20 ka to the present.
In general, the Transitional factor changed little south of 40° N latitude (Figure
18). There was a minor increase in factor loadings from the last glacial maximum to
present, with the time series showing localized fluctuations (Figures 18b - 18g).
North of 40° N, the Transitional factor loadings were greatly reduced between 20 and
15 ka (Figure 18a). Northward migration of the factor began at 16 ka, reaching high
factor loadings at 14 ka at cores W8709a-PC,TC8 (42°N), TT39-PC12 (49°N),
PARS7a-01.
PAR87a-1O
rr39-PC12
rr39-PC17
rj
0
W8709a-PC.TC8
W8709a-13PC
V1-80-P3
L13-81-G138
F8-90-G25,
F-9O-G21
F2-92-P3
V 1-18-C 15
0.0
5.0
15.0
10.0
20.0
Age, kyr
'
I
0.10
I
I
0.20
0.30
factor loading
I
I
0.40
Figure 17a. Distribution of the Subtropical factor, 20 ka to present,
an interpolated graph of latitude vs. age. Pluses indicate
locations of radiolaria samples
41
17m. Time series of the Subtropical factor at each
core site. Arrows indicate modern day values. b) Vl-81-
Figure 17b
G15, c) F2-92-P3, d) F8-90-G21, e) F8-90-G25, t) L13-81g138, g) V1-80-P3, h)W8709a-PC13, i) W8709a-PC,TC8,
j) rF39-PC17, k) Tr39-PC12, 1) PAR87a-1O, m) PAR87a01.
c. F2-92-P3
b. V1-81-G15
-0.1
0
0.1
0.2
0.3
0.4
-0.1
0.5
0
0.1
0.2
e. F8-90-G25
d. F8-90-G21
35.62°N
33.6°N
37.45°N
37.22°N
0.3
0.4
-0.1
0.5
0
0.1
0.2
0.3
0.4
0
0.5
5
5
10
10
1'
15
15
1
LU
Figures 17b
17e.
0.1
0.2
0.3
0.4
0.5
L13-81-G138
38.41°N
Al
A
Al
A'I
V1-80-P3
W8709a-PCI3
W8709a-PC,TC8
42.12°N
42.26°N
38.43°N
A') AA A
Al
(1
Al A'
A'2 AA A
fl1
(1
-'I
Al
A')
A'
(1,1
Ac
(1I
U
U
U
5
5
5
5
10
.w
10
10
15
15
15
15
21
20
20
20
Figures 17f- 17i
C)
Al
(1')
(1'
(1st
(1
-0.1
I
01
0
I
0,1
0.3
0.4
I
I
I
-0.1
0.5
0
I
0.1
t
54.42N
54.36°N
49.41°N
0.2
I
m. PAR87a-0l
1. PAR87a-10
k. TT39-PC12
j. TT39-PC17
48.23°N
0.2
0.3
0.4
I
I
I
-0.1
0.5
0
0.1
I
I
0.2
I
0.3
I
0.4
I
-0.1
0.5
101
I
I
0
0
5
5
5-
5
10
10
10-
10
15
15
15
15
A
4..
cI
20
20
20
Figure 17j - 17m.
0
I
0,1
I
4
0.2
0.3
0.4
I
I
I
0.5
PARS7a-01,
PAR87a-1O
'1T39-PC12
Tr39-PC17
4-i
W8709a-PC.TC8
W8709a-13PC
V1-80-P3.
L 13-8 1-0 138
P8-90-025.
F8-90-G21
F2-92-P3
V1-18-G15
0.0
5.0
10.0
15.0
Age, kyr
I
0.50
0.70
0.60
factor loading
0.80
Figure 1 8a. Distribution of the Transitional factor, 20 ka to
present, an interpolated graph of latitude vs. age. Pluses
indicate locations of radiolaria samples
20.0
Figure 1 8b - 1 8m. Time series of the Transitional factor at each
core site. Arrows indicate modem day values. b) V1-81G15, c) F2-92-P3, d) F8-90-G21, e) F8-90-G25, f) L1381-g138, g) V1-80-P3, h)W8709a-PC13, i) W8709aPC,TC8, j) TT39-PC17, k) TT39-PC12, 1) PAR87a-1O, m)
PAR87a-Ol.
0.3
0.4
0.5
0.6
0.7
0.8
0.3
0.9
0.4 0.5
0.6
37.45°N
37,22°N
35.62°N
33.6°N
F8-90-G25
d. F8-90-G21
c. F2-92-P3
b. Vl-81-G15
0.7
0.8
0.9
0.3
0.4
0.5
0.6
0.7
0.8
1)3
0.9
U.'
U.3
I
I
5
5
5
5
10
10
10
10
15
15
15
15
20
"I
Figures 1 8b
1 8e.
V.0
I
0.!
0.O
I
U,
9
W8709a-PC,TC8
W8709a-PC1
V1-80-P3
Li 3-81-G138
38.41°N
4226°N
42.12°N
38.43°N
03
0.3
0.4
0.5
0.6
0.7
0.8
0.9
0.3
0.4
0.5
0.6
0.7
0.8
0.9
0.3
0.4
0.5
0.6
0.7
0.8
0.9
U
0
5
5
5
10
10
10
15
15
15
III
10
15
20
Figures 18f
18i.
0.4
0.5
0.6
0.7
0.8
0.9
j. 1T39-PCI7
k. TT39-PCI2
49,41N
48.23°N
0.3
0
0.4 0.5 0.6 0.7 0.8
0.3
0.9
0.4 0.5 0.6 0.7 0.8
m. PAR87a-01
54.42°N
1. PAR87a-10
54.36°N
0.9
ç
0
ç
0
'
fl Q
fl
5
5
5
10
10
10
10
15
15
20
15
15
20
LU
Figures 18j
18m.
flit
fi
6
1
fi
'7
fiR
(1 Q
50
TT39-PC17 (48°N), PAR87a-10 (54°N) and PAR87a-01 (54°N) (Figures 18i 18m). A short term, southward retreat occurred at 13 ka (Figure 18a) and reduced
factor loadings occurred at two core sites; W8709a-PC13 (42°N, Figure 18h) and
TT39-PC12 (49°N, Figure 18k). In cores with data extending through the Holocene,
the Transitional factor loadings increased over the past 5 ka and has maintained its
position between 40°N and 50°N since 12 ka. It is currently the dominant factor in
the Northeast Pacific Ocean.
The Eastern Boundary Current factor changed significantly between 20 ka and
the present (Figure 19a). Southern cores show low values and little change between
20 and 15 ka (Figures 19b,c, 19f 19i). Factor loadings at this time were low along
the transect (Figure 19a). TT39-PC12 at 49°N (Figure 19k), has factor loadings
upwards of 0.3 around 16 ka, but the other northern cores have lower loadings. Core
TT39-PC17 has factor loadings of 0.0 between 20 and 15 ka, and cores
PAR87a-01 and PAR87a-10 have factor loadings <0.2 (Figures 19j,1,m). At 15 ka,
the Eastern Boundary Current factor appeared stronger at lower latitudes (south of
45°N) and factor loadings in the north dropped. A northward expansion of the factor
began at 15 ka with a second expansion at 13 ka. The Eastern Boundary Current
factor has been focused between
and 45°N for the past 13,000 years.
The Arctic factor has consistently been absent or of minimum importance at
sites south of 40°N (Figures 20a -20g) for the past 20 kyr, and has consistently been
high at the northern sites (Figure 20h - 20m). Between 20 and 15 ka, the Arctic
Factor had high factor loadings as far south as 40°N (Figures 20a, 20h 20j, 201 and
20m), except at core TT39-PC12 (Figure 20k). At 15 ka, the factor retreated north,
where its focus has remained for the rest of the Holocene. In the interpolated figure,
Figure 20a, increased factor loadings appeared south of 50°N at 13.5 ka and 5 ka and
in cores TT39-PC12 and PAR87a-10 (49°N and 54°N, Figure 20k,l).
51
PAR87a-Oi,
PAR87a-1O
TF39-PCI2
TF39-PC17
z
0
1)
-a
W8709a-PC,TC8
W8709a.I3PC
V1-80-P3.
L13-81-G138
F8-90-G25.
F8-90-021
F2-92-P3
VI-18-G15
0.0
5.0
10.0
15.0
Age, kyr
-0.20 -0.10 -0.00 0.10 0.20 0.30 0.40
factor loading
Figure 19a. Distribution of the Eastern Boundary Current factor,
20 ka to present, an interpolated graph of latitude vs. age.
Pluses indicate locations of radiolaria samples
20.0
52
Figure 19b 19m. Time series of the Eastern Boundary Current
factor at each core site. Arrows indicate modern day values.
b) V1-81-G15, c) F2-92-P3, d) F8-90-G21, e) F8-90-G25,
1) L13-81-g138, g) V1-80-P3, h)W8709a-PC13,
i) W8709a-PC,TC8, j) TT39-PC17, k) TT39-PC12,
1) PAR87a-1O, m) PAR87a-01.
b. V1-81-G15
-0.3
-0.1
0.1
-0.3
-0.1
0.1
37.45°N
37.22°N
35.62°N
0.3
e. F8-90-G25
d. F8-90-G21
c. F2-92-P3
33.6°N
0.3
-0.3
0.5
-0.1
0.1
3
0.3
0
0
0
5
5
5
10
15
15
10
E
-0.1
0.1
0.3
10
15
20
Figure 19b - 19e.
UI
U)
38.43°N
38.41°N
-0.3
0
15
-0.1
0.1
0.3
3
-0.1
0.1
0.3
i. W8709a-PC,TC8
42.26°N
h. W8709a-PC13
42.12°N
g. V1-80-P3
f. L13-81-G138
0.5
-0.3
0.7
-0.1
0.1
3
0.3
0
0
0
5
5
5
10
10
10
15
15
15
-0.1
0.1
0.3
20
Figure 19f- 19i.
Ui
j. TT39-PCL7
48.23°N
-0.3
-0.1
0.1
-0.3
0.3
k. TF39-PC12
1. PAR87a-10
49.41°N
54.36°N
-0.1
0.1
0.3
3
-0.1
0.1
m. PAR87a-01
54.42°N
0.3
3
0
0
0
5
5
5
5
10
10
10
10
15
15
15
15
20
Figures 19j
19m.
-0.1
0.1
0.3
56
0
4-a
.1C8
'C
38
Age, kyr
-0.100.00 0.10 0.20 0.30 0.40
factor loading
0.50 0.60
Figure 20a. Distribution of the Arctic factor, 20 ka to present, an
interpolated graph of latitude vs. age. Pluses indicate
locations of radiolaria samples
57
Figure 20b - 20m. Time series of the Arctic factor at each core site.
Arrows indicate modem day values. b) V1-81-G15, c) F292-P3, d) F8-90-G21, e) F8-90-G25, f) L13-81-g138, g)
V1-80P3, h)W8709a-PC13, i) W8709a-PC,TC8, j)
TT39-PC17, k)
TT39-PC12, 1) PAR87a-lO, m)
PAR87a-O 1.
c. F2-92-P3
b. V1-81-G15
-0.3
0-
-0.1
0.1
d. F8-90-G21
e. F8-90-G25
37.22°N
37.45°N
35.62°N
33.6°N
0.3
0.5
0.7
I
I
I
-0.3
II
-0.1
0.1
0.3
0.5
I
I
0.7
-0.3
-0.1
0.1
0.3
0.5
0.7
I
I
I
-0.3
o.
II
-0.1
0.1
I
Figures 20b - 20e.
0.3
0.5
0.7
I
I
I
f. L13-81-G138
-0.3
-0.1
0.1
0.3
I
I
0.7
-0.3
I
-0.1
0.1
0.3
0.5
0.7
I
I
I
-0.3
0
II
-0.1
5
10-
42.26°N
42.12°N
38.43°N
0.5
i. W8709a-PC,TC8
h. W8709a-PC13
g. V1-80-P3
38.41°N
10-
0.1
0.3
I
0.5
0.7
I
I
-03 -0.1
II
0.1
0.3
03
0.7
I
I
I
5.(
10-
Figures 20f 20i.
UI
j. TT39-PC17
48.23°N
-0.3
-0.1
0.1
0.3
3
0.5
k. rF39-PC12
1. PAR87a-10
49.41°N
54.36°N
-0.1
0.1
0.3
3
0.5
-0.1
0.1
0.3
m. PAR87a-01
54.42°N
0.5
3
0
0
0
5
5
5
10
10
10
10
15
15
15
15
0
20
ha-,
Figures 20j - 20m.
-0.1
0.1
0.3
0.5
[11
Sea Surface Temperature
The marine record illustrates the warming trend which has occurred since the
last glacial maximum (around 18 ka) (Figure 21a). The trend persists until the
present, with temperature increases on the order of 4° C. Superimposed on this
general trend are some coherent regional temperature variations. While these
variations are on the order of 2°C the fact that the pattern is seen in more than one
place along the transect suggests that these features reflect real changes. At sites
south of 37°N, there has been little temperature change. A maximum of 15°C
occurred between 11 and 9 ka (Figures 21b, c), with a temperature increase of 2.5° C
since 18 ka. Temperatures are then relatively consistent with a decrease to present
temperatures between 12° and 13°C.
The sites at latitudes between 37° and 45°N experienced three maxima: at 17,
11 and 4 ka, with average temperature increases of 1.5° C, 2.5° C and 2.5° C
(respectively) from their previous minima (Figures 21a, d, g-i). The 17 ka maximum
is present at two separate cores, V1-80-P3 (38°N, Figure 21g) and W8709a-13PC
(42°N, Figure 21h). It is followed by a slight minimum between 16 and 15 ka.
Temperatures increased to 11° C at the 11 ka maximum (Figures 21d,e,h,i) after
which they decreased slightly. The 4 ka maximum is seen in core, W8709a-PC,TC8
(Figure 21a, 21i), with a temperature of 12.5° C up from 10° C at 8 ka.
Temperatures reached 12° C at 4 ka at V1-80-P3 and L13-81-G138 (38°N, Figures
21f, g), which is potentially a third maximum, but no data points exist at this latitude
between 4 ka and the present to verify this.
At 49°N and 48°N (Figure 21a), warming occurred until 14.5 ka. A decrease
of temperature then occurred, reaching a minimum at 4.5 ka, followed by warming to
2.5 ka. After this age (2.5 ka), no data is available at this latitude. At 54°N (Figures
:
(
-
'
"
I
p4
=
?
)
" '
N
r
I
.
- -J
a
a
n
1
I..
*
a
0
.1
.1
.
- 0
0
0
63
Figures 21b 21m. Time series of sea surface temperature at each
core site.
Arrows indicate present day sea surface
temperatures from the Levitus Atlas (1977). b) V1-81-G15,
c) F2-92-P3, d) F8-90-G21, e) F8-90-G25, L13-81-g138,
g) V1-80-P3, h)W8709a-PC13, i) W8709a-PC,TC8, j)
TT39-PC17, k) TT39-PC12, 1) PAR87a-1O, m) PAR87a-01
10 12 14
8
16
I
I
10 12 14 16
I
I
e. F8-90-G25
1'7 Ac°M
37.22°N
35.62°N
33.6°N
8
d. F8-90-G21
c. F2-92-P3
b. V1-81-G15
10 12 14
8
16
I
4*1
F-ç1
5
5
5
10
10
5
F-kI
.10
H1
10
Fl__i
I I
IIH
15
15
F-J_1
15
I d'
15
LU
20
Figures 21b 21e.
f. L13-81-0138
8
38.43°N
10 12
14
16
i
8
10 12
i. W8709a-PC,TC8
h. W8709a-PC13
42.12°N
g. V1-80-P3
38.41N
14
16
5
8
10 12
14
A' ')OT..J
16
I
I
0
F-if-I
HI?H
H)1-1
5
5
5
10
7H
I10
10
*
FAI
H/H
FfI
E,41
i11i
15
15
15
F-/H
iy
(-1
H-I
i'h I
Figures 21f 21i.
UI
j. TT39-PCI7
k. 1T39-PC12
1. PAR87a-10
49.41°N
54.36°N
48.23°N
8
10 12 14 16
8
I
0
10 12 14 16 18
4
6
8
10 12
m. PAR87a-01
54.42°N
14 16
4
18
I
0
5
I-
10
5
:
10
F
I-
15
15
LU
L)
I-
Figures 21j
LU
21m.
6
8
10 12 14 16 18
67
211,m) temperatures generally increased from
C at 20 ka to 110 C at 8 ka, after
which the region cooled slightly. The thermal maximum at 14 ka and subsequent
minimum at 13 ka seen at 48°N is seen here as well in cores PAR87a-01 and
PAR87a-1O (54°N, Figure 211,m), though not as pronounced.
The time series from cores TT39-PC12 and TT39-PC17 (49°N and 48°N)
reveals minor maxima and minima smoothed out in Figure 21a. In Figures 21j and
21k, temperature reached a maximum of 110 C at TT39-PC12 and 12.5° C at TT39-
PC17 at 14.5 ka, followed by a minor depression of temperature at 13.5 ka. In core
TT39-PC12, temperature increased, peaking at 12.5 ka at 10° C. A minimum
occurred at 10.5 ka, followed immediately by a minor maximum at 9.5 ka. A
minimum of 8° C was reached at 7 ka and was followed by slight warming to 7 ka
(9.5° C). Temperature dropped to 7° C at 4 ka and then warmed to around 10° C.
DISCUSSION
Summary of Past Oceanographic Conditions
The northward retreat of the Arctic factor and expansion of the Subtropical
factor delineate a general warming trend over the past 20 kyr. The dominance of the
Arctic factor and absence of the Eastern Boundary Current factor during this time
period indicate that between 20 and 15 ka, Arctic conditions prevailed and upwelling
was at a minimum. These conditions are likely if the North Pacific High pressure cell
did not migrate as far north during summer months as it does today, allowing the
Alaskan Low pressure cell to dominate wind patterns in the northeast Pacific Ocean.
The West Wind Drift intersected the west coast of North America south of
N
latitude, resulting in a more southern position for the Transition Zone and therefore a
more southern origin for the California Current during the glacial-interglacial
transition at 20 to 15 ka.
The sudden appearance of the Eastern Boundary factor at 15 ka is evidence for
a change to conditions favorable to upwelling. One possible explanation is that the
North Pacific High pressure cell migrated northward, providing conditions not unlike
the California Current in spring and summer today. In response to this migration, the
Subarctic Front moved northward to its present day position. After the small thermal
maximum at the beginning of the Holocene (11 -9 ka), the Transition Zone migrated
to its present location, as did the West Wind Drift.
Superimposed on these general trends are short term changes in the radiolarian
fauna that are not necessarily reflected in the SST estimation. For example, no
Younger Dryas event occurred in the temperature record, but implications of it appear
in the factor analysis record. A "Younger Dryas event" refers to evidence found for a
sudden return to cold conditions in the North Atlantic ocean at 11 ka, (radiocarbon
years) (Broecker et al, 1990), which is equal to 13.4 ka in the chronology of this
study. The Transitional factor shows a decrease in factor loadings at 48°N, 49°N and
54°N (Figures 18a,j,k,), and the Arctic factor shows a significant increase in factor
loadings at this time (Figures 20a,j,k,1). A movement of the Alaskan Low pressure
cell to a lower latitude may have provided the right environment for the change in
radiolaria assemblages at the higher latitudes, but was not strong enough to affect
sites further south. The lack of an event in the SST record implies that the Younger
Dryas may not have been a global cooling event, but that some atmospheric change
affected the ocean environment in the Northeast Pacific Ocean.
Comparison to the Continental Record
Summer temperature and mean annual precipitation equations have been
developed based on Pacific Northwest pollen (Heusser et al, 1980), with standard
errors of 1.10 C and 620 mm/yr. respectively. These equations provide quantitative
records for direct comparison of temperature and precipitation records from
continental sites identified in Figure 6 to the SST record. At Hoh Bog, Washington,
a record extending back to 18 ka is available (Figure 22). A 16 ka record is available
from Marion Lake, B.C. (Figure 23). The continental sites are correlated to the
marine records at the present location of the West Wind Drift (TT39-pcl7, TT39pcl2), and are compared to these cores. The glacial history of the Pacific Northwest
(continental and alpine) is also compared to cores TT39-PC17 and TT39-PC12 and is
also shown on Figures 22 and 23. The pollen records and glacial records have been
published
0
B. Mean Annual
Precipitation, mm
A. Mean July
Temperature, °C
C. SST estimates, °C,
at TF39-PCI2,17
5 6 7 8 9 110111
4
I
I
I
21131t115
5
10
1
-
/
15
'p
1
aI
20
YF39-PC12
- - a -
TF39-PC17
glacial
EJ interglacial
Figure 22. a) and b): Hoh bog records from Heusser, Heusser and Streeter, 1980; a) mean
July temperature, °C and b) mean annual precipitation, mm/yr. c) Sea surface
temperature estimateds from cores TT39-PC 12, TT3 9-PC 17. d). Glaciation
record from the Pacific Northwest.
0
:
c
cJ
A. Mean July
Temperature, °C
12
13
14
15
16
B. Mean Annual
Precipitation, mm
17
P
U
1000
C. SST estimates, °C,
at TF39-PC12,17
2000
D.
5 6 7 8 9101112131415
3000
0
0
5
5.
5
10
10
10
15
15
15
0
4
I-
I- u-I
20
20
D..
20
...__,,. -.-, -
iL)'rUIz
- -- - - TT39-PC17
LU
glacial
EJ interglacial
Figure 23. a) and b): Marion Lake records from Mathewes and Heusser, 1981; a) mean
July temperature, °C and b) mean annual precipitation, mm/yr. c) Sea surface
temperature estimateds from cores TT39-PC 12, TT39-PC 17. d). Glaciation
record from the Pacific Northwest.
72
using bulk organic radiocarbon dates. The same age model applied to the marine
sediment cores has been applied to these published dates, the results of which are
listed in Appendix A.
The Fraser Glaciation was the driest cold interval experienced in the Pacific
Northwest during the last 25 ka, with a glacial advance around 20 ka and final retreat
of its last lobe, the Okanogan Lobe, beginning around 13 ka from the Columbia
Basin. In the Cascade Mountain Range, alpine glaciation reached its maximum at
22.8 ka (Booth, 1987). At 20 ka, the Cordillera Ice Sheet had two lobes split by the
Coastal Mountain Ranges in Washington; the Juan de Fuca Lobe covered the Olympic
Peninsula, Washington and Vancouver Island, British Columbia, and the Puget Lobe
covered the present day Puget Sound and Seattle. At 20.8 ka the Juan de Fuca Lobe
reached its maximum extent (Waitt and Thorson, 1983), while the Puget Lobe
reached its maximum extent at 18.4 ka (Booth, 1987). Relatively cool temperatures
occurred at sites TF39-PC12 and TT39-PC17 at 17 ka.
Cold and thy conditions on the continent coincided with the initial retreat of
the Cordillera Ice Sheet between 17.8 and 17.6 ka (Booth, 1987). Temperature then
increased to maxima at Marion Lake, Hoh Bog and core sites TT39-PC17 and
TT39-PC12 between 15 and 14.5 ka, and subsequently reached a minimum between
14 and 13 ka. This minimum coincided with a minor ice sheet advance between 14.7
and 13.9 ka (Booth, 1987), as well as an alpine glaciation between 14.7 and 13.4 ka.
This ice sheet advance occurred in the east Fraser Lowlands (north of the Puget
Lowlands), but is ambiguous elsewhere, suggesting it may have been a local glacial
response.
A temperature increase began at all three locations after 13 ka, along with a
precipitation decrease at Hoh Bog and Marion Lake. Temperature was at a maximum
between 12.5 and 11.5 ka at TT39-PC12 and Marion Lake, while the Hoh Bog site
73
recorded a maximum at 10.5 ka, 1 kyr later. Hoh Bog and the marine temperatures
reached minor minima shortly thereafter, and maxima at 10 to 9 ka. The Marion Lake
record shows no minimum at this time. By 10 ka, the Cordilleran Ice Sheet had
retreated well northward of the study area.
After the thermal maxima at 9.5 ka at Hoh Bog and Marion Lake, a
temperature decrease occurred which coincided with the SST decrease beginning at 8
ka. SST near 48°N reached a minimum around 4 ka, as did the Marion Lake site. A
similar temperature minimum at Hoh Bog occurred at 5 ka, preceding the other two
records by 1 kyr. Between 5.7 and 3.9 ka, both Dome Peak (Burke and Birkebind,
1983), and Glacier Peak, Washington (Davis, 1988) experienced glacial advances,
which also correlate to the SST minimum at 4 ka at core TT39-PC12. Thus these data
sets support our hypothesis that the ocean and continental climate record of the Pacific
Northwest are coupled.
74
CONCLUSIONS
Large scale warming and cooling occurred during the last deglaciation, with
the absolute SST maximum in the northeast Pacific Ocean occurring around 10 ka. A
general expansion of the Transition factor occurred at 16 ka and 13 ka, and of the
Eastern Boundary factor occurred at 13 ka, indicating an increase in upwelling at this
time. These migrations reflect the northward movement of the West Wind Drift's
intersection with the coast of North America over the past 20 ka as well as the
northward shift in position of the North Pacific High atmospheric pressure cell.
The Pacific Northwest continental record contains similar patterns and are
correlative to the SST data at 48°N. Two continental records (Hoh Bog and Marion
Lake) correlate directly to the SST data, with changes in temperature and precipitation
occurring simultaneously with the SST record. The glacial record from the Pacific
Northwest also correlates to the SST record at 48N. Altogether, the systematic
relationships of continental climate to sea surface temperature indicate that ocean
conditions and continental climate in the Pacific Northwest are related, and may be
linked to large scale atmospheric changes. Comparison of the temperature record at
48.23°N and 49.41°N (cores TT39-PC17 and TT39-PC12) to the continental
temperature records (Figure 24) demonstrate that the region where the West Wind
Drift intersected the North American continent and diverged in particular played a
significant part in continental temperature and precipitation records, reflecting the
importance of the westerly winds to continental climate change. Thus, we suggest
that the link between SST and continental response is through the position of the
North Pacific High Pressure cell, but what drives SST changes is still unknown.
75
A. Hoh Bog Temperature,
oc
10
12
11
13
B. Marion Lake Temperature,
15 13.5
14
oc
14
14.5
16
15.5
15
165
0
-
D
0
5-
____-
-
*
10.
D -------
*
:::
15
20-
1
6
7
8
9
1
10
-I
11
I
12
I
13
6
---.
- -.
8
I
I
I
9
10
11
12
13
Mean Annual SST,
oc
Mean Annual SST,
oc
HohBog
1T39-PC17
1T39-PCI2
I
7
-
..
-
MarionLake
TF39-PCI7
- - -. 1T39-PC12
.......
Figure 24. Comparison of the SST records at TT39-PC12 and
TT39-PC17 to continental temperature records at a)
Hoh Bog and b) Marion Lake.
76
BIBLIOGRAPHY
Anderson, O.R., 1983. Radiolaria. Springer-Verlag, New York, New York. 355p.
Bard, E., 1992, Kiel Conference personal communication via A. Mix, COAS,
Oregon State University, Corvallis, OR 9733 1-5503.
Barnosky, C. W., Anderson, P. M., Bartlein, P. J., 1987. The northwestern U.S.
during deglaciation; vegetational history and paleoclimatic implications, in
North America and Adjacent Oceans During the Last Deglaciation, W. F.
Ruddiman and H. E. Wright, eds. The Geological Society of America. p 289321.
Booth, D.R., 1987. timing and processes of deglaciation along the southern margin
of the Cordilleran ice sheet, in North America and Adjacent Oceans During the
Last Deglaciation, W. F. Ruddiman and H. E. Wright, eds. The Geological
Society of America. p. 71-90
Broecker, W.S., Andree, M., Woifli, W., Oeschger, H., Bonani, G., Kennett, J.
and D. Peteet. The chronology of the last deglaciation: implications to the
cause of the Younger Dryas Event. Paleoceanography. 3(1): 1-19
Burke, R.M. and P.W. Birkebind, 1983. Holocene glaciation in the mountain
ranges of the western United States, in Late-Quaternarv environments of the
United States, H.E. Wright, ed. University of Minnesota Press, Minneapolis,
MN. vol.1: 3-11
Davis, P.T., 1988. Holocene glacier fluctuations in the American cordillera.
Quaternary Science Reviews, 7: 129-157.
Freeland, H.J., Crawford, W.R., Thomson, R.E., 1984. Currents along the Pacific
coast of Canada. Atmosphere Ocean, 22(2): 15 1-172.
Heusser, C.J., Heusser, L.E., and Streeter, S.S., 1980. Quaternary temperatures
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APPENDICES
Ages for the data used in this study. For each core, depth, raw 4C age, reservoir
corrected 14C age if applicable, calendar corrected 14C age, and standard error
if available are listed. Table A. 1. Depths and dates of marine sediment cores.
Raw ages are from planktonic foraminifera using 14C AMS techniques, unless
otherwise noted. Table A.2. Dates of continental pollen sites. Raw ages are
from bulk organic carbon. Hoh Bog data is from Heusser, Heusser and
Streeter, 1980. Marion Lake data is from Mathewes and Heusser, 1981).
Table A.3. Dates of continental glacial events. Raw ages are from bulk organic
carbon. Also listed are the source of the raw ages.
Table A. 1.
Depth, cm
Depths and dates of cores. Raw ages are from planktonic forarninifera
using 14C AMS techniques, unless otherwise noted.
Standard
Raw l4C Age
Res. Corr. Age
8860
10960
16340
37100
41500
8143
10243
15623
36383
40783
41742
45871
100
90
110
999
999
8786
8826
9306
9906
11096
11436
12426
15936
8469
8509
8589
9189
10379
10719
11709
15219
9748
9799
10420
11192
12710
13140
14386
18712
90
90
100
100
110
140
110
220
Calendar
Correct Age
Error, ±
Vi -81 -Gi 5
60
80
120
220
260
9843
10243
19201
F2-92-P3
90
100
120
140
160
170
214
298
E31
Table A.1 Continued
F8-90-G2 1
62
75
83
155
60
9200
9800
10050
14280
8483
9083
9333
13563
10283
11056
11376
16689
9270
9730
10590
8553
9013
9873
10374
10966
12066
----
1929
13898
19908
24938
32574
620
440
2109
12304
13760
70
90
200
140
190
90
F8-90-G25
70
80
100
210
107
300
Li 3-81 -G 138
bulk organic 14C dates
8
88
154
254
398
2212
11320
16210
20490
27370
----
-------
----
80
120
150
Vi -80-P3
bulk organic 14C dates
8
74
138
2370
10060
11210
----------
Table A. 1 Continued
W8709a-PC 13
27.
127.
197.
222.
270.
302.
332.
392.
402.
7415
230
230
95
7000
9960
13430
14035
14550
16870
17650
19100
21955
6683
9243
12713
13318
13833
16153
16933
18383
21238
20773
22488
25795
270
610
245
2640
6140
11560
11000
15130
15040
17770
20200
20440
2640
6140
2056
6278
110
110
10843
11000
14413
14323
17053
19483
19723
13297
13495
17732
17622
20915
23774
24052
250
210
290
400
280
380
610
11261
15639
16387
17021
19839
140
220
135
W8709aPC,TC8
27.5
83.5
125.0
125.5
155.0
162.5
192.5
222.5
253.5
11I'39-PC 17
bulk organic 14C dates
0
120
360
520
10000
14000
-------
12228
17226
25523
28183
----
2851
15994
18447
21055
21000
24000
TT3 9-PC 12
bulk organic 14C dates
10
230
256
255
3020
13000
15000
17170
Table A. 1 Continued
PAR87a- 10
23
50
121
213
6640
12490
16670
31600
6323
11773
15953
30883
6940
14467
19599
36261
PAR87a-0 1
oxygen isotope correlation to PAR87a-10
1
7
12
17
21
27
32
36
41
47
52
56
61
67
71
77
81
86
92
96
101
106
111
117
122
5858
6713
7560
8415
9271
10032
10785
11281
11769
12265
12590
12889
13206
13522
13839
14155
14463
14780
15233
15686
16131
16585
17038
17491
17936
5541
6396
7243
8098
8554
9315
10068
10564
11052
11548
11873
12172
12489
12805
13122
13438
13746
14063
14516
14969
15414
15868
16321
16774
17219
5904
7037
8150
9266
10375
11353
12315
12944
13561
14185
14592
14965
15360
15752
16145
16535
16915
17304
17858
18409
18949
19497
20041
20583
21113
300
230
562
2000
Table A.2.
Dates of continental pollen sites. Raw ages are from bulk organic carbon.
Hoh Bog (Heusser, Heusser and Streeter, 1980)
Sample number
Raw 14C Age
95
155
195
255
1370
1960
2510
295
355
495
530
575
4150
6080
8660
13340
14950
15600
Calendar Corrected
Age
970
1642
2269
4139
7148
10512
16415
18386
19173
Marion Lake (Mathewes and Heusser, 1981)
Sample number
1
4
18
33
71
83
94
Raw 14C Age
Calendar Corrected
Age
520
890
2140
4035
8000
10090
12350
0.8
423
1848
4008
9659
12343
15187
Table A.3.
Dates of continental glacial events. Raw ages are from bulk organic
carbon.
Raw 14C Age
Calendar Corrected Age
Source of
Dates
4000
4700
4900
5000
3968
4766
4994
5716
11400
12000
14000
14500
15000
17000
18700
13999
14751
17226
17838
18447
20852
22860
Burke and Birkebind, 1983
Davis, 1988
Davis, 1988
Burke and Birkebind, 1983
Booth, 1987
Booth, 1987
Booth, 1987
Booth, 1987
Booth, 1987
Waitt and Thorson, 1983
Booth, 1987
APPENDIX B.
Table B.1.
A summary of factor loadings from core tops used in the Pisias et al
factor analysis.
Tro.
Tm.
Ant.
EBC
Art
Mix
WPac
= Subtropical factor
= Transitional factor
= Antarctic factor
= Eastern Boundary Current factor
= Arctic factor
= Mixed factor
= West Pacific factor
Core Name
Tro.
Tm.
Ant.
EBC
Art.
Mix.
Y69-71P
Y69-103P
Y69-104M
Y71-6-12
Y71-6-14
Y71-7-27
Y71-7-28
Y71-7-30
Y71-7-32
Y71-7-35
Y71-7-36
Y71-7-38
Y71-9-87
Y71-9-89
V15-33TW
V15-56TW
V17-58TW
V17-88TW
V21-029W
V24-040T
V24-046T
0.887
0.884
0.847
0.859
0.908
0.895
0.856
0.899
0.914
0.931
0.917
0.933
0.901
0.924
0.889
0.720
0.846
0.929
0.906
0.921
0.932
0.884
0.953
0.909
0.954
0.921
0.888
0.899
0.872
0.741
0.766
0.788
0.832
0.612
0.503
0.559
0.513
0.598
0.737
0.865
0.830
0.896
0.943
0.767
0.866
0.621
0.186
0.309
0.359
0.455
0.351
0.434
0.463
0.405
0.309
0.210
0.311
0.185
0.055
0.267
0.281
0.426
0.666
0.627
0.350
0.212
0.320
0.273
0.619
0.137
0.172
0.231
0.312
0.243
0.221
0.184
0.111
0.086
0.102
0.099
0.053
0.116
0.117
0.231
0.329
0.528
0.819
0.084
0.107
0.107
0.218
0.111
0.841
0.776
0.904
0.851
0.224
0.305
0.359
0.427
0.325
0.153
0.343
0.549
0.504
0.535
0.523
0.466
0.326
0.343
0.194
0.086
0.441
0.252
0.464
-0.079
0.256
0.125
0.157
0.172
0.209
0.413
0.113
0.185
0.005
-0.003
0.018
0.383
0.206
0.210
0.290
0.037 -0.206
0.020 -0.085
0.218 -0.179
0.216 0.176
0.283 0.103
0.185 0.220
0.105 0.014
0.036 -0.023
-0.007 -0.046
-0.043 0.010
-0.071 0.032
0.034 0.129
0.121 0.002
-0.027 0.061
0.208 0.074
-0.025 0.330
0.033 -0.073
0.064 0.056
-0.040 -0.030
-0.069 -0.060
-0.011 -0.093
0.108 0.049
-0.009 -0.039
0.123 0.108
0.037 -0.002
0.039 -0.052
0.011 -0.040
0.039 0.177
0.112 0.154
0.081 0.190
0.014 -0.046
RCO9-86
RC1O-69T
RC12-225
RC12-227
RC12-230
RC12-232
RC13-100
RC15-55T
RC15-61T
RC15-63T
0.3 14
0.335
0.907
0.870
0.881
0.513
0.913
0.183
0.294
0.111
0.180
0.618
0.126
0.161
0.291
0.28 1
0.326
0.508
0.290
0.358
0.537
0.803
0.684
0.626
WPac
Table B. 1 Continued
Core Name
Tro.
Tm.
Ant.
EBC
Art.
RC15-67T
RC15-73T
RCI7-213
E11-3TW
E17-3OTW
E25-7TW
E25-1OTW
TR1-9G0
R1S-36
UR-1-FFRC13-62T
RC12-65T
V18-333
0.954
0.864
0.948
0.956
0.831
0.912
0.933
0.882
0.842
0.922
0.920
0.929
0.821
0.888
0.913
0.896
0.900
0.889
0.160
0.073
0.252
0.045
0.279
0.191
0.415
0.403
0.129
0.351
0.533
0.229
0.377
0.043
0.112
0.153
0.161
0.160
0.179
0.084
0.910
0.891
0.833
0.882
0.850
0.849
0.715
0.088
0.157
0.074
0.084
0.072
0.103
0.120
0.110
0.072
0.049
0.193
0.119
0.147
0.173
0.079
0.091
0.220
0.052
0.095
0.107
0.107
0.061
0.088
0.066
0.080
0.090
0.092
0.072
0.092
0.138
0.103
0.018
0.097
0.094
0.126
0.097
0.054
0.124
0.062
0.088 0.091 0.060
-0.021 -0.014 0.046
0.105 -0.042 0.055
-0.003 0.074 0.093
0.123 0.268 -0.041
-0.067 -0.017 -0.048
-0.020 -0.037 0.108
0.145 -0.046 0.269
0.001 -0.005 0.290
0.048 0.005 -0.009
0.148 -0.027 -0.030
0.042 0.029 -0.054
0.428 0.158 0.096
0.085 -0.022 -0.038
0.336 0.047 -0.055
0.063 0.011 0.004
0.082 -0.011 -0.022
0.288 0.011 0.258
-0.03 1 -0.040 0.248
0.177 -0.017 0.437
0.322 0.130 -0.105
0.357 -0.019 0.120
-0.1190.107 0.098
0.054 0.005 -0.022
-0.023 0.058 -0.031
-0.154 0.039 0.151
0.095 0.036 -0.035
0.168 -0.035 -0.006
-0.092 0.115 0.097
0.187 -0.084 -0.107
0.093 -0.020 -0.050
V24-6OTW
RC1O-88T
V28-181T
V28-185T
TR1-1360
MFZ-4-00
FAN-HMSY69-71P
Y71-7-32
V24-112
RC1O-206
V24-104
V21-99
V24-054
V24-056
V24-078
V24-051
V21-203
V24-049
V24-052
V21-097
V21-126
V21-080
V18-328
V20-138
V19-109
V20-137
V21-083
V20-136
V18-324
V18-319
RC1O-167
RCI 1-209
0.9 13
0.902
0.883
0.832
0.884
0.911
0.890
0.911
0.939
0.915
0.868
0.929
0.944
0.923
0.942
0.932
0.902
0.954
0.855
0.943
0.890
0.939
0.929
0.948
0.869
0.935
0.911
0.926
-0.021
0.246
0.350
0.849
0.768
0.947
0.933
0.946
0.753
0.912
0.866
0.937
0.929
0.679
0.870
0.683
0.762
0.776
0.871
0.214
0.939
0.852
0.926
0.912
0.891
0.902
0.948
0.845
0.914
0.925
0.900
0.912
0.860
0.902
0.909
0.903
0.915
0.916
0.860
0.953
0.863
0.944
0.16 1
0.490
0.208
0.437
0.367
0.132
0.189
0.897
-0.025
0.157
0.202
0.143
0.135
0.187
0.166
0.165
0.206
0.157
0.088
0.252
0.158
0.244
0.005
0.289
0.232
0.262
0.148
0.088
0.327
0.084
0.3 11
0.186
-0.050
-0.038
0.116
0.234
0.000
-0.056
0.069
0.051
0.040
0.252
0.094
Mix.
WPac
0.010 -0.216
0.006 -0.078
-0.014 0.090
0.101 0.171
0.052 0.065
0.123 0.011
0.054 0.019
0.084 0.128
0.011 -0.005
-0.059 -0.101
-0.016 -0.101
0.098 -0.054
-0.001 0.041
0.03 1 -0.070 -0.090
0.094 0.003 0.030
Table B.1 Continued
Core Name
RC11-211
RC1O-160
V21-042
V2l-207
RC1O-094
V24-147
V24- 146
V24-150
V21-074
V20-095
V21-040
V20-057
zrrs
420
V24-095
V19-068
TR1 110
V21-036
MEN-4G
LFGS 50G
RC11-232
LFGS 48G
V19-039
Y70-5-67
Y70-5-64
V19-040
V21-073
RC11-208
V21-139
V21-075
V20-088
Y70-5-63
Y70-5-62
V24-143
V24-141
V24-139
V24-115
V24-117
TR1 8PG
RIS-5G
R15-127G
SCAN5PG
LPFE-68G
TRI-12G
Y70-2-34
Y70-4-56
RC1O-217
WPac
Tro.
Tm.
Ant.
EBC
Art.
Mix.
0.905
0.917
0.949
0.897
0.944
0.847
0.900
0.923
0.900
0.857
0.921
0.818
0.966
0.842
0.924
0.944
0.907
0.873
0.934
0.941
0.755
0.847
0.190
0.374
0.249
0.313
0.073
0.056
0.099
0.037
0.269
0.307
0.137
0.123
0.256
0.210
0.174
0.287
0.119
0.601
0.710
0.060
0.707
0.277
0.895
0.939
0.201
0.165
0.140
0.270
0.314
0.618
0.898
0.923
0.078
0.151
0.144
0.174
0.125
0.254
0.167
0.127
0.144
0.086
0.132
0.054
0.068
0.044
0.043
0.094
0.107
0.071
0.050
0.165
0.091
0.070
0.155
0.069
0.154
0.194
0.091
0.180
0.101
0.138
0.126
0.075
0.114
0.073
0.086
0.093
0.141
0.124
0.149
0.075
0.077
0.037
0.086
0.072
0.089
0.080
0.144
0.128
0.211
0.161
0.125
0.119
0.117
0.206
0.025
0.140
0.240
-0.030
-0.203
-0.065
-0.056
-0.017
0.043
0.102
0.003
-0.009 0.014
-0.022 -0.128
-0.004 0.001
-0.081 -0.174
0.93 1
0.906
0.919
0.922
0.783
0.877
0.895
0.861
0.912
0.890
0.934
0.931
0.915
0.897
0.912
0.935
0.862
0.927
0.939
0.905
0.870
0.863
0.906
0.941
0.905
0.840
0.926
0.908
0.912
0.864
0.867
0.879
0.861
0.916
0.890
0.928
0.903
0.947
0.88 1
0.793
0.912
0.454
0.533
0.931
0.507
0.835
0.231
0.169
0.868
0.912
0.951
0.900
0.858
0.579
0.199
0.173
0.918
0.868
0.949
0.891
0.936
0.752
0.876
0.753
0.484
0.282
0.627
0.035
0.154
0.126
0.35 1
0.677
0.789
0.412
0.789
0.826
0.907
0.028 0.001
0.123 -0.028
0.071 0.006
0.058 0.018
-0.05 1 0.023
-0.037 0.121
0.020 0.003
0.033 0.128
-0.011 -0.030 0.328
-0.072 -0.030 0.211
0.188 -0.067 0.088
0.076 -0.053 0.341
0.186 0.057 0.033
0.172 -0.054 0.509
0.3 11 -0.013 0.03 1
0.139
0.270
0.299
0.095
0.018
0.237
-0.061
0.061
0.041 0.141
0.032 -0.068
0.074 0.126
-0.161 -0.023
-0.084 -0.032
-0.006 0.070
-0.018 -0.002
-0.006 -0.036
-0.079 -0.057
-0.086 0.010
-0.189 0.271
-0.016 -0.08 1
-0.109 -0.122
0.057
-0.032
0.117
0.163
0.097
-0.092 0.065 0.126
-0.088 0.065 0.021
0.031 -0.023 -0.038
-0.082 0.009 0.196
-0.018 0.016 0.097
0.455 0.016 -0.020
0.056 -0.049 0.241
0.058 -0.070 0.379
0.369 0.018 -0.008
0.363 0.108 -0.033
0.016 -0.081 0.542
-0.0 83 0.471 0.184
-0.201 0.267 0.195
-0.118 0.227 0.106
Table B. 1 Continued
Core Name
MUK1-1-1
Y70-2-41
Y70-1-3P
TR1 14G
Y69-106MEN-5G
ZAP 2G
6910-2PG
V21-146
V21-148
V21-151
V21-145
V21-147
RC14-125
RC14-115
RC14-145
RC14-148
V20-128
V20-131
V20-136
V21-71
V21-75
V21-147
RC14-114
RC14-109
RC14-98
RC12-417
RC12-411
RC12-402
RC1O-184
RC1O-181
RC13-108
RC13-110
RC13-138
V20-75
Y70-4-51
V20-139
RC11-176
MEN-3G
Y70-1-1
6910-4
65-11-69
RC11-193
RC11-184
RC1O-230
DM-945
DM-946
Tro.
Tm.
0.956
0.944
0.902
0.889
0.906
0.904
0.912
0.937
0.906
0.814
0.825
0.898
0.927
0.760
0.949
0.857
0.845
0.930
0.927
0.910
0.915
0.918
0.932
0.959
0.919
0.906
0.924
0.959
0.919
0.956
0.951
0.888
0.903
0.926
0.863
0.847
0.902
0.908
0.917
0.894
0.868
0.858
0.905
0.867
0.889
0.785
0.772
0.110 0.843
0.058 0.830
0.338 0.839
0.702 0.5 19
0.885 0.238
0.436 0.745
0.792 0.144
0.336 0.785
0.712 0.568
0.496 0.682
0.079 0.734
0.804 0.446
0.669 0.630
0.052 0.549
0.043 0.810
0.007 0.585
0.040 0.656
0.660 0.640
0.759 0.562
0.839 0.404
0.816 0.393
0.840 0.423
0.608 0.686
0.079 0.713
0.129 0.804
0.716 0.517
0.582 0.7 18
0.707 0.617
0.523 0.701
0.078 0.8 17
0.295 0.887
0.846 0.289
0.842 0.342
0.847 0.301
0.056 0.907
0.103 0.857
0.883 0.321
0.113 0.873
0.364 0.712
0.350 0.808
0.307 0.762
0.133 0.762
0.527 0.661
0.205 0.847
0.306 0.789
-0.046 0.210
-0.047 0.219
Ant.
Mix.
EBC
Art.
WPac
0.153
0.113
0.135
0.164
0.081
0.200
0.069
0.168
0.163
0.202
0.220
0.154
0.167
0.070
0.152
0.100
0.087
0.135
0.138
0.128
0.142
0.155
0.150
0.144
0.118
0.172
0.140
0.158
0.162
0.139
0.172
0.169
0.103
0.161
0.144
0.114
0.107
0.175
0.261
0.154
0.143
0.191
0.192
0.237
0.170
0.032
0.049
-0.114 0.389 0.101
-0.093 0.469 -0.008
0.203 -0.153 -0.001
0.290 -0.020 0.117
0.165 -0.037 0.089
0.308 -0.015 0.086
0.479 0.095 -0.065
0.337 0.041 -0.129
0.145 -0.097 0.034
0.217 0.032 -0.055
-0.080 0.447 0.125
0.062 -0.1370.007
0.191 -0.042-0.113
0.050 0.63 1 -0.225
-0.102 0.475 0.148
0.005 0.706 -0.056
-0.0980.611 -0.062
0.205 -0.100 -0.119
0.112 0.006 0.000
0.062 -0.071 -0.097
-0.045 -0.032 0.164
0.026 -0.065 0.054
0.207 -0.097 -0.125
-0.026 0.649 0.007
-0.104 0.473 -0.094
0.227 0.098 -0.050
0.174 -0.129 0.002
0.203 -0.012 -0.094
0.228 0.207 -0.135
-0.137 0.467 0.097
0.070 0.075 -0.195
0.235 0.030 0.009
0.237 -0.004 -0.064
0.280 0.021 -0.088
0.088 -0.075 0.026
-0.175 0.188 -0.028
-0.008 0.032 0.044
-0.1570.244 0.077
0.252 -0.008 0.383
0.266 -0.118 -0.081
0.329 0.022 0.244
0.373 0.177 -0.077
0.101 -0.065 0.374
-0.055 0.049 0.162
0.236 -0.012 0.295
0.173 0.839 0.009
0.177 0.827 0.019
APPENDIX C
Table C. 1. Pseudofactor matrices of the twelve marine cores used in this study.,
Comm.= Communality
Tro. = Subtropical factor
Tm. = Transitional factor
Ant. = Antarctic factor
Depth
Comm.
Vi -81-015
3
0.8726
10 0.8697
20 0.8811
30 0,8920
40 0.9057
50 0.7287
60 0.8518
10 0.8417
80 0.8846
90 0.7933
100 0.7680
110 0.4942
120 0.5919
130 0.6181
F2-92-P3
2 0.7925
10 0.8204
20 0.7409
30 0.7136
40 0.7494
50 0.6351
60 0.6933
70 0.7213
80
90
100
110
0.7661
0.6829
0.7030
0.6804
EBC = Eastern Boundary Current factor
= Arctic factor
= Mixed factor
Wpac = West Pacific factor
Art.
Mix.
Ant.
EBC
0.2682
0.3235
0.3236
0.2568
0.3850
0.4131
0.3603
0.2628
0.3073
0.1831
0.2714
0.1996
0.7988
0.8000
0.8069
0,7867
0.8120
0.7051
0.7246
0.6633
0.7600
0.7418
0.7340
0.5580
0.6355
0.6957
0.2074
0.2463
0.2453
0.2029
0.1956
0.1928
0.1760
0.1914
0.2077
0.2011
0.2506
0.3241
0,3198
0.2574
0.2902 -0.0046 0.1355 -0.0039
0.3234 0.0461 0.0281 0.0420
0.3002 0.0386 0.0707 0.0363
0.3351 -0.0412 0.1076 0.0409
0.2597 -0.1361 0.1234 "0.0457
0.3311 -0.0721 0.1143 0.0216
0.3588 0.0271 0.1286 0.0393
0.2811 -0.0857 0.3119 -0.0857
0.2063 -0.0777 0.2843 -0.0677
0.0889 -0.0445 0.3515 0.0094
0.0910 0.0089 0.2433 0.0669
-0.0125 -0.0169 0.2075 -0.0275
0.0029 -0.0043 0.1102 0.0041
-0.0754 0.0256 0,1460 0.0184
0.1986
0.2015
0.3169
0.3911
0.3826
0.2100
0.3876
0.3409
0.2894
0.2579
0.3068
0.3171
0.8040
0.8100
0.7510
0.6944
0.7341
0.7223
0.6897
0.7353
0.7571
0.6995
0.6689
0.6417
0.2206
0.1868
0.1756
0.1265
0.1652
0.1886
0.1713
0.1692
0.2528
0.2001
0.1950
0.2221
0.2283
0.2408
0.1294
0.1673
0.1387
0.0078
0.1394
0.1595
0.1578
0,2719
0.3386
-0.0156
-0.0006
-0.0784
-0.1010
-0.0342
-0.0576
-0.0581
-0.0671
-0.0910
-0.0629
-0.0796
0.3241
-0,1126
Tro.
0.2981
0.2443
Tm.
Art.
Mix.
0.0351
0.1753
0.1476
0.1544
0.1248
0.1740
0.1170
0.0490
0.1100
0.0580
0.0469
WPac.
0.0667
0.0141
0.0303
-0.0194
0.0300
0.0073
.0.0387
0.0582
0.0016
-0.0493
-0.0173
-0.0058 0.0318
Depth
Comm.
Tm.
Tm.
Ant.
120
130
140
148
160
170
180
190
0.6705
0.6903
0.6893
0.7365
0.6747
0.6854
0.5994
0.4766
0.4980
0.4954
0.6180
0.6719
0.5198
0.6303
0.5905
0.7315
0.5388
0.5745
0.6198
0.5916
0.4810
0.2560
0.3286
0.2908
0.2316
0.1340
0,1934
0.1713
0.1655
0.2062
0.2568
0.1300
0.1012
0.1608
0.1028
0.0897
0.1987
0.2074
0.1135
0.0272
0.0961
0.0121
0.7011
0.6542
0.6703
0.7591
0.6965
0.6898
0.6233
0.4531
0.5437
0.5500
0.7148
0.7740
0.6691
0.7403
0.7170
0,7645
0.6491
0.6949
0.6051
0.6611
0.4969
0.1649
0.2449
200
210
220
230
240
250
260
270
290
298
310
320
330
o
10
20
30
40
50
60
70
0.6362 0.1160 0.6832
0.7003 0.1108 0.7501
0.6847 0.0614 0.7329
0.7206 0.1576 0.7315
0.7125 0.1449 0.7466
0.6508 0.0525 0.7485
0.6629 0.1649 07133
0.6637 0.2416 0.6697
0.27.58
0.1963
0.2093
0.2608
0.2717
0.2642
0.3184
0.2460
0.2091
0.1714
0.1988
0.2385
0.2218
0,2365
0.2316
0.2231
0.1860
0.2201
0.1644
EBC
Art.
Mix.
0.2097 -0.1142 0.0809
0.2458 -0.1277 0.1308
0.2557 -0.1012 -0.0308
0.1701 -0.1535
0.1158
0.3533 -0.0275 -0.0173
0.2971 -0.0800 -0.0928
0.2815 -0.1482 .0.0735
0.3726 -0.0706 -0.1500
0.1934 -0.1419 -0.0289
0.1434 -0.2097 -0.0352
0.1519 -0.1064 -0.0836
-0.0710 -0.1127 0.0887
-0.0105 -0.0444 -0.0012
-0.0018 .0.1191 0.0127
-0.0898 0.0336 0.0963
-0.1319 0.1068 0.1483
-0.0501
0.0807 -0.0147
-0.1110 0.0339 -0.0384
0.2116 0.3884 -0.0900
0.1868 0.2079 -0.0586
0,2773 0.3059 -0.0929
WPac.
-0.1504
0.0234
-0.0524
-0.0476
0.0440
0.0285
0.0348
0.0884
-0.0111
-0.0258
0.0106
-0.0867
-0.0671
0.0223
-0.0275
-0.0292
-0,1076
-0.1182
0.1210
0.1236
0.1668
0,2222 0.1713 0.1979 -0.0024 0.1952
0.1921
0.2511 0.1420 0.0323 0.0650
0.2037 0.1297 0.1492 0.2069 0.1426
0.2314 0.2336 0.0970 0.1091 0.1768
0.1873 0.2523 0.0852 0.1427 0.0876
0.2080 0.1724 0.0616 0.1023 0.0215
0.2429 0.2361 0.0495 -0.0558 0.0815
0.2841
0.2562 0.0157 -0.0226 0.0987
Table C. 1 Continued
Depth Comm.
80
90
100
110
120
130
140
0.7000
0.7539
0.5343
0,6299
0.5495
0.5668
0.4836
F8-90-G25
3
0.7450
10
20
30
40
50
60
70
80
90
100
110
0.6943
0.6709
0.6297
0.6587
0.5991
0.4511
0.5869
0.5664
0.6239
0.6738
0.6910
Tro.
Tm.
Ant.
0.0377
0.1719
0.1279
0.1960
0.1665
0.1466
0.0074
0.7683
0.7889
0.5885
0.5983
0.5894
0.6222
0.6591
0.2196
0.2478
0.2225
0.2303
0.2418
0.2257
0.1699
EBC
0.2213
0.1656
0.2355
0.2680
0.2235
0.2391
0.1093
0.7227
0.7212
0.6647
0.6589
0.6542
0.7074
0.5004
0.6315
0.6456
0.6408
0.7000
0.6275
0.2408
0.2261
0.2140
0.2240
0.2419
0.1582
0.2652
0.1515
0.2297
0.2113
0.2204
0.2243
0.3441
0.2444
0.3131
0.4596
0.6082
0.5657
0.6299
0.4868
0.6468
0.5831
0.4174
-0.0025 0.3126
-0.0020 0.3424
-0.0420 0.6426
-0.0114 0.4051
0.0025 0.4328
0.0084 0.4821
0.4617
-0.0001
0.0290 0.6178
-0.0019
0.2357
0.0066 0.4190
-0.0091 0.4162
0.0198
0.0839
0.1127
0.1246
0.1186
0.2169
0.1319
0.1313
0.0859
0.1673
0.2154
0,1355
0.2749
0.2435
0.2272
0.2920
0.3309
0.1903
0.2965
0.3423
0.1838
0.2424
0.2081
0.3834
Ati.
Mix.
WPac.
0.0579 0.0444 0.0754
0.0319 0.0342 0.1048
0.0904 -0.2144 0.1122
0.0119 -0.2956 0.1455
0.0054 -0.2257 0.1223
-0.0301 -0.2019 0.0913
0.0890 0.0142 -0.0138
0.0540 0.1324
0.0112 0.1759
-0.0550 0.0808
-0.0035 0.1327
-0.0258 0.1056
0.0537 0.1309
-0.0203 0.0468
-0.0216 0.0092
-0.2001 0.0366
-0.0935 0.1529
-0.1364 0.1181
-0.0131 -0.1747 0.1330
0.1019
0.1348
0.1693
0.1588
0.1835
0.0998
0.1089
0.0317
0.0580
0.0457
-0.0021
L13-81-g 138
0
20
40
60
80
100
140
200
220
240
260
280
300
320
340
360
380
400
420
0.6236
0.7246
0.6935
0.7164
0.5044
0.6279
0.4445
0.4089
0.4528
0.4609
0.5188
0.5899
0.6874
0.5991
0.4387
0.6749
0.4517
0.5692
0.5554
Vl-80-P3
19 0.7656
29 0.6176
39 0.7184
49 0.6444
0.0549
0.0633
0,0488
0.1846
0.0388
0.0648
0.0238
0.0460
0,2342
0.2439
0.1457
0.0535
0.6324
0.6068
0.5454
0.5576
-0.0261
-0.0274
-0.0081
0.0239
0.0007
0.0540
-0.0085
0.0312
-0.0126
0.1000
-0.0215
-0.0338
-0.0130
-0.0444
-0.0377
-0.0157
0.0012
-0.0681
0.1799
0.1139
0.2023
0.1544
0.087 1
0.0630
0.0988
0.1053
0.2732
0.2922
0.2173
0.2930
0.2624
0.2066
0.3525
0.2601
0.3071
0.3789
0.3172
0.2869
0.1929
0.4265
0.3577
0.4751
0.4146
0.6336 -0.0156 0.0124
0.5778 -0.0524 -0.0257
0.5920 -0.1083 -0.0248
0.1659
0.4991 -0.0701
0.4723 0.0204 0.1794
0.3783 -0.1073 0.1989
0.0318 0.0458 0.1524
0.2479 -0.0062 0.2927
0.5348 0.0221 0.1424
0.4847 0.0354 0.1465
0.0813 0.1363
0.0077
0.6184 0.0062 -0.0100
0.6056 0.0008 0.0890
0.5415 -0.0173 -0.0726
0.3369 -0.0881 0.0895
0.3583 0.0061 -0.1378
0.5331 0.0008 0.1056
0.5430 0.0581 0.1140
0.5821
-0.0237
-0.0282
0.1919 -0.1338 0.2043
0.1024 -0.1854 -0.0636
0.2352 -0.2521 0.1189
0.3175 -0.1837 0.01843
Depth Comm.
59
69
79
89
99
109
129
139
149
159
169
179
189
199
209
219
229
239
249
259
289
319
339
0.7560
0.5606
0.6015
0.7257
0.6490
0.6662
0.6673
0.5967
0.7486
0.8171
0.8188
0.6109
0.6615
0.2118
0.3388
0.7059
0.6721
0.5375
0.5542
0.7779
0.5249
0.5691
0.5897
EBC
Tro.
Tm.
Ant.
0.1759
0.1346
0.1012
0.2268
0.1659
0.1907
0.2863
0.6449
0.3836
0.4913
0.7153
0.6509
0.5013
0.6767
0.6242
0.7227
0.8120
0.8194
0.5893
0.6285
0.3563
0.3721
0.5910
0.6000
0.5448
0.5067
0.8004
0.6582
0.5837
0.6353
0.1829
0.0785
0.1151
0.2026
0.1947
0.0728
0.2434
0.2444
0.2383
0.2232
0.2065
0.1902
0.2160
0.0051
0.1112
0.2678
0.1842
0.1421
0.1630
0.1753
0.2325
0.2610
0.2141
0.4760
0.4943
0.5425
0.3046
0.3443
0.3214
0.2395
0.0424
0.2876
0,2214
0.1681
0.3476
0.3501
0.1639
0.2424
0.3885
0.4175
0.2138
0.2270
0.1705
0.0166
-0.0189
0.7412
0.7516
0.7595
0.7612
0.7302
0.7007
0.7801
0.7619
0.7677
0.7575
0.7808
0.6869
0.6956
0.6524
0.7908
0.8323
0.7207
0.1996
0.1709
0.65 15
0. 1501
0.6727
0.8408
0.6356
0.6743
0.5859
0.1251
0.1224
0.1750
0.2085
0.2173
0.3337
0.3924
0.3858
0.3910
0.3912
0.4046
0.3578
0.3410
0.3463
0.3843
0.3581
0.4601
0.4016
0.3424
0.2530
0.1617
0.3126
0.3547
0.3135
0.1200
-0.0702
-0.1029
-0.0838
0.278 1
0.2668
0.2254
0.2218
0.1691
0.1896
0.0563
0.0078
0.2349
0.0928
0.1427
0.0808
0.1830
0.1375
0.1479
0.1554
-0.0833
Art.
Mix.
WPac.
0.1663 -0.1272
0.1601 -0.3195
0.1458 -0.1361
0.0724
0.1312
0.0496
0.0801
0.0986
0.0544
0.0199
0.1372
0.0466
0.0702
0.0971
-0.0629
0.0347 -0.1453
0.0989 -0.1477
-0.0577 -0.5135
0.0775 -0.0665
0.0887 -0.2037
0.0884 -0.0750
-0.0343 -0.0438
-0.0543 -0.1221
0.0511 -0.2673
0.0508 -0.2421 -0.0146
0.1831 -0.0700 -0.1280
0.3182 -0.1508 0.0724
-0.0075 -0.2768 -0.0463
0.1160 -0.2575 0.1240
0.2138 -0.2594 -0.2036
0.2021 -0.4113 -0.0536
0.0898 -0.1174 -0.1489
0.1230 0.0284 -0.0491
0.3281 0.0363 -0.1703
0.3294 -0.0255 0.0022
W8709a-PC13
0
10
20
30
40
50
60
80
90
100
110
120
130
140
150
160
170
180
190
200
210
220
230
0.8372
0.8841
0.8978
0.8647
0.8053
0.7902
0.8385
0.8055
0.8003
0.8620.
0.8521
0.8050
0.7757
0.7204
0.7980
0.8001
0.7749
0.7296
0.7305
0.8214
0.6252
0.6400
0.6830
0.1615
0.1880
0.1389
0.1573
0.1172
0.1273
0.1212
0.0470
0.0994
0.1748
0.1504
0.1947
0.1278
0.1384
0.0664
0. 1260
0.1230
0.1517
0.1267
0.0739
0.0521
0.0597
0.0855
0. 1943
0. 1644
0.1450
0. 1539
0.1696
0. 1436
0. 1939
0.2248
0.1773
0.1637
0.1994
0.2529
0.2539
0.1855
0.1728
0.2292
0,2273
0.1867
0.2028
-0.1260
-0.1247
-0.1950
-0.1504
0.2381
-0.0888
0.1806
0.1648
0.2119
0.1387
0.1468
0.1472
0.1077
0.1504
0.1341
0.1327
0.0756
0.1067
0.2100
0.1628
0.2448
-0.1567
-0.0874
-0.1582
-0.0596
-0.0943
-0.1249
-0.1534
-0.1916
0.5171
-0.1021
-0.1862
-0.0705
-0.1454
-0.2807
-0.2624
-0.3125
-0.1361
0.4161 -0.0974
0.3501 -0.0266
0.2051
0.1827
0.2054
0.1299
0.1405
0.1961
0.1539
0.1263
0.1440
0.1706
0.1514
0,1471
0.1228
0.2045
0.1307
0.0643
0.1502
0.1442
0.1545
0.0352
-0.0192
-0.0663
0.0189
\0
I-
Table C. I Continued
Depth Comm. Tro.
Tm.
Ant.
0.73 11
0.773 1
0.1691
0. 1985
0. 1974
EBC
An.
Mix.
WPac.
W8709a-TC,PC8
0.8558 0.1966
1
7 0,9082 0.2393
16 0.8827 0.1979
26 0.9156 0.2023
36 0.8603 0.2764
46 0.8265 0.2404
56 0.8545 0.1346
65 0.8334 0.1862
76 0.8810 0.2167
86 0,8280 0.1775
96 0.8217 0.2157
105 0.8368 0.2307
125 0.7531 0.2140
135 0.8014 0.1818
145 0.7906 0.1087
155 0.6561 0.0527
165 0.4908 0.1036
175 0.5529 0.0405
185 0.6028 0.0203
0.7988
0.7488 0.2090
0.7610 0.1261
0.7494 0. 1532
0.7736 0. 1849
0.729 1 0.1715
0.7848 0.2177
0.7736 0.1973
0.7785 0. 1644
0.7622 0.2290
0.6998 0. 1887
0.81 85 0.2298
0.8248 0.2497
0.7 159 0.2644
0.4842 0.1039
0. 507 1 0.0696
0.5759 0. 1760
0.3591
0.4007
0.4092
0.3361
0.3576
0.3378
0.3540
0.3526
0.1965
-0.0139
-0.0487
0.0872
0.0451
0.0351
1T39-PC17
0 0.7330 0.1574
10 0.5524 0.2296
39 0.4613 0.0580
50 0.7359 0.2734
60 0.6271 0.1783
79 0.5435 0.1090
92 0.4231 0.1320
100 0.4755 0.1253
120 0,4662 0.1210
129 0.5003 0.0389
228 0,5094 0.1221
0.8210
0.5797
0.5386
0.7849
0.7361
0.5214
0.4253
0.5023
0.5335
0.6551
0.6131
0.1225
0.2037
0.1218
0.0954
0.1717
0.1215
0.0301
0.0047
0.0294
0.0928
0.0911
0.0973
0.2608
-0.1446
0.0245
0.0527
-0.0740
0.0020
-0.0343
-0.0654
0.0375
-0.0947
0.0257 -0.0688 -0.0661
0.0689 -0.2015 0.0935
0.3042 -0.0399 -0,1948
-0,0666 -0.1423 -0,1035
0.0144 -0.1361 -0.0499
0.4670 -0.1409 0.0391
0.2929 -0.3662 -0.0632
0.3148 -0.3264 -0.0260
0.3062 -0.2347 -0.1140
0.1356 -0.1517 -0.1351
0.0838 -0.3071 0.0081
0.0863 0.8259
0.1000 0.7842
0.0562 0.7737
-0.0087 0.6878
0.0200 0.7193
0.0605 0.7807
0.0688 0.6736
0.1184 0.8168
0.0563 0.7529
0.1150 0.6844
0.0969 0.7060
0.1074 0.7837
0.0756 0.7288
0.2076
0.1285
0.1352
0.1021
0.1394
0.1525
0.1672
0.1252
0.0400
0.0804
0.0963
0.1435
0.2171
0.1176
0.0091
-0.0596
0.0806
0.1299
0.0811
0.0956
0.0969
0.1523
0.1389
0.0982
0.0247
0.0818
0.0841
T1'39-PC12
0 0.7563
10 0.6612
20 0.6713
30 0.5511
40 0.5720
50 0.6974
60 0.5447
70 0.7191
80 0.6286
90 0.5839
100 0.5687
110 0.6644
119 0.6011
0.1630 -0.1659
0.1172 -0.1304
0.1339 -0.1082
0.1473 -0.1592
0.3740 0.1443 -0.1036
0.3891
0.3801
0.3238
0.4098
0.1203 -0.0677
0.0896 -0.0231
0.0982 -0.1181
0.0978 -0.1384
0.0865 -0.1001
0.0671 -0.1195
0.0793 -0.0826
0.0612 -0.1985
0.0634 -0.0490
0.1874
0.0286
0.2204
0.1964
0.1786
0.2352
0.1324
0.1887
0.1860
0.2162
0.1703
0.1169
0.0960
0.1086
0.1204
0.0243
0.0030
0.2560 -0.0009 -0.0547
0.0357 -0.0776
0.0659 -0.0192
0.4754 -0.1000 0.0499
0.4689
0.5315
0.0490 0.0177
0.0950 -0.0881 -0.0539
0.1531 -0.0115 -0.1553
0.2348 -0.0505 -0.0575
0.1290
0.2292
0.2035
0.0569
0.0935
-0.0344 -0.0062
0.0111 -0.0424
-0.0871 -0.0091
-0.0923 0.0344
-0.1582 -0.0072
0.1651 -0.2217 0.0081
0.0348 -0.1969 -0.0437
0.0749 -0.0903 -0.0607
0.0921
0.0450 -0.0025
Depth Comm.
130
139
150
159
170
1St)
190
199
210
219
229
239
Tm.
0.5793 0.1131
0.5402 0.0585
0.6590 0.1231
0.6415 0.0188
0.6043 0.0189
0.4638 0.1724
0.5802 0.1332
0.5521 0.1518
0.5439 0.0778
0.4889 0.1061
0.5311 0.1093
0.5640 0.1557
PAR87a-10
0 0.8262
5 0.8324
10 0.8808
15 0.8207
20 0.7758
25 0.7410
30 0,7888
35 0.7678
40 0.8953
45 0.8867
50 0.8031
55 0.7987
60 0.7371
65 0.7989
70 0.7477
75 0.7627
80 0.7545
85 0.7547
90 0.7332
95 0.7544.
100 0.7559
105 0.7879
110 0.7627
115 0.7598
0.1376
0.1278
0.1362
0.1547
0.1454
0.1856
0.1640
0.1697
0.1428
0.1067
0.0991
0.0942
0.0752
0.1469
0.1309
0.0923
0.0335
0.0466
0.0289
0.0669
0.0868
0.0281
0.0603
0.0469
Tm.
Ant.
0.7257
0.6943
0.7809
0,7782
0.7442
0.4684
0.7087
0.6666
0.6286
0.5941
0.5580
0.5309
0,1273
0.0760
0.1483
0.0800
0.1122
0.1245
0.0604
0.1593
0.1230
0.1280
0.0637
0.0723
0.0942
0.7698
0.7631
0.7961
0.7773
0.7283
0.6981
0.7067
0.6800
0.7378
0.6798
0.5735
0.5869
0,6290
0.6343
0.6384
0.6563
0.5860
0.5661
0.5183
0.5455
0.5573
0.6023
0.5638
0.5622
0.2551
0.2579
0.2307
0.2615
0.2060
0.2336
-0.0742 0.3628 0.1071 -0.0319
-0.1137 0.3753 0.1141 -0.0202
-0.1511 0.3880 0.0439 0.0008
-0.1481 0.3177 0.0301 0.0208
-0.2189 0.3500 0.0158 -0.1053
-0.1787 0.3625 -0.0300 0.0201
-0.1476 0.4253 -0.0606 0.0131
-0.1889 0.4260 -0.0368 -0.0752
-0.1979 0.5010 -0.0174 -0.1181
-0.1214 0.6097 -0.0654 -0.1085
-0.0669 0.6510 -0.1222 -0.0163
-0.0888 0.6174 -0.0743 0.0122
-0.1046 0.5330 -0,0267 -0.0097
-0.0460 0.5460 0.0286 0.0323
-0.0125 0.4818 0.0567 0.0003
-0.065 1 0.5082 0.0534 0.0394
0.0439 0.5836 0.0495 0.0147
0.0819 0.6042 -0.0101 0.0910
0.1088 0.6359 0.0136 0.0570
0.0805 0.6356 -0.0501 0.0890
0.1076 0.6154 -0.0050 0.0961
0.0644 0.6116 0.0404 0.0343
0.0529 0.6211 0.0315 0.0703
0.0164 0.6208 0.0156 0.0041
0.238
0.2291
0.1616
0.1033
0.1444
0.2251
0.1998
0.2701
0.2958
0.2377
0.2546
0.2277
0.2100
0.1773
0.1952
0.2080
0.2160
0.2357
EBC
Ait.
Mix.
WPac.
0.0660 -0.0734 -0.0708
0.1295 -0.0269 -0.1708 -0.0471
0.0925
0.0454
0.0263 -0.0720
0.0620 -0.0879
0.1501
0.0226
0,0299
0.0378 -0.1476
0.1015 -0.1255
0.0701 -0.4135
0.0275
0.0870 -0.1109 -0.1653 -0.0967
0.1359 -0.0581 -0.1829 -0.0632
0.2546 0.0282 -0.2450 -0.0431
0.2492 0.0155 -0.2144 0.0016
0.3042 0.0394 -0.3311 0.0002
0.3328 -0.0662 -0.3581 0,0962
Table C.! Continued
PAR87a-Ol
13
24
34
44
55
70
76
86
96
106
115
128
0.7413
0.7555
0.7013
0.6005
0.7935
0.6895
0.7092
0.7660
0.7158
0.6130
0.7142
0.7041
0.0851
0.0912
0.0524
0.0211
0.0041
-0.0154
-0.0188
0.0394
0.0121
0.0183
0.0052
0.0195
0.6376
0.6591
0.6130
0,5804
0.4410
0.4507
0.4713
0.4943
0.5148
0.5585
0.5718
0.5294
0.1686
0.1619
0.2088
0.2263
0.1750
0.1890
0.2024
0.2129
0.1868
0.2027
0.1945
0.2213
-0.2172
-0.0679
-0.0822
-0.1779
0.1361
0.1357
0.1471
0.1289
0.0861
-0.0202
0.0250
0.0711
0,4814
0.5310
0.4910
0.3379
0.7413
0.6500
0.6449
0.6674
0.6370
0.5028
0.5874
0.6021
0.0553 -0.1307
0.0007
0.1487 -0.0959
0.1287 -0.2226
0.0103- 0.0146
0.0690 0.0690
0.0783
0.0469
0.0734 0.0859
0.0487 -0.0127
0.0734 -0.0324
0.0594 -0.0114
0.0763
0.0335
-0.0001