University of Southern California Dissertations and Theses

Recent variability in the hyrdological cycle of tropical Asia from oxygen isotopes of tree celulose

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Recent variability in the hyrdological cycle of tropical Asia from oxygen isotopes of tree celulose

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RECENT VARIABILITY IN THE HYDROLOGICAL CYCLE OF TROPICAL ASIA
FROM OXYGEN ISOTOPES OF TREE CELLULOSE

by

Mengfan Zhu

________________________________________________________________________

A Dissertation Presented to the
FACULTY OF THE USC GRADUATE SCHOOL
UNIVERSITY OF SOUTHERN CALIFORNIA
In Partial Fulfillment of the
Requirements for the Degree
DOCTOR OF PHILOSOPHY
(GEOLOGICAL SCIENCES)

August 2012

Copyright 2012 Mengfan Zhu
ii

Acknowledgements

I would like to acknowledge the following persons for their help and support during my
graduate studies. My greatest gratitude goes to my advisor, Dr. Lowell Stott, who guided
me through the whole PhD training and taught me how to become a scientist. I am
grateful to our lab manager, Miguel Rincon, who patiently showed me the laboratory
skills and instrumental techniques. I owe my gratitude to my dissertation committee
members, Dr. Julien Emile-Geay, who helped me on statistical methods and graphic
display of data, Dr. Sarah Feakins, who reviewed and edited not only my dissertation, but
also my manuscripts for publication, and Dr. John Wilson, for his support as my
committee member outside of the Earth Sciences Department. I also would like to thank
my guidance committee members who were not on my dissertation committee, Dr. Doug
Hammond, whose breadth of knowledge inspired me greatly, and Dr. Ashish Sinha, for
many valuable discussions about the Indian Monsoon. I am also grateful to my research
collaborators and coauthors of my publications, Dr. Brendan Buckley and Wenhuo Liu,
for supplying the sample materials for my research, and Dr. Kei Yoshimura, for
providing his climate model outputs that I used in my studies. I am also thankful to my
labmates over the past years, including Dr. Max Berkelhammer, Dr. Deborah Khider,
Patrick Horan, Dr. Reetta Saikku, Dr. Nikolaus Buenning and Dr. Lisa Kanner. At last, I
would like to acknowledge my parents in China who have been my strongest support
while pursuing my degree overseas in the United States.

iii

Table of Contents

Acknowledgements ........................................................................................................... ii

List of Tables .................................................................................................................... vi

List of Figures .................................................................................................................. vii

Abstract ............................................................................................................................ xii

Chapter One
Introduction ....................................................................................................................... 1

Chapter Two
Background: the Indian Monsoon and the El Niñ o-Southern Oscillation ................ 11
2.1. The Indian Monsoon .............................................................................................. 11
2.1.1. Evolution of the Indian Monsoon .................................................................... 13
2.1.2. New theories of the Asian Monsoon ............................................................... 17
2.1.3. Future projections of the monsoon .................................................................. 19
2.2. The El Niñ o-Southern Oscillation .......................................................................... 22
2.2.1. ENSO mechanisms .......................................................................................... 24
2.2.2. ENSO-monsoon relationship ........................................................................... 26
2.2.3. Variability of ENSO ........................................................................................ 26

Chapter Three
Methodology: Oxygen Isotopes in Precipitation and Tree Cellulose ......................... 30
Summary ....................................................................................................................... 30
3.1. Oxygen isotopes in precipitation ............................................................................ 31
3.1.1. Temperature effect ........................................................................................... 31
3.1.2. Amount effect .................................................................................................. 32
3.2. Oxygen isotopes in tree cellulose ........................................................................... 35
3.2.1. Evaporative isotopic enrichment ..................................................................... 36
3.2.2. Peclé t effect ..................................................................................................... 38
3.2.3. Biochemical fractionation ................................................................................ 39
3.2.4. Exchange with xylem water ............................................................................ 39

Chapter Four
20th Century Seasonal Moisture Balance in Southeast Asian Montane Forests ...... 42
Summary ....................................................................................................................... 42
4.1. Introduction ............................................................................................................ 43
4.2. Materials and Methods ........................................................................................... 46
4.2.1. Study site ......................................................................................................... 46
iv

4.2.2. Tree ring sampling and processing .................................................................. 48
4.2.3. δ
18
O in tree cellulose ....................................................................................... 49
4.3. Results .................................................................................................................... 50
4.3.1. Cellulose δ
18
O overview .................................................................................. 50
4.3.2. Seasonal cycle .................................................................................................. 51
4.3.3. Interannual variability ...................................................................................... 54
4.4. Discussion .............................................................................................................. 57
4.4.1. Comparison with an earlier study .................................................................... 57
4.4.2. Cellulose δ
18
O as a proxy for regional rainfall ................................................ 58
4.4.3. ENSO-monsoon relationship reflected in cellulose δ
18
O ................................ 63
4.4.4. Hydrological balance of the winter dry season ............................................... 66
4.5. Conclusions ............................................................................................................ 74

Chapter Five
Indo-Pacific Warm Pool Convection and ENSO Since 1867 ...................................... 76
Summary ....................................................................................................................... 76
5.1. Introduction ............................................................................................................ 77
5.2. Materials and Methods ........................................................................................... 79
5.3. Results .................................................................................................................... 84
5.4. Discussion .............................................................................................................. 89
5.4.1. Convective activity over the warm pool .......................................................... 89
5.4.2. Comparison with tropical corals ...................................................................... 95
5.5. Conclusions and implications .............................................................................. 101

Chapter Six
Rapid Warming of the Tibetan Plateau and Monsoon Strengthening .................... 104
Summary ..................................................................................................................... 104
6.1. Introduction .......................................................................................................... 105
6.2. Oxygen isotopes on the Tibetan Plateau .............................................................. 107
6.2.1. Precipitation δ
18
O .......................................................................................... 107
6.2.2. Ice core δ
18
O .................................................................................................. 109
6.2.3. Tree cellulose δ
18
O ........................................................................................ 111
6.3. Methods ................................................................................................................ 112
6.4. Results .................................................................................................................. 113
6.4.1. Reproducibility .............................................................................................. 113
6.4.2. The δ
18
O relationship to climate parameters ................................................. 115
6.5. Discussion ............................................................................................................ 118
6.5.1. Comparison with a previous study ................................................................ 118
6.5.2. Latitudinal gradient of δ
18
O ........................................................................... 120
6.5.3. Variability of monsoon circulation ................................................................ 122
6.5.4. Hydroclimate history of the northeast Tibetan Plateau ................................. 125
6.6. Conclusions and implications .............................................................................. 127

v

Chapter Seven
Conclusions .................................................................................................................... 130

References ...................................................................................................................... 135

Appendix A. DCK subannual cellulose δ18O values ................................................. 158
Appendix B. DCK cellulose δ
18
O annual maxima, minima and mean values ......... 194
Appendix C. KRPM age-adjusted subannual cellulose δ
18
O values ........................ 196
Appendix D. KRPM monthly interpolated cellulose δ
18
O values ............................. 264
Appendix E. TDB and XDC annual cellulose δ
18
O values ........................................ 268

vi

List of Tables

Table 4.1. Correlation coefficients and p-values between Doi Chiang Dao
cellulose δ
18
O annual mean and the following: Doi Chiang Dao precipitation,
represented by the nearest grid point (19.25 ° N, 98.75 ° E) of GPCC V4 0.5
degree precipitation (Rudolf et al., 2003); Mainland Southeast Asia (MSEA)
precipitation, an area-weighted GPCC precipitation over the region of 10-25 ° N,
95-110 ° E; and All India Rainfall (AIR) (Parthasarathy et al., 1993). In bold are
the strongest correlations…………………………………………………………..

56

Table 5.1. Correlation coefficients between the cellulose δ
18
O annual minimum
values (first row) and the precipitation δ
18
O values in October (first
column)……………………………………………………………………………..

86

Table 5.2. Correlation coefficients between the cellulose δ
18
O values of any two
cores and the EPS values…………………………………………………………...

86

Table 5.3. List of coral δ
18
O records in the tropical Pacific Ocean, and the
correlation coefficients (R) of their October to December mean values with
Kirirom cellulose October values..............................................................................

96

Table 6.1. Correlation coefficients between the cellulose δ
18
O values of different
cores at XDC……………………………………………………………………….

114

Table 6.2. Correlation coefficients between the cellulose δ
18
O values of different
cores at TDB………………………………………………………………..............

114

vii

List of Figures

Figure 2.1. Long-term wind vectors at 850 mb atmospheric level and surface
precipitation over the Indo-Pacific region during June to September. Created
from NCEP Reanalysis data provided by the NOAA/OAR/ESRL PSD, Boulder,
Colorado, USA..........................................................................................................

12

Figure 2.2. Variation of surface latent heat flux, subsidence, and mixing ratio
deficit of air sinking into the boundary layer (Betts and Ridgway, 1989)………....

22

Figure 3.1. The first EOF mode of a) IsoGSM simulated precipitation δ
18
O and
b) CMAP precipitation over Southeast Asia (0-30 ° N, 90-120 ° E) and their
correponding PCs, c) the standardized monthly anomaly of the first PCs of the
precipitation (blue) and the precipitation δ
18
O (red), and d) the twelve month
moving averages. The first modes explain 23% and 20% of the total variance,
respectively, of the precipitation δ
18
O and the precipitation. The negative
correlation between the two (R = -0.59) reveals the precipitation amount effect.....

33

Figure 4.1. a) A hill shade map of Mainland Southeast Asia, created from 90m
digital elevation data (Jarvis et al. 2008). b) Climatology of five-day mean
precipitation and temperature from the nearest meteorological station Chiang
Mai, calculated from daily observations from 1951 to 2006……………………...

47

Figure 4.2. a) Subannual cellulose δ
18
O measurements from six different tree
cores and b) a close-up…………………………………………………………...

51

Figure 4.3. a) A scatter plot of the cellulose δ
18
O seasonal cycle from all the
annual rings of all cores. Horizontal axis represents the fractional distance from
the previous ring boundary. Anomalies are taken by subtracting annual means
from the raw δ
18
O values to get rid of the interannual variation. A third order
polynomial fit shows the average annual cycle is ~5‰. b) A scatter plot of the
monthly IsoGSM precipitation δ
18
O anomalies for the nearest grid point (20 ° N,
99.375 ° E). The anomalies are taken in the same fashion as in a………………….

52

Figure 4.4. The cellulose δ
18
O annual maxima values near tree ring boundaries
are singled out and averaged among all the cores to construct an annual
timeseries. Annual minima and annual mean

are constructed in similar fashion…..

53

Figure 4.5. Spatial correlation between the timeseries of Doi Chiang Dao annual
mean cellulose δ
18
O values and the field of September to November a) HadISST
(Rayner et al., 2003) and b) HadSLP (Allan and Ansell, 2006). Only correlations
higher than 90% significance level are shown……………………………………..

57
viii

Figure 4.6. a) and b) Long term mean vector wind field at 850 mbar atmospheric
level over India and Southeast Asia. c) and d) Long term mean surface
precipitation δ
18
O. e) and f) Correlation between the timeseries of Doi Chiang
Dao precipitation δ
18
O and the field of precipitation. Plots on the upper panel (a,
c and e) are for June-July-August (JJA), and plots on the lower panel (b, d and f)
are for September-October. The data for a and b is from NCEP reanalysis
(Kalnay et al., 1996), provided by the NOAA/ESRL Physical Sciences Division,
Boulder Colorado from their Web site at http://www.esrl.noaa.gov/psd/. Plots c,
d, e, and f use the data output from the IsoGSM model. Squares in c show the
GNIP stations in this region. The hollow square in both e and f is the grid box for
which the precipitation δ
18
O is calculated for Doi Chiang Dao..…………..............

60

Figure 4.7. Long term monthly mean of precipitation δ
18
O averaged for GNIP
stations in India (red) and Mainland Southeast Asia (blue). Refer to Fig. 4.6c for
locations of the GNIP stations………………………………………………….......

61

Figure 4.8. 21-year moving window correlations of September to November SOI
with cellulose δ
18
O annual mean (blue), and with June to September AIR (red).
For direct comparison, the signs of the correlation coefficients with cellulose
δ
18
O are reversed. Dots are correlations higher than 95% significance level…..…

64

Figure 4.9. a) The first EOF mode of CMAP precipitation (Xie and Arkin, 1997)
over the Indo-Pacific region. b) The corresponding first principle component
(PC1) strongly correlates with Niñ o4 SST (R=0.61, p<0.001)………………….....

66

Figure 4.10. Relative humidity (red) for the dry season November to April at the
nearest meteorological station Chiang Mai, and the November to April Parmer
Drought Severity Index (UCAR PDSI) for the region of 18-20 ° N, 98-100 ° E…

67

Figure 4.11. a) Monthly fog and rainfall amounts at Mengla, Xishuangbanna,
Southwest China for a three year interval. b) Isotope measurements of the dry
season (November to April) fog water and rain water. c) A linear regression of
monthly fog drip amount against the frequency of fog occurrence indicates that
the fog frequency could be used to represent the total amount of fog water
intercepted by plant canopy. Data are provided by Liu et al. (2007)……………....

70

Figure 4.12. Monthly SST/T2m anomalies averaged over the region of 10-25 ° N,
95-110 ° E show a warming trend in the 20th century. Data is from National
Climatic Data Center’s Global Historical Climatology Network Gridded
Products, accessed through the KNMI climate explorer (http://climexp.knmi.nl)...

72

Figure 4.13. Dry season (November to April) fog frequency at six
meteorological stations in northern Thailand. Refer to Fig. 4.1 for the location of
these meteorological stations……………………………………………………….

73
ix

Figure 5.1. a) Map of Southeast Asia showing the sampling site Kirirom and the
nearby meteorological station Phnom Penh. Boxed region represents the Indo-
Pacific Warm Pool. b) Scanned image of a tree core sample showing the annual
ring structures. c) Climatology at the meteorological station of Phnom Penh, with
temperature in curve, and precipitation in bars………………………………….....

79

Figure 5.2. The long term mean wind vectors at 850 mbar level for the rainy
months of a) June-July-August, which represents the Indian Summer Monsoon
season, and b) October-November, which represents the rainy period after the
Indian Summer Monsoon retreats. Also shown in color for each rainy period is
the spatial correlation between the precipitation δ
18
O at Kirirom and the field of
precipitation amount. Only correlation above 90% significance level is shown.
The data for wind vectors, precipitation δ
18
O and precipitation amount are all
from IsoGSM model outputs…………………………….........................................

80

Figure 5.3. a) Subannual cellulose δ
18
O measurements of the three cores
KRPM15B (red), KRPM10A (blue) and KRPM09A (green), continued in b……..

83

Figure 5.4. a) Intraannual variation of the cellulose δ
18
O composited from all the
individual annual rings of all three cores. Horizontal axis represents the distance
to the ring boundary with respect to the width of the ring. Anomalies are taken
by subtracting annual means from the raw δ
18
O values to get rid of the
interannual variation. b) Same but for precipitation δ
18
O from GNIP observations
in Bangkok. c) Same but for precipitation δ
18
O from monthly IsoGSM outputs…..

84

Figure 5.5. a) Monthly interpolated cellulose δ
18
O averaged from three cores. b)
Anomalies of October cellulose δ
18
O after subtracting the long-term mean. Also
shown are recent ENSO events…………………………………………………….

87

Figure 5.6. The difference in precipitation δ
18
O between June-July-August mean,
when the moisture source is the Indian Summer Monsoon, and October, when
the moisture source is the South China Sea-Maritime Continent. Data are from
Bangkok GNIP record (a) and IsoGSM simulation at the grid point near Kirirom
(b)…………………………………………………………………………………..

91

Figure 5.7. Spatial correlation of October Kirirom cellulose δ
18
O values with the
October-November-December mean of a) CMAP precipitation, and b) NOAA
interpolated OLR. Only correlation above 90% significance level is shown. Box
in a shows the Niñ o-4 region and triangles in b show the sites of tropical Pacific
coral δ
18
O records, see Table 5.3 for details of the sites………………………......

93

x

Figure 5.8. Correlation between Kirirom cellulose δ
18
O October values and
Niñ o-4 SST index for October (R=0.56). Thick lines are the 10-year low-pass
filters. Shaded bars highlight the similar decadal variations between the two
timeseries…………………………………………………………………………...

95

Figure 5.9. The monthly values of the five coral δ
18
O records that best correlate
with the Kirirom cellulose δ
18
O. Tarawa, Maiana, and Palmyra corals are from
the central Pacific, and Bunaken and Madang corals are from the western Pacific..

98

Figure 5.10. Power spectral density of the monthly Kirirom cellulose δ
18
O
showing major periodicities at 2.5, 3.6, 6, and 13.5 years………………................

99

Figure 5.11. 2-7 year band-pass filters of the five coral δ
18
O records and the
Kirirom cellulose δ
18
O record. The central Pacific coral records (Tarawa, Maiana,
and Palmyra) correlate negatively with the Kirirom cellulose δ
18
O, therefore their
y-axes are reversed. The western Pacific coral records (Bunaken and Madang)
correlate positively with the cellulose record. Decreased variability between
1920s and 1960s (interval between the shaded bars) appears to be the common
feature of all the records…………………………………………………………....

100

Figure 6.1. a) Map of the Tibetan Plateau showing tree sampling sites XDC and
TDB of this study. The other square is the tree cellulose site of Bomi (Shi et al.,
2011). Ice core sites are represented by triangles. Arrows show the atmospheric
circulation pattern in the summer rainy season. Shaded region approximates the
present northward extent of the summer monsoon influence. b) This map
corresponds to the boxed region in a, showing our two tree sites in squares and
their nearby meteorological stations in filled circles. Another square to the north
of XDC represents the tree cellulose site in the study of Liu et al. (2009)………...

107

Figure 6.2. a) Ice core δ
18
O in decadal resolution for the past millennium from
Dunde (red), Puruogangri (green), and Dasuopu (blue). b) Annual cellulose δ
18
O
averaged from the different cores at the same site for XDC (red), TDB (green),
and the annual cellulose δ
18
O from a previous study in Bomi (blue). Bold black
lines are 40-year low-pass filter…………………………………………………...

110

Figure 6.3. Annual measurements of cellulose δ
18
O for the four tree cores from
site TDB (a) and XDC (b)…………………………………………………………

113

Figure 6.4. Correlation between cellulose δ
18
O and climate parameters for
different months from previous year (-) to the current year. TDB cellulose δ
18
O
is correlated with the climate parameters from its nearest three meteorological
stations Tongde (a), Zeku (b) and Henan (c); and XDC cellulose δ
18
O is
correlated with the climate parameters from its nearest meteorological station
Qilian (d). Solid lines represent 95% significance level…………………………...

116
xi

Figure 6.5. a) The disagreement between our XDC cellulose δ
18
O (red) and the
cellulose δ
18
O from a previous study (Liu et al., 2009) that is only ~50 km away.
b) A sketch showing the topographic profile through our site XDC and the site of
Liu et al. (2009)……………………………….........................................................

119

Figure 6.6. a) The long term mean monthly relative humidity at Bomi, Tongde,
Zeku, Henan and Qilian meteorological station. b) The difference in growth
season (May to August) relative humidity between Tongde, Zeku, Henan, which
represent TDB tree site, and Qilian, the nearby meteorological station of XDC
tree site……………………………………………………………………………..

121

Figure 6.7. The difference of cellulose δ
18
O between XDC and TDB. Larger
difference implicates stronger summer monsoon. Bold black lines are 20-year
low-pass filter…………………………………………………………………...….

124

Figure 6.8. XDC cellulose δ
18
O plotted with Northern Hemisphere temperature
reconstruction and Dunde ice core δ
18
O. Bold black lines are 40-year low-pass
filter………………………………………………………………………………...

127

xii

Abstract

This dissertation investigates hydrological variability within tropical Asia over the past
several few centuries as reflected in the stable oxygen isotope composition of
atmospheric moisture. The stable isotopes of water in the climate system are unique
tracers of moisture transport and tropical rainfall variability. The isotopic signal of
atmospheric moisture within the tropics is transferred to cellulose of tropical trees during
photosynthesis. Thus, the isotopic composition of tree cellulose can provide an archive of
past hydrologic variability through isotopic reconstructions of the cellulose extracted
from annual rings of long lived trees. The tropical atmospheric variability reflected in
tropical trees can include variations in the Indian Monsoon and changes in moisture
availability over Asia in response to the El Niñ o-Southern Oscillation (ENSO). Here an
attempt has been made to better understand how the atmospheric dynamics associated
within these climate phenomena influence the isotopic composition of tree cellulose and
how these climate signatures have changed through time. High-resolution water isotope
records are developed from trees collected from northern Thailand, southern Cambodia,
and eastern part of the Tibetan Plateau. These records are examined to assess whether and
how the 20th century is unique in terms of the hydrological conditions in tropical Asia
under the influences of both monsoon and ENSO with the observed temperature changes.

In northern Thailand, the oxygen isotopic composition (δ
18
O) of tree cellulose samples of
Pinus kesiya from a montane forest has been analyzed in subannual resolution for the past
xiii

80 years. The cellulose δ
18
O values exhibit a distinctive annual cycle with an amplitude
of up to 12‰, which is interpreted to reflect primarily the seasonal cycle of precipitation
δ
18
O. The cellulose δ
18
O annual mean values correlate significantly with the amount of
summer monsoon precipitation over the India subcontinent, corroborating recent studies
that suggest the so-called “isotope amount effect” in the tropical precipitation δ
18
O
reflects the hydrological processes of the upstream or the moisture source regions instead
of the rainfall amount at the local site. No obvious trend in the summer monsoon
precipitation is detected from the cellulose δ
18
O record. However, the record does suggest
a temporal weakening relationship between the Indian Monsoon and ENSO over the 20th
century. The annual maxima in the cellulose δ
18
O values are representative of the
moisture balance during the winter dry season, and possibly document a decreasing trend
in the isotopically-distinct fog water input during the dry season because of the warming
in the 20th century.

Isotope chronologies of Pinus merkusii from a coastal lowland forest in Cambodia have
been generated to investigate hydrological variability over the Indo-Pacific Warm Pool
(IPWP), based on the aforementioned observation that the δ
18
O in precipitation reflects
the hydroclimate of the moisture source region. The IPWP is a major source of heat and
moisture to the atmosphere and thus strongly influences the global climate. Recognizing
its past variability is crucial for understanding large scale climate dynamics such as
ENSO. The subannual cellulose δ
18
O has been replicated with multiple tree cores which
span the past 140 years. The analysis of model outputs from a water isotope-enabled
xiv

atmospheric model is used in conjunction with isotopic data from tree cellulose and
precipitation to investigate moisture sources and how these sources of moisture vary on
different timescales. The cellulose δ
18
O exhibits strong correlations with convection
intensity and precipitation amount over the IPWP. Spectral analysis of the cellulose δ
18
O
reveals significant peaks at 2-7 years corresponding to ENSO frequencies. This cellulose
δ
18
O record exhibits no clear overall trend, but the period of 1880s through 1910s is
characterized by relatively enriched cellulose δ
18
O values, which possibly indicates a
background condition in the tropical Pacific Ocean that was more El Niñ o-like.

Stable isotope dendrochronologies have been developed for sites across the eastern
Tibetan Plateau. The plateau plays a pivotal role in creating the land-sea thermal contrast
that is theorized to drive the summer monsoon circulation. Today, precipitation across the
southern Tibetan Plateau is dominated by moisture carried by the summer monsoon
winds. The isotopic composition of this moisture varies with the precipitation amount.
Over the northern Tibetan Plateau, atmospheric moisture that falls as precipitation is from
westerly air masses that carry a large fraction of recycled moisture across the continent.
The isotopic composition of this moisture source is distinct from monsoon moisture over
the southern Plateau. In addition, there is an important temperature effect that affects the
isotopic fractionation of oxygen isotopes in precipitation over the northern and central
Plateau. An inter-comparison of annually resolved tree cellulose δ
18
O values from two
sites on the Tibetan Plateau forming a latitudinal transect, together with data from a
former study are used here to investigate the interplay of these different moisture sources
xv

and temperature influence over time. The data from the northerly site indicate the late
20th century was the warmest and/or driest period of the past 500 years in the
northeastern Tibetan Plateau, whereas evidence from the southerly site suggests there has
been an increase in the strength of the summer monsoon circulation since the 1940s
compared to the past two centuries.

These studies have demonstrated that tree cellulose δ
18
O is a robust high-resolution proxy
for hydroclimate in the past. In tropical Southeast Asia, tree cellulose δ
18
O could shed
light on surface hydrology of the IPWP that is closely related to ENSO. Observations
from tree cellulose δ
18
O in my studies have suggested no overall trend in the frequency or
magnitude of ENSO variability through the 20th century, but a possible El Niñ o-like
condition from the 1880s to the 1910s. Tree cellulose δ
18
O in northern Thailand indicates
no overall trend in the monsoon precipitation in South and Southeast Asia. However, the
new isotopic data presented here suggest monsoon circulation has intensified in the late
20th century across the eastern Tibetan Plateau.

1

Chapter One

Introduction

The Indian Monsoon has been recognized as the dominant climate phenomenon in South
and Southeast Asia. During Northern Hemisphere summer, low atmospheric pressure
over the Asian continent associated with intense lower tropospheric heating produces
what is termed the Indian Summer Monsoon. These are moist southwesterly winds from
the tropical Indian Ocean. The transport of tropical moisture by the monsoon winds
results in a rainy season in South Asia. Although the summer monsoon rains are a
reoccurring phenomenon, the interannual variability of the monsoon timing and duration
of the rains have profound societal and humanitarian impacts. Therefore the Indian
Monsoon attracted the attention of scientists as early as the 17th century (Halley, 1686).
However, currently the dynamics of the monsoon still remain unclear, which hinders
prediction of monsoon variability on interannual to centennial scales.

A traditional view of the Indian Monsoon attributes the seasonal variations in winds to
the land-sea thermal contrast that arises from atmospheric heating of the Asian landmass
during summer (Webster et al., 1998). Warming of the Northern Hemisphere continents
is therefore an important forcing of the monsoon system. With homogeneous radiative
forcing, the smaller thermal inertia of the land and the snow-albedo feedback leads to a
more pronounced warming over land than ocean. This differential heating increases the
land-sea thermal and pressure gradient and is hypothesized to strengthen the monsoon
2

circulation (Douville et al., 2000). However, in climate model simulations of global
warming scenarios, monsoonal circulation and other tropical large-scale circulations
often weaken (Knutson and Manabe, 1995). Besides the strength of the monsoon
circulation, the amount of atmospheric water vapor that is transported towards the
monsoon regions is also responsible for the amount of monsoonal precipitation. Because
there is a positive relationship between the saturation water vapor pressure and
temperature of the atmosphere, the Clausius-Clapeyron relation (Li, 1956), as Sea
Surface Temperatures (SSTs) warm, evaporation increases and this increases the amount
of moisture in the tropical atmosphere. Many studies recognized that this increased
atmospheric moisture content is the dominant influence over any effect of the monsoon
circulation, and leads to intensified monsoonal precipitation under global warming
scenario (Douville et al., 2000; May, 2004; Ueda et al., 2006), even without a notable
intensification of monsoonal circulation. These contrasting views of how the monsoon
system will respond to future warming are difficult to reconcile without an adequate
database of observations of past natural variations of the monsoon behavior at times of
cooling and warming.

Direct evidence of the Indian Monsoon variability includes meteorological
measurements of rainfall in South Asia. All India Rainfall (AIR) has been compiled as an
index for the monsoonal precipitation that extends back to the mid-19th century
(Parthasarathy et al., 1994). Although there is clear evidence of interannual variability in
AIR that is related to other climate phenomena such as the El Niñ o-Southern Oscillation
3

(ENSO), there is no significant long-term trend in the AIR index during the 20th century
as temperature has warmed (Parthasarathy et al., 1994). However, the instrumental
records and the reanalysis data that are available reveal an apparent weakening of
monsoon circulation in recent decades over both India and East Asia (Wang, 2001; Wu,
2005).

In an effort to put the 20th century variability of monsoon in the context of its longer-
term record of natural variability, paleo-records of monsoon variability have been
obtained from both marine and terrestrial proxies. Using abundance data of planktonic
foraminifera that inhabit the upper ocean in regions influenced by wind-forced upwelling
in the Arabian Sea, Anderson et al. (2002) concluded that the southwest monsoon winds
have increased during the past four centuries, which is consistent with a response to
Northern Hemisphere warming. But here, the response of planktonic foraminiferal
production to changing monsoon winds is not a direct measure of how monsoon winds
over the continents have varied in response to the warming. Asian speleothem records
(Fleitmann et al., 2003; Zhang et al., 2008) document enhanced monsoon rainfall
amounts during the Medieval Warm Period and reduced monsoon rainfall during the
Little Ice Age, but the interpretation of speleothem calcite δ
18
O is also subject to debate
(Pausata et al., 2011). Moreover, neither marine sediments nor speleothems have high
enough temporal resolution to resolve interannual variations of monsoon. Clearly, the
network of proxy reconstructions needs to be expanded to include more high-resolution
proxies in order to better document the natural monsoon variability in terms of both the
4

circulation and the rainfall amount on interannual to centennial timescales beyond the
instrumental period.

On interannual timescales, the variability of monsoon precipitation over India is strongly
affected by ENSO (Walker, 1918; Webster, 1995; Yasunari, 1990). ENSO itself is a
coupled atmospheric-oceanic phenomenon that occurs within the tropical Pacific. In
normal years or during La Niñ a, easterly trade winds force warm surface waters towards
the western tropical Pacific, creating a pool of warm water termed the Western Pacific
Warm Pool (WPWP). The heat provided to the lower atmosphere from these warm
waters leads to uplift and atmospheric convection, which drives large scale atmospheric
circulation. During an El Niñ o the warm surface waters recede from the western Pacific
towards the central and eastern equatorial Pacific. And with the migration of these warm
waters, the center of atmospheric convection also migrates eastward. As a result of the
eastward migration of atmospheric convection, El Niñ o years are associated with
reduced rainfall over the Indian Monsoon region as well as much of Southeast Asia.

An accurate prediction of future monsoon variability in response to atmospheric
warming also requires a better understanding of ENSO’s response to warming.
Unfortunately, our current knowledge of ENSO variability over extended periods of time
is equally limited. Scientific inquiries about ENSO longer term behavior have focused
primarily on two major themes: how has the temperature structure of the tropical surface
ocean within the Pacific responded to global climate changes such as those occurring
5

during the last millennium, and how have the frequency and amplitude of ENSO events
changed in response to global temperature variations. With regard to the first theme, a
number of paleo-SST reconstructions for the tropical Pacific in the past when the
background climate was different (Cobb et al., 2003; Newton et al., 2006; Oppo et al.,
2009) have supported the so-called thermostat mechanism (Clement et al., 1996), which
projects a La Niñ a-like tropical Pacific mean condition as the global climate warms. But
other paleoclimate records have pointed to more La Niñ a-like tropical Pacific conditions
during cooler global climate states such as the Little Ice Age (Newton et al., 2006; Yan
et al., 2011), and these records appear to support some coupled Global Climate Model
(GCM) simulations that find weakened Walker circulation as the climate warms (Held
and Soden, 2006; Vecchi et al., 2006).

The second theme has investigated past interannual variations of ENSO using high-
resolution paleoclimate monsoon proxies including tree rings (dendrochronology) and
paleo-SST reconstructions from coral δ
18
O (Cane, 2005). The traditional
dendrochronology approach relies upon an empirical relationship between tree ring
width/density and climate parameters such as precipitation and temperature, and
reconstructs ENSO by sampling trees in regions with strong ENSO influence (Braganza
et al., 2009; D'Arrigo et al., 2005; Fowler, 2008). In this case, the reconstruction of
ENSO behavior is indirect, since based on long-range teleconnections (Cane, 2005). This
approach also assumes a stationary tree growth response to ENSO variations, which has
not been thoroughly evaluated. Tropical Pacific coral geochemistry has been used to
6

reconstruct SSTs as well as hydrological variations (salinity) in the ENSO core regions
(Cole et al., 1993; Quinn et al., 2006), but most existing coral records barely extend
beyond the past two centuries. Currently, the Palmyra coral δ
18
O record from Cobb et al.
(2003) is the only record that documents how the frequency and amplitude of SSTs have
varied on interannual timescales during times when the climate background was different
than today (e.g. the Medieval Warm Period and the Little Ice Age). But the coral δ
18
O
contains both SST and hydrological (salinity) influences, and the Palmyra record is
discontinuous during several intervals. The fact that there are so few records available
from the tropical Pacific to assess how ENSO has varied in the past underscores a need to
find additional highly-resolved proxies that can be used to reconstruct the hydrological
conditions on interannual timescales over the past few centuries.

In conclusion, the inadequate state of knowledge about the monsoon’s natural variability
and how ENSO has varied on longer timescales motivates additional efforts to obtain
well-resolved paleoclimate records that extend the available observational database. In
this dissertation, oxygen isotopes in tree cellulose are used as an investigatory tool to
reconstruct the climatological and hydrological variability in tropical and subtropical
Asia. Oxygen isotopes (δ
18
O) are tracers in the hydrological cycle due to the mass-
dependent fractionation of heavy and light isotopologues during evaporation and
condensation. In the tropics and in the monsoon region, the δ
18
O of precipitation exhibits
what has been termed the amount effect (Araguas-Araguas et al., 1998) that could be
utilized to reconstruct surface hydrology. The δ
18
O of precipitation has also been
7

demonstrated to effectively indicate the moisture source (Aggarwal et al., 2004) or to
track changes in moisture transport trajectory (Pausata et al., 2011). Due to these traits, a
Global Network of Isotopes in Precipitation (GNIP) has been established to routinely
measure the δ
18
O of precipitation in addition to traditional climate parameters such as
precipitation amount and temperature, in order to facilitate investigations related to water
cycle of the Earth (IAEA/WMO, 2006). But this program has become operational in 1961,
and the instrumental network is sparse in remote locations. As an effort of extending the
limited observational database, information about precipitation δ
18
O has been extracted
from terrestrial archives such as ice cores (Thompson et al., 2003; Thompson et al., 1989;
Thompson et al., 2000) and speleothems (Sinha et al., 2011; Wang et al., 2001; Yuan et
al., 2004) to infer climatological and hydrological changes on centennial to millennial
timescales. However, on shorter timescales, these records usually fail to provide
information that can be used to assess interannual or decadal-length variability because of
the coarse temporal resolution of these archives and because of difficulty in dating the ice
cores.

The δ
18
O signature of precipitation can also be documented from plant organic matter
because the growth of plants utilizes soil moisture, which is ultimately derived from
precipitation. The δ
18
O of tree cellulose from living trees has been found to exhibit
empirical relationships with humidity and temperature (Burk and Stuiver, 1981).
Mechanistic models have been developed afterwards to show that the isotope signals in
soil water are transmitted to tree cellulose during photosynthesis (Farquhar and Lloyd,
8

1993; Roden et al., 2000; Sternberg, 2009). The synthesis of cellulose also incorporates
isotope enrichment at leaf surfaces due to evaporative isotope exchange determined by
relative humidity and other factors such as leaf boundary conditions. In the tropical
monsoon region, high relative humidity suppresses the leaf evaporative signal, and recent
studies of tropical trees have indicated that cellulose δ
18
O varies primarily as a function
of the precipitation amount and variations in moisture source (Anchukaitis and Evans,
2008; Evans and Schrag, 2004; Poussart and Schrag, 2005), consistent with the isotope
effects in precipitation δ
18
O. These studies have illustrated the potential of cellulose δ
18
O
to reconstruct precipitation δ
18
O beyond the instrumental period. The most important
attribute of tree cellulose δ
18
O is that tree rings can be precisely dated to the exact year
because of the annual patterns of xylem growth. The study of tree ring width has been a
mature discipline in climate research (Cook et al., 2010; Sano et al., 2009), which allows
accurate dating of tree rings with sophisticated cross-dating techniques. Temporally,
living trees can provide chronologies up to several centuries or even over a millennium
back in time (Leavitt et al., 2010). Spatially, the wide geographic distribution of growing
trees makes tree cellulose δ
18
O studies available for different climatological and
environmental conditions. These advantages make tree ring cellulose an excellent
candidate as a recorder of precipitation δ
18
O at annual to subannual resolution on
centennial to decadal timescales. The δ
18
O records are then utilized to reconstruct past
hydroclimate variability in high resolution. In this dissertation, the δ
18
O of tree cellulose
has been analyzed at different locations in Southeast Asia and the Tibetan Plateau in
order to answer the following questions.
9

i. How has the monsoon precipitation changed with the observed warming
trend?
ii. Has the monsoon circulation varied in the same way as the monsoon
precipitation?
iii. Is the influence of ENSO on the monsoon a stationary phenomenon?
iv. How could tree cellulose δ
18
O be used to understand ENSO such as the mean
state of tropical Pacific, and the frequency and amplitude of ENSO events?

Chapter 2 provides the background knowledge about the Indian Monsoon and ENSO.
Existing theories and hypotheses about the physics of both monsoon and ENSO will be
introduced. Past variability of monsoon and ENSO from geological to centennial
timescales as reconstructed from a vast array of proxy records will be described.
Mechanisms that induce future changes of monsoon and ENSO as simulated by
numerical climate models will also be presented.

Chapter 3 explains in detail the methods that have been used in my studies. It includes the
isotope fractionation of oxygen isotopes in water, and the resulting different isotope
effects in precipitation, namely the amount effect and the temperature effect. This chapter
also covers the processes through which oxygen isotope signatures in precipitation is
transmitted to the cellulose component of tree wood. A simplified equation is derived
from geobiochemical models for oxygen isotopes in tree cellulose.

10

Chapters 4, 5 and 6 presents tree cellulose δ
18
O studies from several sites in Southeast
Asia and the Tibetan Plateau. These are original studies published in scientific journals or
currently in revision, respectively as
Zhu, M., Stott, L., Buckley, B., and Yoshimura, K., 2012. 20th century seasonal
moisture balance in Southeast Asian montane forests from tree cellulose δ
18
O, Climatic
Change, DOI 10.1007/s10584-012-0439-z.
Zhu, M., Stott, L., Buckley, B., Yoshimura, K., and Ra, K., 2012. Indo-Pacific Warm
Pool convection and ENSO since 1867 derived from Cambodian pine tree cellulose
oxygen isotopes, Journal of Geophysical Research-Atmospheres, Vol. 117, D11307,
doi:10.1029/2011JD017198.
Zhu, M., Stott, L., Liu, W., and Gou, X., in revison. Twentieth century rapid warming
and monsoon strengthening on the Tibetan Plateau, Geology.

Chapter 7 summarizes the observations and findings from the three tree cellulose δ
18
O
studies and synthesizes them in order to answer the questions raised above.

11

Chapter Two

Background: the Indian Monsoon and the El Niñ o-Southern
Oscillation

2.1. The Indian Monsoon
The Indian Monsoon is one of the most complex climate phenomena on earth.
Traditionally, the annual monsoon cycle is interpreted as a result of the differential
heating between the Eurasian landmass and the adjacent tropical oceans (Webster et al.,
1998). During boreal summer, the troposphere over the Eurasian continent is intensively
heated by the surface heat fluxes primarily from the Tibetan Plateau due to its high
elevation, which creates a low pressure center over the Asian continent at lower
atmospheric level. This continental low draws moist winds from the tropical oceans.
Uplift and subsequent cooling of these winds over the continent bring about large
amounts of precipitation.

At lower tropospheric level, the Asian monsoon region is dominated by two large scale
circulation patterns during boreal summer (Lau et al., 2000). The Inter-hemisphere Gyre
Circulation consists of easterlies over the southern Indian Ocean, Somali jets over the
Arabian Sea and the westerlies across the Indian subcontinent and the Bay of Bengal.
This evolves into southwesterly flow over Southeast Asia and the South China Sea (Fig.
2.1). The other circulation pattern is the anti-cyclonic flow around the Western Pacific
Subtropical High, on the west flank of which is the southwesterly flow over East Asia.
12

These monsoonal winds transport large amount of precipitation to South and East Asia.
In South Asia, the Indian Monsoon display classical monsoon circulation patterns. In East
Asia, the meridional circulation of the East Asian Monsoon is more complicated. In this
dissertation, I focus on the Indian Monsoon, which affects South Asia, Southeast Asia
and southern parts of the Tibetan Plateau. The word monsoon refers to the Indian
Monsoon thereafter.

Figure 2.1. Long-term wind vectors at 850 mb atmospheric level and surface precipitation over the Indo-
Pacific region during June to September. Created from NCEP Reanalysis data provided by the
NOAA/OAR/ESRL PSD, Boulder, Colorado, USA.
13

2.1.1. Evolution of the Indian Monsoon
The Indian Monsoon is an annually reoccurring pattern which has been evidenced to be a
stable phenomenon since the collision of the Indian continent with Asia (Clemens, 2006).
Geological records indicate increased seasonality across South and East Asia in the last
11 million years, which marks the onset of strong summer and winter monsoons in
response to the tectonic uplift of the Tibetan Plateau (Prell and Kutzbach, 1992).
Paleoclimate records have shown that the monsoon responds to insolation on different
timescales. In particular, evidence including loess, speleothem and marine sediments that
extends back to orbital timescales indicates 23 and 41 thousand year (kyr) cycles in the
monsoon variability. However, two different views exist as to whether the Northern
Hemisphere summer insolation or the latent heat transfer from the Southern Hemisphere
is the dominant forcing on monsoon variability (Ruddiman, 2006). According to the first
view, Northern Hemisphere summer insolation causes differential heating between land
and ocean in the monsoon region and is important to induce the monsoon circulation
(Kutzbach, 1981). Evidence supporting this view includes the 23 kyr precession cycle
present in monsoon records such as the Mediterranean sapropel layers (Rossignolstrick,
1983), African tropical lakes (Kutzbach and Streetperrott, 1985), and Chinese and
Brazilian speleothems (Cruz et al., 2005; Wang et al., 2005; Yuan et al., 2004). This 23
kyr cycle is also exhibited in records of methane concentration extracted from Antarctic
ice cores (Petit et al., 1999). Methane is a well-mixed atmospheric component. One of its
major sources is the tropical wetlands in the vast monsoon region of tropical and
subtropical Asia (Chappellaz et al., 1990). The δ
18
O of O
2
in air extracted from ice cores
14

also exhibits this 23 kyr cycle (Shackleton, 2000). The variation of δ
18
O in air is
controlled by the respiration in plants and animals, which removes the lighter isotope
16
O
from the atmosphere and leaves the remaining O
2
more isotopically enriched, the so-
called Dole effect (Dole, 1936). Changes in tropical monsoons could affect the global
biomass productivity and therefore cause shifts in both methane and the δ
18
O of O
2
in air
(Bender et al., 1994).

On the other hand, marine sediment records from the Arabian Sea indicate monsoon
variability that is in phase with the Northern Hemisphere summer insolation at the 41 kyr
obliquity cycle, and lags the Northern Hemisphere summer insolation at the 23 kyr
precession band by 8 kyr (-120° phase). Clemens and Prell (2003) therefore proposed that
besides sensible heating of the Asian landmass determined by the Northern Hemispheric
summer insolation, condensational heating from moisture evaporated and transported
from the subtropical Indian Ocean in the Southern Hemisphere is another heat source for
the troposphere over the Indian Monsoon region. They further reasoned that warmer
Southern Hemisphere summer increases energy storage in the Southern Hemisphere
ocean, and a following colder Southern Hemisphere winter leads to cold air temperature
and creates a large sea-air temperature gradient. This large sea-air temperature gradient
facilitates the latent heat transfer from the ocean to the atmosphere and provides a major
heat source for the monsoon circulation. At obliquity maxima, the Southern Hemisphere
experiences warmer summer and colder winter, which increases the latent heat forcing.
Summer insolation for Northern Hemisphere also peaks at obliquity maxima, which
15

enhances the sensible heating over the Asian continent. Both latent heating from the
Southern Hemisphere and the sensible heating from the Northern Hemisphere work
together to produce the monsoon maxima at obliquity maxima. In the 23 kyr precession
band, hot Southern Hemisphere summer and cold Southern Hemisphere winter occur at
the December perihelion, which is -180° lagging the July perihelion (Northern
Hemisphere summer insolation maxima). In addition, glacial boundary conditions act as
another forcing to the monsoon. The ice minima at -78° , Southern Hemisphere latent
heating at -180° , and the Northern Hemisphere summer insolation at 0° produce the -120°
phase of monsoon maxima at the precession band. Overall, these two theories that
explain the orbital forcing and variability of the monsoon are supported by difference
evidence, but neither could explain all the different and seemingly-opposing observations.
It is evident that there must be flaws in the current understanding of monsoon dynamics.

On millennial timescales, the variability of the monsoon, as recorded in Chinese
speleothems, coincides with the North Atlantic Dansgaard-Oeschger (D-O) events
(Overpeck et al., 1996; Wang et al., 2001). The mechanism that links the monsoon and
the D-O events remains unclear as the lead-lag relationship between the two is
ambiguous. One group views the North Atlantic climate variability as leading the
monsoon. Cooling of the mid-latitude North Atlantic influences climate of the mid-
latitude Eurasia continent through planetary waves or the Arctic Oscillation, resulting in a
cooler Eurasia and a weaker land-sea thermal contrast that is critical for the monsoon
strength (Ganopolski and Rahmstorf, 2002). Also, the fresh water flux during the D-O
16

events slows down the meridional overturning circulation in the North Atlantic (Dickson
et al., 1996). This displaces the Inter-Tropical Convergence Zone (ITCZ) to a southward
position. As the ITCZ is a global phenomenon, rainfall bands over the Asian monsoon
region also shift southward, causing a weakening of the monsoon rainfall over the
continents (Gadgil, 2003). On the contrary, another view is that the monsoon signal leads
the North Atlantic signal. ENSO frequency and amplitude affect the monsoon, with
weaker monsoon co-occurring with El Niñ o or El Niñ o-like conditions (Kumar et al.,
1999). Salinity records from the ENSO-sensitive western Pacific warm pool region
indicate stronger and/or more frequent El Niñ os during Greenland stadials (Stott, 2002).
The signal starts within the ENSO and monsoon regions and then propagates to the North
Atlantic (Clemens, 2006).

On centennial timescales, one most interesting question is how the monsoon responds to
warming and cooling of the global climate. The widely held notion is that stronger solar
output increases monsoon rainfall. This is achieved by two effects. First, insolation
causes larger differential heating between land and ocean because of the difference in
thermal inertia, and this increases the land-sea thermal contrast. Second, more insolation
leads to warming and less snow cover over Eurasia. Less heat is consumed to melt the
snow and more radiative heating occurs due to the snow-albedo feedback. This also
increases the land-sea thermal gradient. This solar forcing hypothesis is bolstered by
speleothem records in China (Zhang et al., 2008) and Oman (Fleitmann et al., 2003),
which show enhanced monsoon during the Medieval Warm Period and weak monsoon
17

during the Little Ice Age. Similarly, sediments from the Arabian Sea suggest an increase
in monsoon winds in the past four centuries as the climate warms (Anderson et al., 2002).

2.1.2. New theories of the Asian Monsoon
Clearly, the traditional view of monsoon as a result of the land-sea thermal gradient is
able to explain some but not all geological and paleoclimate records about monsoon
variability. It certainly does not explain other aspects of the modern monsoon such the
rapid onset of the summer monsoon (Cane, 2010). The land-sea thermal gradient changes
gradually as the land warms in the beginning of the summer, but the wind reversal occurs
rapidly usually within a week over the tropical Indian Ocean and the Indian subcontinent.
Moreover, according to the land-sea thermal gradient theory, the strength of the monsoon
winds should be proportional to the thermal and pressure gradient. However, the
continental thermal low is the strongest in May prior to the arrival of the monsoon rain in
June. It is also observed that in years with weak monsoon rains, the average temperature
of the Indian subcontinent is in fact higher than years with stronger monsoon rains (Cane,
2010). To resolve these conflicts between the long-existing theory and the observations,
new hypotheses have been proposed to explain the dynamics of the monsoon.

Another view of the Asian monsoons is the seasonal migration of the ITCZ in response to
seasonal variation of the latitude of maximum insolation (Gadgil, 2003). The ITCZ in the
Indo-Pacific region is represented by a Continental Monsoon Trough (CMT) centered
over the northern Indian subcontinent, an Oceanic Monsoon Trough (OMT) over the
18

WPWP, and a Trade Wind Trough (TWT) over the western and central tropical Pacific
(Chan and Evans, 2002). The CMT is characterized by a classical monsoonal circulation
during the boreal summer (Webster et al., 1998), with the rising limb of the local Hadley
cell centered over the Indian Monsoon region. In the OMT, the meridional circulation
exhibits a multi-cellular structure. The East Asian summer monsoon represented by this
circulation structure is therefore more complicated than the Indian Summer Monsoon.

Another theory is proposed by Bordoni and Schneider (2008) to explain the rapid onset of
the Indian Summer Monsoon. During spring, the equinox regime of the Hadley
circulation is characterized by two symmetrical cells whose strength is controlled by eddy
momentum fluxes. The Hadley circulation develops into a single cell regime in the
summer and the strength is thermally driven. During the transition, the newly-developed
upper level easterlies shield the cross-equatorial cell from the eddies. The overturning
cell reaches the angular momentum conserving limit, thus accelerating the transition. The
rapid onset of the monsoon is believed to occur as a result of this transition. In their
model simulation, Bordoni and Schneider (2008) showed that surface inhomogeneities
such as the contrast between land and ocean does not play an important role in the
occurrence of the summer monsoon. Instead, the significance of the subtropical
continents is to provide a surface of sufficiently low thermal inertia for the near surface
moist static energy to adjust abruptly, which leads to the rapid strengthening of the single
Hadley cell.

19

In another recent study, Boos and Kuang (2010) explained the monsoon rains as a result
of the orographic insulation by the Himalayas, instead of the heating of the entire Tibetan
Plateau. They pointed out that the traditional view of the Tibetan Plateau as a heat pump
may be able to explain the monsoon wind shift, but not the rainfall. Observations indicate
the upper tropospheric temperature is warmest south of the plateau during boreal summer
instead of right over the plateau. They proposed that the mountain chain at the southern
edge of the plateau insulates warm, moist air over Indian subcontinent from cold, dry
extra-tropical air in the north. The convection of this warm and moist air with high
energy drives the monsoon circulation between the Indian Ocean and the Indian
subcontinent.

2.1.3. Future projections of the monsoon
South and East Asia that is affected by the Indian Monsoon accommodates more than one
third of the world’s population. The agriculture, economy and society across Asia are
critically dependent on the monsoon precipitation. Therefore, how the monsoon has
responded and will respond to global warming is an important question. Since 1850, the
instrumental temperature record documents a general warming trend in the Northern
Hemisphere. It has been argued that this warming trend is unprecedented in the last
millennium (Mann et al., 1999). In the Indo-Pacific region, a 20th century warming trend
is also recorded in climate proxies (Cole et al., 2000; Thompson et al., 2000). Since the
late 19th century, when instrumental records became available, both rainfall over India
and average monsoon wind speed over the Arabian Sea indicate a positive yet weak and
20

insignificant trend (Parthasarathy et al., 1993; Schulz et al., 1998). In the 2007 IPCC 4th
Assessment Report, most global climate models project an intensification of the mean
monsoon rainfall with increased warming during the next century. However, the skill of
the models in simulating present monsoon climate is poor, with a generally cold and wet
bias in all the regions in Asia (IPCC, 2007).

On the other hand, there is evidence that atmospheric circulation in the monsoon region
has weakened in recent decades. Wang (2001) noticed that the monsoon winds weakened
after the late 1970s. By examining tropospheric temperature and the Webster-Yang
monsoon index, Wu (2005) found that the Indian Summer Monsoon has gone through
two weakening processes in the mid-1960s and the late 1970s. Many of these authors
interpreted the transition of monsoon in recent decades as a response to the anthropogenic
greenhouse warming.

The strength of circulation is only one aspect of the monsoon. The amount of monsoonal
precipitation is essentially determined by the interplay between the amount of moisture
transported from the tropical oceans and the strength of the monsoon circulation. An
intensification of monsoon rainfall is attributed to enhanced moisture transport from a
warmer tropical ocean (Hu et al., 2000; May, 2004; Meehl and Arblaster, 2003; Ueda et
al., 2006). As SSTs warm in the tropical Indian and western Pacific oceans there is
enhanced evaporation and subsequently, greater water vapor in the atmosphere. During
the summer monsoon season, more moisture is therefore transported from the tropical
21

oceans to the Asian continent. The strength of the monsoon circulation determines how
far north the monsoon rainfall belts could be pushed by the winds, and is related to more
complicated atmospheric dynamics. In a coupled GCM with quadrupled CO
2

concentration in the atmosphere, precipitation increases over the WPWP with warmer
SSTs, but the rising motion over this region and the eastern Indian Ocean has weakened
(Knutson and Manabe, 1995). In a simple radiative-convective equilibrium model, Betts
and Ridgway (1989) showed how the net mass circulation in the tropics decreases in a
climate with warmer SSTs. The rising motion in the ascending branch of the Walker
circulation is balanced by the subsidence into the convective boundary layer in the
descending branch. The water vapor balance is given as
(

)
Where LH is the surface latent heat flux through evaporation; L is the latent heat of
vaporization; g is the gravitational acceleration, ω is the subsidence at convective
boundary layer top, which equals the convection in the ascending branch; and Δq is the
difference in mixing ratio between the boundary layer and dry air sinking in at the
boundary layer top. Δq is related to temperature, and increases much faster with
temperature than surface evaporation does. Therefore the subsidence term ω decreases
with temperature, so does the rising motion in the ascending branch (Fig. 2.2). These
hypotheses and model simulations regarding the response of monsoon to warming need
to be validated by high-resolution observational records, which is the motivation behind
the studies included in this dissertation.
22

Figure 2.2. Variation of surface latent heat flux, subsidence, and mixing ratio deficit of air sinking into the
boundary layer (Betts and Ridgway, 1989).

2.2. The El Niñ o-Southern Oscillation
Another large climate system that affects the climate and hydrology in the Asian
monsoon region is ENSO. ENSO is the primary atmospheric and oceanic phenomenon in
the tropical Pacific Ocean. In normal conditions, easterly trade winds transport warm sea
surface water from the eastern equatorial Pacific (EEP) to the western equatorial Pacific
(WEP), accumulating warm water in the WPWP. The thermocline, which divides warm
surface water from cold deep water, is deeper in the WEP, and shallower in the EEP. In
the atmosphere, sea level pressure above the warm WEP is lower than over the cold EEP.
This pressure gradient is the driving force of the easterly surface winds which are in turn
responsible for the westward flow of surface water. The lower tropospheric easterly trade
winds, together with the convection over WEP, descending air over EEP, and the upper
23

tropospheric eastward flow, completes the Walker circulation, which is the zonal
atmospheric feature above the equatorial Pacific.

During El Niñ o events, the easterly trade winds weaken, and warm water flows reversely
from the WEP to the EEP, decreasing the tropical Pacific east-west zonal SST gradient,
and deepening the thermocline in the EEP. In the atmosphere, the east-west pressure
gradient decreases, which is responsible for the weakened easterly trade winds. On the
contrary, during La Niñ a conditions, the tropical Pacific east-west zonal SST gradient
enlarges and the thermocline in the WEP deepens, which increases the warm water
accumulation in the WPWP and enhances the atmospheric convection.

Both oceanic and atmospheric indices have been developed to record and describe the
ENSO status over the tropical Pacific Ocean. Rectangular regions are selected from the
eastern to central equatorial Pacific, and their SSTs are monitored and used to construct
the Niñ o SST indices. Positive Niñ o SST anomaly corresponds to warm ENSO phase, the
El Niñ o, and negative SST anomaly indicates cold ENSO phase, the La Niñ a. An
atmospheric index Southern Oscillation Index (SOI) calculates the pressure difference
between Tahiti in the east and Darwin, Australia in the west. Negative SOI anomalies
correspond to El Niñ os.

24

2.2.1. ENSO mechanisms
The relationship between atmospheric circulation and the surface ocean in the tropical
Pacific is described by the Bjerknes feedback (Bjerknes, 1969). Stronger easterly trade
winds accumulate warm water in the WPWP, and cool the EEP, resulting in larger SST
gradient along the equator and thus larger pressure gradient, which further strengthens the
easterly winds and amplifies the SST and pressure gradient. This positive feedback loop
explains how the ENSO warm phase or cold phase sustain themselves but does not
account for the shift between the two phases.

The delayed oscillator theory was postulated by Schopf and Suarez (1988) to explain the
shift between the positive and negative phases of ENSO. The central Pacific shows the
largest atmospheric-oceanic coupled feedback because it is the most SST-sensitive region
of the atmosphere. During an El Niñ o event, the westerly wind stress anomaly in the
central Pacific generates an eastward downwelling Kelvin wave and a westward
upwelling Rossby wave. Kelvin wave propagates fast, brings warm water eastward, and
deepens the thermocline along its way. When the Kelvin wave reaches the eastern
boundary of the ocean basin, the South American continent, it is reflected into a
downwelling Rossby wave which propagates westward. Meanwhile, the upwelling
Rossby wave originally generated in the central Pacific shoals the thermocline in the
western Pacific. When the Rossby wave reaches the eastern boundary of the ocean basin,
it is reflected into an eastward upwelling Kelvin wave. The eastward upwelling Kelvin
wave shoals the thermocline in the central Pacific and reverses the initial warming. About
25

one year is needed to complete this negative feedback cycle, which lags the Bjerknes
positive feedback between SST and air pressure. This negative feedback continues
eroding the development of the El Niñ o in the central Pacific until the westerly wind
anomaly starts to decay and La Niñ a starts to develop.

On the opposite side, during a La Niñ a, the easterly wind stress anomaly in the central
Pacific generates an eastward upwelling Kelvin wave and a westward downwelling
Rossby wave, which act to shoal the thermocline in the eastern Pacific and to deepen the
thermocline in the western Pacific. When these waves reflect off the basin boundaries and
propagate as westward upwelling Rossby wave and eastward downwelling Kelvin wave,
the negative effect tries to shift the La Niñ a conditions into the other phase.

The recharge oscillator (Jin, 1997a, b) is an alternative model to explain the shift between
ENSO warm and cold phases. It is associated with the geostrophic Sverdrup transport.
During an El Niñ o, the high sea surface height in the EEP and the low sea surface height
in the WEP lead to poleward geostrophic flow. The warmth built up in the tropics is thus
dispersed to high latitudes. It takes another several years to recharge the warmth before
another El Niñ o event could take place. To recharge the warmth, a La Niñ a event is
necessary. In contrast to El Niñ o, during La Niñ a, the low sea surface in the EEP and
high sea surface in the WEP lead to equatorward geostrophic transport, recharging the
tropics with heat from higher latitudes.

26

2.2.2. ENSO-monsoon relationship
ENSO is the dominant cause of the interannual variability of the monsoon, with cold
ENSO events favoring stronger monsoon while warm ENSO events associated with
suppressed monsoon strength (Walker, 1918; Webster, 1995; Yasunari, 1990). The
mechanism that governs the negative correlation between ENSO and the monsoonal
circulation is explained as an east-west shift of the Walker circulation (Kumar et al., 1999;
Webster et al., 1998). Under normal, non-El Niñ o conditions, the center of atmospheric
convection associated with the Walker circulation is located over the WPWP. During El
Niñ o events, the convection center shifts eastward with the eastward flow of warm
surface waters. The descending limb of the Walker cell is therefore located over the
Indian Monsoon region. The subsidence creates anomalously high pressure over the
western Pacific-eastern Indian Ocean sector and suppresses precipitation over the Indian
subcontinent and Southeast Asia. However, the relationship between ENSO and the
Indian Monsoon has weakened in recent decades (Kumar et al., 1999; Singhrattna et al.,
2005). The authors suggested that during recent El Niñ o events, the Walker circulation is
centered more eastward, and correspondingly the descending limb is shifted away from
India.

2.2.3. Variability of ENSO
The early Pliocene warm period (4.5 - 3 Ma) is the most recent interval with climate
warmer than today, with global surface temperature 3° C warmer and the atmospheric
CO
2
30% higher than pre-anthropogenic value. Also similar to today are the earth’s
27

continental configuration, ice coverage in the Northern Hemisphere, intensity of the solar
radiation, and ocean circulation patterns. Therefore, the early Pliocene has been widely
studied as an analogue of future anthropogenic warming. SSTs reconstructed from
foraminifera in WEP and EEP sites indicate a smaller east-west SST gradient over the
tropical Pacific Ocean, and a deeper thermocline in the EEP (Wara et al., 2005). These
findings point to permanent El Niñ o-like conditions 4.5 to 3 million years ago (Fedorov
et al., 2006). However, fossil coral evidence from the Philippines does not support the
view of a permanent El Niñ o state, but suggests ENSO behavior during the early Pliocene
similar to present day in spite of the warmer climate in early Pliocene (Watanabe et al.,
2011).

ENSO is found to vary in the glacial-interglacial cycles. Fossil corals indicate weaker
ENSO during glacial than the last interglacial (Tudhope et al., 2001). During glacial, the
significantly decreased equatorial Pacific temperature weakens the coupled ocean-
atmosphere interaction, and thus subdues the ENSO system. ENSO also varies on
precession cycle. Precession modulates how much insolation the earth receives during
different seasons. ENSO grows during Northern Hemisphere summer through autumn,
therefore the changing amount of heating due to precession influences ENSO behavior.

The mid-Holocene suppressed ENSO is another example of the influence of orbital
forcing. A 15 kyr continuous record of deposition events from an alpine lake in Ecuador
indicated weak ENSO variability prior to 7 ka (Rodbell et al., 1999). In mid-Holocene,
28

the greater heating of the equatorial regions during boreal summer has asymmetric
response in the eastern Pacific and western Pacific. Due to the modulation of temperature
by upwelling, EEP warms less than WEP, thus increasing the east-west SST gradient.
This more La Niñ a-like condition inhibits the growth of El Niñ o during boreal summer.
The differential response to warming in the EEP and WEP is simulated by the Zebiak-
Cane ENSO model (Clement et al., 1996), and is termed the thermostat mechanism,
which indicates a La Niñ a-like response to heating of the Pacific basin, and El Niñ o-like
conditions in response to cooling. Lake sedimentation in Ecuador also shows increase in
ENSO occurrence after 7 ka (Moy et al., 2002), which is regarded as the onset of modern
ENSO (Cane, 2005).

ENSO variability in the last millennium is modulated by natural radiative forcing
including solar and volcanic forcing (Emile-Geay et al., 2007; Emile-Geay et al., 2008).
In agreement with the thermostat mechanism, both paleoclimate reconstructions and
model results suggest higher probability of El Niñ o event occurs in the winter following a
volcanic eruption, especially large volcanic eruptions in the tropics. Insolation also
correlates well with ENSO index (Mann et al., 2005). However, it is still not clear how
the amplitude and frequency of ENSO events have varied in different climate
backgrounds of the past millennium such as the Medieval Warm Period and the Little Ice
Age (Cobb et al., 2003; Yan et al., 2011). Some GCM simulations seem to disagree with
the thermostat mechanism and indicate weakened Walker circulation in a warming
scenario (Held and Soden, 2006; Vecchi et al., 2006). Needless to say, efforts from
29

climate reconstructions using proxy records are required in order to obtain high-
resolution information about past variability of ENSO which could be used to calibrate
the physics of climate models.

30

Chapter Three

Methodology: Oxygen Isotopes in Precipitation and Tree
Cellulose

Summary
In this dissertation, oxygen isotopes are used as a tracer in the hydrological cycle. The
two major isotopes of oxygen, H
16
O and H
18
O as in water molecules, are differentiated
during phase changes due to their mass difference. This isotope fractionation results in
different isotopic composition between the liquid and vapor phase of water. And because
the fractionation factor is temperature dependent and is also related to large dynamic
processes, the oxygen isotopic composition, i.e. the relative abundance of H
16
O versus
H
18
O, of precipitation is found to exhibit a positive correlation with temperature in high-
latitude regions (Dansgaard, 1964) and a negative correlation with the amount of
precipitation in low-latitude tropical regions (Araguas-Araguas et al., 1998). These
empirical relationships are validated by physical models and are widely used as the
theoretical basis for paleoclimate reconstructions. As the isotopic composition of
precipitation is transmitted to natural archives such as ice cores, speleothems, and plant
tissues (leaf wax and xylem cellulose, etc.), the studies of these terrestrial proxies have
been conducted extensively to reconstruct climatic and hydrological conditions on a
variety of timescales. This dissertation primarily uses the oxygen isotopic composition of
tree xylem cellulose. In the following, I will discuss the isotope effects in precipitation
oxygen isotopes, as well as the processes during which the isotope signatures of
31

precipitation are transmitted to the cellulose of trees. The δ notation is used to denote the
oxygen isotopic composition, which is defined as the relative difference of
18
O/
16
O with
respect to a standard sample, in our case the Vienna Standard Mean Ocean Water
(VSMOW)
δ

(

(

)

(

)

)

‰

3.1. Oxygen isotopes in precipitation
3.1.1. Temperature effect
In high-latitude and high-elevation regions, the δ
18
O in precipitation exhibit a positive
relationship with temperature (Dansgaard, 1964). This is explained as the temperature
dependence of equilibrium isotopic fractionation during condensation. The vapor
pressure of lighter water molecules (H
2
16
O) is higher than that of heavier water molecules
(H
2
18
O). Therefore, when water condenses in clouds, heavier isotopologues are
preferentially removed to form water droplets, leaving the remaining water vapor in the
clouds isotopically depleted (more negative δ
18
O). This equilibrium fractionation
between water vapor and condensate is related to temperature through the following
equation (Majoube, 1971)

⁄

⁄
This equation is valid for temperatures ranging from 273.15 to 373.15 K. The
fractionation factor increases with decreasing temperature, so the removal of heavier
isotopologues is more efficient at colder temperatures, resulting in more isotopically
32

depleted water vapor remaining in the clouds, and the subsequent rainfall is more
depleted in δ
18
O as well. A global correlation between mean annual surface air
temperature and δ
18
O of meteoric precipitation has long been recognized (Dansgaard,
1964) and is described as

The temperature effect is largest and most linear at high latitudes and high altitudes,
especially where condensation occurs near the land surface, whereas in the tropics,
because temperature variation is small, an amount effect dominates.

3.1.2. Amount effect
The amount effect depicts a negative relationship between the δ
18
O of precipitation and
the amount of precipitation in the tropics and the monsoon region (Araguas-Araguas et al.,
1998). When water evaporates from the surface ocean, a kinetic isotope fractionation
controls the water isotope distribution. The lighter isotopologues preferentially enters the
vapor phase, leading to isotopically depleted water vapor with respect to the ocean
surface water. Condensation in an open system is described by Rayleigh fractionation.

where R is the isotopic ratio of the remaining water vapor, R
i
is the initial isotopic ratio
of the water vapor, F is the fraction of water vapor remaining, and α is the equilibrium
fractionation factor. Fractionation occurs when the condensed liquid water is at
equilibrium with the remaining water vapor, and the condensate is immediately removed
from the system to avoid any back exchange with the water vapor. As more water
33

precipitates out, the remaining water vapor becomes more isotopically depleted, thus the
subsequent precipitation is also more depleted. The equilibrium fractionation factor is
also controlled by temperature, as described in the previous section, but the small
temperature variation in the tropics minimizes the temperature effect.

Figure 3.1. The first EOF mode of a) IsoGSM simulated precipitation δ
18
O and b) CMAP precipitation
over Southeast Asia (0-30 ° N, 90-120 ° E) and their correponding PCs, c) the standardized monthly
anomaly of the first PCs of the precipitation (blue) and the precipitation δ
18
O (red), and d) the twelve
month moving averages. The first modes explain 23% and 20% of the total variance, respectively, of the
precipitation δ
18
O and the precipitation. The negative correlation between the two (R = -0.59) reveals the
precipitation amount effect.

A further fractionation can occur after the rain droplets leave the cloud (Bony et al., 2008;
Risi et al., 2008). The rain droplets falling through a dry atmosphere begins to evaporate
and isotopic fractionation occurs at the surface of the droplets. During less intense rainfall,
34

the relative humidity is lower, so the rain droplets falling through the atmosphere is
subject to more evaporation and their resulting isotopic composition is more enriched in
heavier isotopes. Moreover, smaller droplets have larger surface to volume ratio than
larger droplets and this also enhances evaporation. Both effects tend to cause isotopically
enriched rainwater if the rainfall event is less intense.

A number of other recent studies have provided new interpretations of the amount effect
(Kurita et al., 2009; Lee and Swann, 2010; Pausata et al., 2011). These new
interpretations view the isotope amount effect as a regional phenomenon instead of a
local effect. The precipitation δ
18
O at a site is related to the precipitation amount over a
larger region, a region that could be geographically distant from the precipitation site but
that serves as the moisture source. This new idea is supported by studies included in the
dissertation and will be discussed further in the following chapters.

Overall, in the tropics the reverse correlation between precipitation δ
18
O and precipitation
amount is a robust signal. In this dissertation, the Asian monsoon region is of interest. An
Empirical Orthogonal Function (EOF) analysis has been conducted for the observed
precipitation amount (CPC Merged Analysis of Precipitation) and a model simulated
precipitation δ
18
O product IsoGSM (Yoshimura et al., 2008) in Southeast Asia. The first
principle components of both precipitation amount and precipitation δ
18
O display a strong
negative correlation with each other, illustrating the amount effect in the tropical
monsoon region (Fig. 3.1).
35

3.2. Oxygen isotopes in tree cellulose
The instrumental records of precipitation and the isotopic composition of precipitation
are spatially sparse and temporally limited. To extend our current understanding of water
isotope behaviors and their relation to atmospheric dynamics, water isotope records are
developed from natural archives such as tree ring cellulose. In the past few decades,
isotope fractionation models have been developed for plant tissues (Craig and Gorden,
1965; Farquhar and Lloyd, 1993; Roden et al., 2000) and have been used as guidance in
the development of proxy records using plant tissues. In the following, a review is
provided for the incorporation of oxygen isotopes in the synthesis of tree ring cellulose.

Two major reactants involved in photosynthesis are water and carbon dioxide. Plants take
up water from soil through their root system, and breathe in carbon dioxide through
stomata that are located in the leaves. Both H
2
O and CO
2
contribute oxygen to the
products of photosynthesis, but the oxygen originating from CO
2
undergoes complete
isotopic exchange with tree H
2
O before carbohydrate synthesis (Deniro and Epstein,
1979). Therefore, the oxygen isotopic composition of tree ring cellulose is primarily
representative of the source water isotopic signature. After taken up by roots, the source
water (xylem water) is transported to the leaves, where it is consumed to produce sucrose
during photosynthesis. The sucrose is then exported down the trunk to sites of cellulose
formation. Each of these steps is discussed in detail below in terms of isotope
fractionation.
36

3.2.1. Evaporative isotopic enrichment
There is no isotope fractionation when soil water is taken up by the roots. However,
evaporation at the leaf-atmospheric interface enriches the oxygen isotopic composition of
leaf water that will be available for photosynthesis. The leaf water evaporation is related
to humidity of the ambient environment and leaf boundary conditions. The following
equation describes the leaf water evaporative enrichment (Craig and Gorden, 1965)

(

)
where the subscripts e, s, and a stand for the leaf water at evaporative sites, source water
and water vapor in the atmosphere, respectively; ε
e
o
and ε
k
o
are the equilibrium and
kinetic fractionation factors for water liquid-vapor phase transition; e
a
/e
i
is the ratio of
ambient vapor pressure to intercellular vapor pressure, which varies primarily in response
to differences in temperature within the leaf and ambient atmosphere.

As it is difficult to obtain information for all the factors, assumptions are usually made
when applying this model to tree cellulose isotope studies. These assumptions include
leaf surface maintaining a temperature similar to the ambient air temperature, and
atmospheric water vapor being at isotopic equilibrium with soil moisture. The first
assumption allows the substitute of the term e
a
/e
i
with relative humidity term h, and the
second assumption gives

37

which simplifies the equation for the isotopic composition of the portion of leaf water at
evaporative sites to

( )(

)
The temperature dependence of the equilibrium fractionation of oxygen isotopes in liquid
water and water vapor have been well established empirically. The most reliable
relationship was given by Majoube (1971) and the equations were validated by recent
determinations (Horita and Wesolowski, 1994). To calculate the equilibrium fractionation
factor for
18
O,

⁄

⁄
where the units of ε
e
o
is per mil (‰), and T is in K. This equation is valid for temperature
ranging from 273.15 to 373.15 K.

The kinetic fractionation between liquid water and water vapor arises from the fact that
water molecule with the lighter oxygen isotope
16
O diffuses more slowly in air than water
molecule with
18
O. The ratio of the diffusivities is 1.028, resulting in a kinetic
fractionation factor of 28‰ (Merlivat, 1978). However, the kinetic fractionation at the
leaf surface is also a function of the air flow dynamics in the leaf boundary layer, which
is controlled by the leaf size and morphology (Buhay et al., 1996). For dissected needles
of pine trees, which are the tree types in all the studies of this dissertation, we assume a
static boundary layer and a kinetic fractionation of 28‰ for δ
18
O (Aucour et al., 1996).

38

3.2.2. Peclé t effect
Many measurements have been made and show that the observed leaf water oxygen
isotopic composition is less enriched than that predicted by the Craig and Gorden model
(Cuntz et al., 2007). This overestimation is explained by a Peclé t effect (Farquhar and
Lloyd, 1993). The bulk leaf water represents a combination of different compartments,
which have different oxygen isotopic compositions. The water at evaporative sites is
more enriched than water in other parts of the mesophyll, which still has the signature of
the source water. The bulk leaf water isotopic composition (δ
18
O
l
) is thus predicted by

( )

The fraction of leaf water that is subject to evaporation (f) is determined by the Peclé t
number (ρ)

and

where T is the rate of transpiration; L is the effective mixing length in the leaf; C is the
molar concentration of water; and D is the diffusivity of H
2
18
O in water. Peclé t number
characterizes the relative importance of advection of depleted source water from the
xylem to the evaporative sites and the back-diffusion of the enriched water at the
evaporative sites to the xylem.

39

Although Peclé t number quantifies the fraction of leaf water subject to evaporation, it is
difficult to estimate the rate of transpiration and the effective mixing length in the leaf.
Leaney et al. (1985) and Allison et al. (1985) studied C3 and C4 dicotyledons and
monocotyledons and estimated to range between 70% and 80% to best fit their
experimental data. Roden et al. (2000) found a higher proportion (90%) for alder, birch
and cottonwood.

3.2.3. Biochemical fractionation
When sucrose is formed in the leaf chloroplasts, it reflects the leaf water signature with a
biochemical autotrophic fractionation factor (ε
a
o
). The responsible mechanism is the
equilibrium exchange of oxygen in CO
2
and H
2
O with ambient water during carbohydrate
synthesis. The carbohydrate product is 27‰ more enriched in δ
18
O than the leaf water
(Epstein et al., 1977). Sucrose is then transported down the trunk to form cellulose. No
isotopic fractionation occurs during the formation of cellulose from sucrose.

3.2.4. Exchange with xylem water
Although there is no fractionation between sucrose and cellulose, exchange of oxygen
atoms in sucrose with xylem water occurs during the transport of sucrose. Xylem water is
the water taken up by the roots before leaf enrichment happens, thus it carries the same
isotopic composition as the source water. Cellulose formation in the stem involves a
heterotrophic fractionation (ε
h
o
), which has a value of 27‰, the same as the autotrophic
40

fractionation (Roden et al., 2000). The oxygen isotopic composition of cellulose (δ
18
O
c
)
is thus given by

(

) (

)

The fraction of sucrose oxygen that undergoes exchange with xylem water during
cellulose synthesis (
o
) is an important term in describing the isotopic behavior of
cellulose. Various experimental studies have been conducted to determine this fraction.
Yakir and Deniro (1990) reported that 35% of oxygen atoms exchange with xylem water
for the fern Lemna growing under heterotrophic conditions in the dark. Luo and
Sternberg (1992) studied germinating seeds and found this fraction to be 34% for
cellulose formed from starch. Roden et al. (2000) studied alder, birch and cottonwood in
both greenhouse experiments and field studies, and estimated the fraction of oxygen
exchanged during cellulose synthesis as 42%.

Combining all the equations, we can derive an expression for the isotopic composition of
cellulose

(

)

(

)( )(

)
For oxygen, ε
h
o
= ε
a
o
= 27‰, therefore the above equation can be simplified to:

(

) (

)( )(

)

The first term on the right side of the equation describes the influence of source water on
cellulose oxygen isotopic composition, and the second term represents the leaf
41

enrichment. High relative humidity (h) minimizes the evaporative enrichment of leaf
water δ
18
O (the second term), and thus source water δ
18
O dominates the δ
18
O in the final
product cellulose. Low relative humidity enhances the leaf enrichment, forming cellulose
with high δ
18
O. In the following chapters, the isotopic composition of the source water
and the relative humidity are viewed as the two primary influencing factors for the
isotopic composition of tree cellulose. The signal of source water δ
18
O is fully transferred
into cellulose δ
18
O, i.e. a 1:1 relationship. The sensitivity of cellulose δ
18
O to relative
humidity is ~0.2‰/%, by choosing a value of 70% for f (Allison et al., 1985; Leaney et
al., 1985) and 42% for ϕ
o
(Roden et al., 2000). During rainy months at tropical forest sites,
the relative humidity is considered to be high and with little variance, therefore the δ
18
O
values of cellulose could be used as a surrogate for source water δ
18
O. By selecting trees
growing in shallow soil with permeable base rock where rainfall drains fast, the source
water in soil could approximately represent the simultaneous rain water. It is based on the
above reasoning and assumptions the studies in the following chapters were carried out.

42

Chapter Four

20th Century Seasonal Moisture Balance in Southeast Asian
Montane Forests

Summary
Tropical montane forests are among the most biologically diverse terrestrial ecosystems.
In Southeast Asia, montane forests sustain regular stream flow and stable ecosystem
despite large seasonal variations in water availability because the trees and their root
systems act as moisture catchments, absorbing significant amounts of water during the
wet season and recycling this moisture during the dry season. In this regard, the monsoon
cycle is an inherent mechanistic component to these complex ecosystems. It is also clear
from historic records and from tree-ring reconstructions that more sustained periods of
reduced moisture such as those occurring during El Niñ o can disrupt and harm natural
ecosystem. At present there are large uncertainties in climate model projections of
monsoon response to increasing radiative forcing. In this study we take a retrospective
approach to investigate the hydroclimate of Southeast Asia during the 20th century as the
atmosphere has warmed. The seasonally varying moisture balance in Southeast Asia is
reconstructed from records of oxygen isotopic composition (δ
18
O) of subannual tree
cellulose samples extracted from pine trees that grew in Doi Chiang Dao, a limestone
mountain in northern Thailand. At this location the δ
18
O of tree cellulose exhibits
distinctive annual cycles of up to 12‰, which is a reflection of the seasonally distinct
isotopic composition of the soil moisture. The annual mean cellulose δ
18
O correlates
43

negatively with the strength of the summer monsoon, and its interannual variability,
which is dominated by ENSO. However, the relationship with ENSO appears to weaken
after 1980. The annual cellulose δ
18
O maxima values, which represent the dry season soil
moisture δ
18
O, have declined progressively during the 20th century by about 3.5‰. We
interpret this to reflect a change in the isotopically distinct fog water input to the dry
season soil moisture in response to rising temperature as well as deforestation.

4.1. Introduction
In Southeast Asia, the montane forests play an important role in the annual water cycle.
During the summer wet season the root systems of trees take-up significant amounts of
monsoon rainfall from the soil and store it, reducing the potential for floods and erosion.
The moisture stored in the forests is then released in the dry season and this helps
maintain regular stream flow and provides water to the agriculture until the next wet
season. In this way, the forests operate as modulator of the hydrological imbalance that
characterizes the monsoon wet-dry cycle (Bruijnzeel, 2002; Bubb et al., 2004; Walker,
2003). At elevations between 1200 and 2500m these forests are particularly important
because they are frequently shrouded in mountain fog (Stadtmü ller, 1987). The trees at
these elevations have the ability to capture fog/cloud condensate through the canopy
(Bruijnzeel, 2002; Bruijnzeel, 2004; Bruijnzeel et al., 2005; Bruijnzeel and Veneklaas,
1998; Bubb et al., 2004), which helps ameliorate plant moisture stress particularly during
the dry season. Moreover, tropical montane cloud forests host a vast array of animal
species and marked endemism (Bubb et al., 2004; Foster, 2001). Therefore, a change to
44

the regional climate could impose significant stress on both the ecology of the local
forests as well as the agricultural system that lies downstream within the lowlands. For
example, the severe drought in 2010 in Thailand and Vietnam that accompanied El Niñ o
led to a significant drop in the rice production. Events of this kind have severe
consequences to the growing population in Southeast Asia and thus, understanding how
the climate and particularly the frequency and severity of ENSO-induced drought may
change in the future is of utmost importance.

Some Global Climate Model (GCM) simulations project an intensified summer monsoon
with an enhanced moisture cycle within the tropics as SSTs warm (Hu et al., 2000; May,
2004; Meehl and Arblaster, 2003; Ueda et al., 2006). In addition, more moisture in the
atmosphere could decrease the adiabatic lapse rate, amplifying the tropospheric warming
at higher altitudes (Diaz and Graham, 1996). Importantly, this would raise the lifting
condensation level (LCL), and inhibit orographic cloud/fog formation over much of the
tropical mountains of Southeast Asia (Pounds et al., 1999; Still et al., 1999). A higher
cloud base may also result from deforestation and/or conversion of forest to pasture or
cropland in nearby tropical lowlands, due to a reduction in overall evapotranspiration and
decreased moisture content of the air masses flowing up the regional mountain slopes
(Lawton et al., 2001; Ray et al., 2006). A decrease in fog/cloud cover is especially critical
in Southeast Asia during the dry season, when rainfall is minimal and fog water is the
primary source of soil moisture. Reduced fog would increase evapotranspiration, and lead
to an even larger moisture deficit during the dry season.
45

To evaluate whether these changes are occurring in the tropical montane forests, a
network of long term climate records is needed. Unfortunately, limited instrumental data
is available from these parts of the tropics and there is a particular lack of in situ
meteorological measurements within the montane forest regions that prevents a direct
assessment of ongoing changes to the water cycle. On the other hand, the trees growing
in the forests are themselves potential archives of information about natural hydroclimate
variability. The width of tree rings, for example, reflects the environmental conditions
during the growth season and has been used to reconstruct temperature and drought index
back to hundreds of years (Buckley et al., 1995; Sano et al., 2009). The oxygen isotopic
composition (δ
18
O) of tree cellulose is a potentially much more resolvable indicator of
hydrologic variability than are tree ring widths. This is because the isotope composition
of tree cellulose is a direct reflection of the isotopic composition of soil moisture and the
relative humidity within the local environment (Deniro and Epstein, 1979; Roden et al.,
2000; Sternberg, 2009). In tropical monsoon regions where there is strong seasonality,
soil moisture is isotopically depleted during the wet season due to the isotope amount
effect, and the moisture available in the dry season is characteristically more isotopically
enriched (Araguas-Araguas et al., 1998). By analyzing the isotopic composition of
cellulose taken at subannual resolution from individual rings these isotopic differences
can potentially be used to fingerprint how the hydroclimate in each seasons varied in the
past (Anchukaitis and Evans, 2010; Anchukaitis et al., 2008; Poussart et al., 2004;
Poussart and Schrag, 2005; Roden et al., 2009). The isotopic seasonal signal may be
46

resolvable from subannual sections or samples taken from an annual tree ring. It is this
potential signal that we set out to investigate in the present study.

We investigate how the moisture balance in the tropical montane forest of monsoonal
Southeast Asia has responded to warming through the 20th century by analyzing
cellulose δ
18
O of evergreen trees from a tropical montane forest of northern Thailand.
The trees grow at an elevation of ~1500 m. At this elevation the trees and the moisture
balance are sensitive to shifts in the cloud base level as well as to changing amounts of
summer monsoon precipitation. With high-resolution, subannual sampling and
measurements of cellulose from individual tree rings we are able to reconstruct the soil
moisture and other environmental conditions for both the monsoon rainy season and the
dry season. We then calibrate the isotope measurements with instrumental climate
records and interpret the results in terms of moisture availability in this montane forest
during different seasons.

4.2. Materials and Methods
4.2.1. Study site
Doi Chiang Dao (19°24’N, 98°54’E), Thailand’s third highest mountain, is located in the
northern province of Chiang Mai (Fig. 4.1a). It is a limestone massif sitting on an almost
flat alluvial plain. The highest peak is 2225 meters above sea level. Our core samples
were taken from Pinus kesiya at about 1500 m altitude in the moist lower montane
evergreen forest where the humidity is high (Smitinand, 1966). P. kesiya grows
throughout the lower montane pine-oak forests of northern Thailand, best developed on
47

ridges and moderate to steep slopes at 1000 to 1400 m, with the highest occurrence at
1800 m (Santisuk, 1988). Above 1800-1900 m, there is a prevailing mist belt with
persistent cloud/fog cover (Santisuk, 1988). Between 1800 and 1200m there can be
incipient and intermittent cloud formation (Bruijnzeel, 2002).

Figure 4.1. a) A hill shade map of Mainland Southeast Asia, created from 90m digital elevation data
(Jarvis et al. 2008). b) Climatology of five-day mean precipitation and temperature from the nearest
meteorological station Chiang Mai, calculated from daily observations from 1951 to 2006.

The climate of northern Thailand is monsoonal. The nearest meteorological station is
located in Chiang Mai, which is ~70 km from the tree site. The tree site and station are
influenced by three distinct hydrological seasons (Fig. 4.1b). November to February is
48

the cool dry season. March and April are the hottest months. May marks the onset of the
monsoon rainy season, which lasts until October. During the summer rainy season, there
are typically two periods of high rainfall, a smaller rainfall peak in May-June, and a
larger peak from July to mid-October, which are the expression of the south-north
movement of the ITCZ (Singhrattna et al., 2005).

4.2.2. Tree ring sampling and processing
The growth pattern of P. kesiya is closely related to moisture availability. By monitoring
the cambial activity on a monthly basis for a year in northern Thailand, Pumijumnong
and Wanyaphet (2006) found that these trees grew rapidly during the rainy season May to
October, whereas the cambial activity declined gradually as the dry season commenced in
November, and became dormant until March-April. This growth pattern causes a
formation of a sharp ring boundary during the dormant season, which is different from
most tropical trees that do not develop visible ring structures and makes this species a
better choice for dendrochronology studies.

Six cores from six different trees were analyzed in this study. All cores were around 100
years old, but only from the 1920s to 2000 were precisely dated. Cross-dating took place
in the Tree Ring Lab at Lamont-Doherty Earth Observatory. For this study each core was
sectioned subannually using a microtome under a microscope. Slices were typically at 35
μm intervals, and every 3 full slices were combined into a 2 ml polypropylene centrifuge
tube for cellulose extraction. In this manner, up to 20 samples could be generated from a
49

single ring. Alpha-cellulose was extracted from whole wood samples using a modified
Brendel method (Gaudinski et al., 2005). Each cellulose sample used for isotopic
measurement was weighed and wrapped in silver capsules and loaded into a Thermo
Finnigan TC/EA for pyrolysis at 1420º C. The CO product was then transferred online to
a Delta V Advantage isotope ratio mass spectrometer via a purified He stream. The
isotope ratio (C
18
O/C
16
O) of each sample was measured and compared to a high purity
CO standard. The sample C
18
O/C
16
O values are reported in standard δ notation with
respect to vSMOW. Two standards were analyzed along with the samples, IAEA
cellulose and sucrose standard (e.g. two standards with every twelve tree cellulose
samples). Over the course of this study the analytical precision of the standards is smaller
than 0.3‰.

4.2.3. δ
18
O in tree cellulose
The δ
18
O of tree cellulose is primarily influenced by the δ
18
O of the soil water taken up
by tree roots and the humidity of the ambient environment during the growth season
(Roden et al., 2000; Sternberg, 2009). The trees used in this study grow on highly
permeable limestone ridges with thin soils with little or no storage capacity.
Consequently, these trees utilize mostly precipitation instead of groundwater. During the
summer season heavy monsoon rainfall is the primary source of soil moisture. The
monsoon rainfall has a characteristically depleted δ
18
O composition that varies with the
amount of precipitation (Araguas-Araguas et al., 1998). During the dry season fog/cloud
deposition within the tropical montane cloud forests is estimated to account for 15-100%
50

of total precipitation (Bruijnzeel and Proctor, 1995). Fog/cloud water is isotopically more
enriched relative to rain water (Gonfiantini and Longinelli, 1962; Ingraham and Mark,
2000; Ingraham and Matthews, 1988, 1990; Scholl et al., 2007). The influence of
monsoon rainfall vs. fog moisture on tree cellulose is therefore discernable from trees that
typically flux soil moisture rapidly and produce cellulose throughout the year, which is
the case for P. kesyia.

4.3. Results
4.3.1. Cellulose δ
18
O overview
The subannual δ
18
O values of cellulose from six tree cores for the period AD 1922 to
2000 are illustrated in Figure 4.2. Each annual ring is characterized by a distinct δ
18
O
maximum near the ring boundary, where the growth stops as the dry season begins, and a
δ
18
O minimum in the middle portion of the ring. The intraannual isotope values vary by
up to 12‰, with an average annual cycle of ~5‰. Larger amplitudes of the annual cycle,
i.e. higher δ
18
O maxima and lower δ
18
O minima, is observed prior to the mid-1930s and
in the mid- to late 1950s, although the interval after 1980 needs to be viewed with caution,
because the rings were too narrow to yield a large number of subannual samples. The
δ
18
O from different cores are similar. Cores DCK12A and DCK08A have the longest
chronologies and were growing approximately 1 km apart. Their annually averaged δ
18
O
are correlated at 0.45 (p<0.001).
51

Figure 4.2. a) Subannual cellulose δ
18
O measurements from six different tree cores and b) a close-up.

4.3.2. Seasonal cycle
To compare the cellulosic δ
18
O records to the δ
18
O of precipitation, we first examined the
GNIP record from Bangkok, which is located in the coastal lowlands of central-southern
Thailand. Because of its distance from the tree site, different topography and climatology,
the Bangkok GNIP data do not compare well with our tree δ
18
O record. We therefore turn
to an isotope-enabled GCM IsoGSM. IsoGSM is a gridded global rainwater isotopic
52

composition simulation developed by Yoshimura et al. (2008). The simulation is
accomplished by incorporating processes of the stable oxygen isotopes into an
atmospheric GCM and by applying a spectral nudging technique toward reanalysis
dynamical fields. The published data are available from 1979 to 2008. The monthly
precipitation δ
18
O in the grid point nearest to Bangkok has a correlation coefficient of 0.6
with the Bangkok GNIP data, providing confidence in IsoGSM as a substitute for
instrumental data.

Figure 4.3. a) A scatter plot of the cellulose δ
18
O seasonal cycle from all the annual rings of all cores.
Horizontal axis represents the fractional distance from the previous ring boundary. Anomalies are taken by
subtracting annual means from the raw δ
18
O values to get rid of the interannual variation. A third order
polynomial fit shows the average annual cycle is ~5‰. b) A scatter plot of the monthly IsoGSM
precipitation δ
18
O anomalies for the nearest grid point (20 ° N, 99.375 ° E). The anomalies are taken in the
same fashion as in a.

We calculated δ
18
O anomalies for each annual ring (raw value minus annual mean).
These results are presented as a scatter plot for all the rings. The average amplitude of the
annual cycle is ~5‰ (Fig. 4.3a). The monthly IsoGSM precipitation δ
18
O values for the
nearest grid point were also converted to subannual anomalies for comparison. The most
53

depleted precipitation δ
18
O occurs around August-September, whereas the dry season
from November to April is characterized by the most isotopically enriched precipitation.
The amplitude of the precipitation δ
18
O variation for the growth season from May at the
beginning of the wet season to November, the beginning of the dry season, is ~5‰.

Figure 4.4. The cellulose δ
18
O annual maxima values near tree ring boundaries are singled out and
averaged among all the cores to construct an annual timeseries. Annual minima and annual mean

are
constructed in similar fashion.

Although relative humidity is another major factor that can influence the δ
18
O of
cellulose, there are no measurements of relative humidity available for our montane
forest site. Meteorological stations are usually located in urban areas, and are not
representative of the actual forest environment. A study at another montane forest
location in northern Thailand showed that at an elevation of about 1500m the relative
54

humidity remains above 90% for most of the year, and is frequently 100% if there is
cloud contact (Wolseley and AguirreHudson, 1997). Based on the cellulose isotope
model (Roden et al., 2000), the sensitivity of cellulose δ
18
O to relative humidity is about -
0.2‰/%. If we assume the humidity difference throughout a growth season can induce an
additional ~2‰ of variability to the annual cellulose δ
18
O cycle, the combined effect of
both precipitation δ
18
O and relative humidity would lead to a ~7‰ average annual cycle.
This is larger than the ~5‰ observed in the cellulose δ
18
O measurements and possibly
suggests the seasonal variations in relative humidity are typically smaller than this. There
may also be some mixing in the soil moisture that contributes to the smaller average
amplitude of the cellulose δ
18
O annual cycle.

4.3.3. Interannual variability
The annual δ
18
O mean, maxima, and minima values of each core were calculated and
then averaged for all cores in order to derive annual timeseries for this site (Fig. 4.4). We
find these δ
18
O indices do not correlate well with ring width indices derived from these
trees. The annual δ
18
O mean values represent the cellulose isotopic composition
integrated over the whole growth season. They show no long term trend but do exhibit
smaller interannual variability during the 1940s and 1950s compared with other decades.
The annual δ
18
O mean values correlate negatively with local and regional rainfall
amounts, as well as Webster-Yang monsoon index. The details of the correlation
coefficients are listed in Table 4.1. The strongest correlations are found with August-
September-October (ASO) Global Precipitation Climatology Center (GPCC) area-
55

weighted average rainfall of Mainland Southeast Asia (R=-0.44, p<0.001) and for July-
August-September (JAS) All India Rainfall (AIR) (R=-0.46, p<0.001). The correlation
between cellulose δ
18
O and seasonal rainfall is attributed to the so-called isotope amount
effect, where higher amounts of precipitation lead to more isotopically depleted rainwater.
The interannual variability observed in the annual δ
18
O mean values is also correlated
with ENSO. Positive ENSO events are typically characterized by a rainfall deficit and
thus enriched isotopic composition of soil moisture that is transmitted to the tree cellulose,
and vice versa. The annual mean cellulose δ
18
O correlates significantly with the
September to November (SON) Niñ o4 SST index (R=0.47, p<0.001), and this ENSO
pattern is shown in field correlations with SSTs and Sea Level Pressures (Fig. 4.5).

The interannual variability in the annual δ
18
O minima mimics that of the annual δ
18
O
mean. The two correlate at 0.7. The high degree of correlation between the annual
minima and the annual mean values is interpreted to reflect the fact that the isotopic
composition of the soil moisture is integrated over an entire growth season and is largely
determined by the amount of precipitation occurring during the rainiest months. However,
the annual δ
18
O minima is found to have no good correlation with any of the available
instrumental climate data except for a weak correlation with the amount of precipitation
during July to October at the nearest GPCC grid point (R=-0.29, p=0.009). We believe
the lack of correlation over this period is due to the fact that the rings were too narrow to
section at a sufficient resolution to resolve the large seasonal contrasts in δ
18
O, in
particular the interval after 1980.
56

Table 4.1. Correlation coefficients and p-values between Doi Chiang Dao cellulose δ
18
O annual mean and
the following: Doi Chiang Dao precipitation, represented by the nearest grid point (19.25 ° N, 98.75 ° E) of
GPCC V4 0.5 degree precipitation (Rudolf et al., 2003); Mainland Southeast Asia (MSEA) precipitation,
an area-weighted GPCC precipitation over the region of 10-25 ° N, 95-110 ° E; and All India Rainfall (AIR)
(Parthasarathy et al., 1993). In bold are the strongest correlations.

correlation
coefficient
Doi Chiang Dao
precipitation
MSEA precipitation AIR
Annual -0.26 -0.16 -0.21
MJJASO -0.30 -0.21 -0.30
JJAS -0.30 -0.13 -0.40
JAS -0.32 -0.18 -0.46
JASO -0.38 -0.37 -0.37
ASO -0.32 -0.44 -0.36
JASON -0.39 -0.43 -0.33

p-value
Doi Chiang Dao
precipitation
MSEA precipitation AIR
Annual 0.021 0.158 0.058
MJJASO 0.007 0.057 0.008
JJAS 0.007 0.267 0.000
JAS 0.004 0.106 0.000
JASO 0.000 0.001 0.001
ASO 0.004 0.000 0.001
JASON 0.000 0.000 0.003

The annual δ
18
O maxima, which represents the higher δ
18
O values of moisture during the
dry season, exhibit different interannual variability compared to the annual mean and the
annual minima δ
18
O (Fig. 4.4). We find no good correlation between the annual δ
18
O
maxima and instrumental precipitation or temperature data. It is possible that this lack of
correlation is due to local environmental conditions including fog/cloud interception and
possibly different temperature and humidity conditions in the forest relative to the
lowland urban areas where most meteorological stations are located. We do note a
progressive decreasing trend in the δ
18
O maxima values (Fig. 4.4). In the following
section we explore a possible explanation for this trend that would result from varying
57

fog moisture deposition in the dry season as recognized in other tropical montane forests
as well (Hutley et al., 1997; Kittredge, 1948; Scholl et al., 2007).

Figure 4.5. Spatial correlation between the timeseries of Doi Chiang Dao annual mean cellulose δ
18
O
values and the field of September to November a) HadISST (Rayner et al., 2003) and b) HadSLP (Allan
and Ansell, 2006). Only correlations higher than 90% significance level are shown.

4.4. Discussion
4.4.1. Comparison with an earlier study
In another study of tree cellulose oxygen isotopes at Pangmapa in northern Thailand
(~100 km to the west of Doi Chiang Dao), Poussart and Schrag (2005) documented
intraannual cycles that are smaller than those at our site on Doi Chiang Dao. The
interannual δ
18
O variability at Pangmapa is also different, and their δ
18
O values are
generally more enriched than ours at Doi Chiang Dao. These differences could possibly
be attributed to differing physiological responses or to lower resolution samples in the
Pangmapa trees. The Pangmapa trees are broadleaf species Quercus kerrii and Meliusa
velutina with no visible rings, whereas trees in the current study are evergreen pines with
clear ring structures. Local influences such as relative humidity may also contribute to the
58

differences. Our trees are from a montane forest at relatively high elevation, where the
high humidity inhibits the isotopic enrichment associated with leaf water
evapotranspiration and the forest floor evaporation, which could explain the more
depleted δ
18
O values at Doi Chiang Dao. Moreover, the elevation difference might
simply have affected the precipitation δ
18
O, causing our montane forest site more
isotopically depleted.

4.4.2. Cellulose δ
18
O as a proxy for regional rainfall
The stable oxygen isotopic composition of monsoon precipitation is well characterized by
the so-called amount effect where increasing rainout leads to more depleted rain water
δ
18
O values. However, the monsoon winds that carry moisture to the montane regions of
Thailand travel great distances. By the time these summer season winds reach Thailand
there has been considerable rainout and potentially some remixing of recycled moisture.
Therefore, we infer that the amount effect over Thailand is better described in terms of
the total amount of rainout that has occurred during the transit from the source regions
(Joswiak et al., 2010; Vuille et al., 2005; Yuan et al., 2004). In the first stage of the rainy
season which runs from June-July-August (JJA), an inter-hemispheric gyre circulation
develops in the lower atmosphere over the tropical Indian Ocean (Lau et al., 2000).
Easterly flow south of the equator transports moisture from this low towards the western
Indian Ocean, which is then entrained into the Somali Jet. The Somali Jet carries the
moisture towards Indian subcontinent, the Bay of Bengal and to Mainland Southeast Asia
(Fig. 4.6a). This is the main stage of the Indian Summer Monsoon, when the intense
59

heating of the land causes the ITCZ to shift northerly, thereby pulling the southwesterly
monsoon flow across the continent to as far north as China. The westerly, southwesterly
monsoonal circulation from the Indian Ocean carries large amounts of moisture to
northern Thailand (Fig. 4.6a). The long path length these air masses travel produces
significant rainout. Consequently, the rainout leads to the distinctive isotopic composition
of precipitation that falls in northern Thailand. Higher amounts of rainfall during these
months over India and the Bay of Bengal therefore lead to lower isotopic values in the
precipitation across northern Thailand.

In the latter part of the rainy season, from September to October (SO), the ITCZ shifts
southward and the southwest monsoon flow retreats. The southwesterly winds are
replaced by easterlies over Mainland Southeast Asia (Fig. 4.6b), which lead to the second
rainfall peak in SO (Fig. 4.1b). And again, because these easterly air masses travel across
much of Mainland Southeast Asia, they too undergo considerable rainout before reaching
northern Thailand. The isotopic composition of precipitation in northern Thailand during
this second seasonal rainfall peak in SO is therefore isotopically depleted relative to the
precipitation that falls over the southeastern portion of Mainland Southeast Asia.

The conceptual depiction of monsoon moisture isotopic variability presented above is
evaluated against simulated values for precipitation and its δ
18
O values from the IsoGSM
model. The long-term mean precipitation δ
18
O values simulated by IsoGSM exhibit a
pattern that is consistent with the conceptual model for winds and rainout presented
60

Figure 4.6. a) and b) Long term mean vector wind field at 850 mbar atmospheric level over India and Southeast Asia. c) and d) Long term
mean surface precipitation δ
18
O. e) and f) Correlation between the time series of Doi Chiang Dao precipitation δ
18
O and the field of
precipitation. Plots on the upper panel (a, c and e) are for June-July-August (JJA), and plots on the lower panel (b, d and f) are for
September-October. The data for a and b is from NCEP reanalysis (Kalnay et al., 1996), provided by the NOAA/ESRL Physical Sciences
Division, Boulder Colorado from their Web site at http://www.esrl.noaa.gov/psd/. Plots c, d, e, and f use the data output from the IsoGSM
model. Squares in c show the GNIP stations in this region. The hollow square in both e and f is the grid box for which the precipitation δ
18
O
is calculated for Doi Chiang Dao.

61

above. During JJA the precipitation δ
18
O values become progressively depleted along the
trajectory of winds blowing from Indian subcontinent to the Bay of Bengal, and to
northern parts of Mainland Southeast Asia (Fig. 4.6c). The GNIP observations over India
also indicate an isotopic enrichment of about 4‰ relative to values from Mainland
Southeast Asia during JJA (Fig. 4.7), suggesting that this geographic difference in
rainwater δ
18
O is not simply a model bias.

Figure 4.7. Long term monthly mean of precipitation δ
18
O averaged for GNIP stations in India (red) and
Mainland Southeast Asia (blue). Refer to Fig. 4.6c for locations of the GNIP stations.

The precipitation δ
18
O values simulated by IsoGSM for a grid box near our site at Doi
Chiang Dao, correlates strongly with the amount of JJA rainfall over southern India and
the Bay of Bengal (R<-0.6, Fig. 4.6e). This is a reflection of dominant influence of the
rainout effect described above, that the isotopic composition of the precipitation in
northern Thailand is inversely related to the amount of rainout that occurs in the upstream
portions of the wind trajectories in the India subcontinent and the Bay of Bengal.
Similarly, during SO, as the Indian Summer Monsoon weakens, the moist winds over
62

Mainland Southeast Asia shift to predominantly easterly and southeasterly, carrying
moisture from the South China Sea and the Western Pacific Warm Pool (Fig. 4.6b). In the
IsoGSM simulation the δ
18
O of precipitation becomes progressively more depleted as
winds advance northwestward over Mainland Southeast Asia (Fig. 4.6d). In this season
precipitation δ
18
O at Doi Chiang Dao correlates strongly with the amount of upstream
rainfall occurring to the southeast (Fig. 4.6f).

It is evident from the model results that the wind trajectories and moisture sources vary
seasonally, and the isotopic composition of rainwater over northern Thailand tracks the
precipitation amount across the region. However, it is difficult to separate out the
cellulose δ
18
O signals that are associated with each of the two rainy periods within a
single ring due to our sampling resolution. Nevertheless, both rainy periods and both
moisture sources contribute to the isotopic signature of soil moisture that is integrated
over the growth season.

In conclusion, our annual mean cellulose δ
18
O from northern Thailand correlates well
with the peak monsoon rainfall that occurs in both India and in Mainland Southeast Asia.
Years with lower δ
18
O anomalies reflected in the cellulose represent the combined
periods of enhanced rainfall over the monsoon region, and higher annual δ
18
O mean
values are associated with those years marked by reduced rainfall. There has been no
reported 20th century trend in AIR (Parthasarathy et al., 1994) or rainfall across
Mainland Southeast Asia, despite model projections that simulate enhanced monsoon
63

precipitation (Hu et al., 2000; May, 2004; Meehl and Arblaster, 2003; Ueda et al., 2006).
The cellulose δ
18
O record from northern Thailand does not exhibit a trend that would
point to an overall increase in monsoon precipitation either.

4.4.3. ENSO-monsoon relationship reflected in cellulose δ
18
O
One of the large-scale climate phenomena that influences monsoon is ENSO. It has long
been recognized that ENSO and South Asian monsoon are inversely related, with strong
monsoon coinciding with cold ENSO events and warm ENSO events with suppressed
monsoon strength (Walker, 1918; Webster, 1995; Yasunari, 1990). The mechanism that
governs the negative correlation between ENSO and the monsoonal circulation is
traditionally explained by the east-west shift of the Walker circulation (Kumar et al.,
1999; Webster et al., 1998). Under normal, non-El Niñ o conditions, the center of
atmospheric convection associated with the Walker circulation is located over the WPWP.
During El Niñ o events, the convection center shifts eastward with the eastward flow of
warm surface waters, and the descending limb of the Walker cell moves eastward
concomitantly towards the Indian Monsoon region. The subsidence creates anomalously
high pressure over the western Pacific-eastern Indian Ocean sector and suppresses
precipitation over the Indian subcontinent and western Pacific. However, the relationship
between ENSO and the Indian Summer Monsoon has weakened in recent decades, i.e. the
correlation between AIR and ENSO index has dropped since 1980 (Kumar et al., 1999).
This weakening relationship has also been recognized in tree ring cellulose δ
18
O
timeseries by other authors (Sano et al., 2010). It appears that a similar relationship is
64

present in our Thailand tree cellulose δ
18
O record as well. A 21-year moving window
correlation analysis between our annual mean cellulose δ
18
O and autumn SOI index
indicates a substantial weakening since 1980 (Fig. 4.8).

Figure 4.8. 21-year moving window correlations of September to November SOI with cellulose δ
18
O
annual mean (blue), and with June to September AIR (red). For direct comparison, the signs of the
correlation coefficients with cellulose δ
18
O are reversed. Dots are correlations higher than 95% significance
level.

We carried out an EOF analysis with CPC Merged Analysis of Precipitation (CMAP)
Enhanced dataset within the Indo-Pacific region in order to better elucidate how the time-
varying history of δ
18
O in our cellulose record relates to the regional climatological
changes (Fig. 4.9). In our analysis the first EOF mode explains 15% of the total variance
and the corresponding first Principle Component (PC1) correlates strongly with ENSO
(with Niñ o4, R=0.61, p<0.001). We interpret this first EOF mode to reflect the influence
of ENSO on the amount of precipitation over the Indo-Pacific region. The CMAP dataset
used in this analysis starts in 1979, about the same time that the correlation between
Indian Summer Monsoon precipitation and ENSO weakened. The first EOF mode indeed
shows that the precipitation in India subcontinent and most of Mainland Southeast Asia
exhibits only weak/no ENSO influence during the past three decades. Instead, the first
65

EOF mode/ENSO influence is strongest over the eastern tropical Indian Ocean-Maritime
Continent regions. This is in agreement with the analysis of Kumar et al. (1999), who
showed that during recent (1981-1997) El Niñ o events, the center of anomalous
subsidence was shifted southeastward compared to El Niñ o events between 1958-1980.
As a result, the region marked by rainfall deficits during El Niñ o has moved
southeastward away from India.

The apparent weakening of the monsoon-ENSO relationship over the past several
decades has been attributed to different mechanisms. Kumar et al. (1999) proposed that
the warming over Eurasia since the 1970s has enhanced the land-sea thermal gradient
which counteracts El Niño’s weakening effect on monsoon. Chang et al. (2001) found a
poleward shift of the winter jet stream over the North Atlantic, which results in less storm
activity over mid-latitude Eurasia and less snow cover, intensifying the subsequent
monsoon. Kinter et al. (2002) suggested that the climate regime shift in 1976 cooled the
SSTs in the extra-tropical north Pacific, which gave rise to cyclonic wind anomaly in the
lower troposphere and is responsible for the weakening monsoon-ENSO relationship.
Despite all the possible mechanisms put forth, the recent weakening could simply be a
result of the natural low frequency atmospheric variability (Krishnamurthy and Goswami,
2000). The monsoon-ENSO relationship has indeed been waxing and waning in our 21-
year moving window correlation (Fig. 4.8) as well as in other analyses (Maraun and
Kurths, 2005). Model simulations with greenhouse gas warming scenarios have not
shown systematic change in the monsoon-ENSO relationship either (Annamalai et al.,
66

2007; Ashrit et al., 2003). Therefore, the observed weakening relationship is most likely
due to internal decadal variability of the coupled atmospheric-oceanic system. To better
evaluate this, the existing observational networks for both monsoon and ENSO need to be
extended by terrestrial and marine-based proxies further back in time.
Figure 4.9. a) The first EOF mode of CMAP precipitation (Xie and Arkin, 1997) over the Indo-Pacific
region. b) The corresponding first principle component (PC1) strongly correlates with Niñ o4 SST (R=0.61,
p<0.001).

4.4.4. Hydrological balance of the winter dry season
In the subannual cellulose δ
18
O record, the annual maxima values occur near the ring
boundaries and are believed to be formed during the onset of the dry season. Although
the entire dry season from November to April might not be fully represented in the
67

growth of tree ring, the cellulose δ
18
O annual maxima could provide a glimpse of the
moisture conditions during the beginning of the dry season. A progressive decreasing
trend is detected in the cellulose δ
18
O maxima values (Fig. 4.4). Here we propose several
possible explanations. On the one hand, if we assume that there is no significant change
in the seasonal pattern of precipitation δ
18
O through time, the declining cellulose δ
18
O
maxima through time suggest a shortening of the growth season so that less and less
isotopic signature of the dry season is incorporated in the cellulose, but we found no
evidence to support this argument. On the other hand, if the assumption is made that the
seasonal growth pattern of these trees has been stable, there are a few other possibilities
which we consider.

Figure 4.10. Relative humidity (red) for the dry season November to April at the nearest meteorological
station Chiang Mai, and the November to April Parmer Drought Severity Index (UCAR PDSI) for the
region of 18-20 ° N, 98-100 ° E.

One possible explanation for the decreasing 
18
O maxima could be that as trees grow old
their roots tap water from deeper soil layer. Soil water δ
18
O decreases with depth due to
the evaporative enrichment near the surface (Gazis and Feng, 2004). However, the
cellulose δ
18
O annual mean or annual minima do not exhibit a consistent decreasing trend
68

for the rainy season, ruling out this possibility. An increase in dry season humidity
through time could also account for the decreasing trend in the cellulose δ
18
O maxima,
but neither the instrumental record of relative humidity at a nearby meteorological station
nor the Parmer Drought Severity Index for this area shows a positive trend (Fig. 4.10).
Moreover, the humidity in the local forest environment might have decreased due to less
cloud contact and deforestation as will be discussed below. Overall, these interpretations
seem implausible. In the following, we focus on another possible explanation that
involves an additional moisture source during the dry season.

With little rainfall during the dry months, the forest canopy helps ameliorate water stress
by capturing condensates from the fog/cloud cover (Bubb et al., 2004). The fog/cloud
cover also reduces canopy transpiration and forest floor evaporation, improving soil
water status (Dawson, 1998; Hutley et al., 1997). Epiphytes, which are common in cloud
forests, have an amazing capacity of storing water and supplying the water to animals
that inhabit the canopy (Foster, 2001). For this reason there is great concern that
destruction of the tropical montane forests or decreasing fog/cloud contact may be fatal to
both the hydrological status of these environments and the ecosystem as a whole.

Fog inputs are highly variable with time and location. Advection fogs both in coastal and
mountain areas typically yield higher deposition than radiation fogs in valleys (Clark et
al., 1998; Holwerda et al., 2006), and dry season tends to have larger fog input than wet
season (Liu et al., 2005; Liu et al., 2007). Worldwide studies for a range of evergreen
69

forest types across the humid tropical to subtropical and warm-temperature maritime
climatic spectrum show a net input of precipitation from fog deposition in the range of
19.5-64.5 mm/month (Bruijnzeel et al., 2005). In comparison, the average dry season
rainfall in Chiang Mai is 22± 33 mm/month. No work has been done to quantify the fog
water input in Doi Chiang Dao, however, but at a forest location Mengla in Southwest
China, which is a few hundred kilometers to the northeast of Doi Chiang Dao (Fig. 4.1),
Liu et al. (2007) have carried out field measurements of both rainfall and fog drip on a
monthly basis for two consecutive years 2002-2004. Fog drip is clearly in comparable
amount as rainfall in the dry months from November to April (Fig. 4.11a).

Fog generally has more enriched oxygen isotopic composition than rain (Gonfiantini and
Longinelli, 1962; Ingraham and Mark, 2000; Ingraham and Matthews, 1988, 1990; Scholl
et al., 2007). Rain and fog are both water condensates from vapor in the moist air, but
rain condenses at higher elevation whereas fog usually condenses near the ground surface,
where the temperature is warmer and the oxygen isotopic fractionation between vapor
and liquid is smaller. This is seen as the positive effect of temperature on the isotopic
composition of precipitation (Dansgaard, 1964). Moreover, fog in montane forests is
formed from terrestrial recycled water vapor, which is from surface evaporation and
forest evapotranspiration (Ingraham and Matthews, 1990; Liu et al., 2007). When plants
transpire vapor, there is no isotopic fractionation during root uptake, so the transpired
vapor carries the same isotopic signature as the xylem and soil water, which is
isotopically enriched than the original vapor in the air (Kurita and Yamada, 2008).
70

Therefore, recycled vapor, especially the vapor from forest evapotranspiration, is
isotopically enriched. The difference between fog/cloud water and rainfall δ
18
O is ~4-6‰
from worldwide studies (Anchukaitis and Evans, 2008; Dawson, 1998; Ingraham and
Matthews, 1990; Liu et al., 2007; Scholl et al., 2007). In the study site of Mengla that is
near Doi Chiang Dao, the δ
18
O of dry season fog water also shows a similar magnitude of
enrichment than the dry season rain water (Fig. 4.11b).

Figure 4.11. a) Monthly fog and rainfall amounts at Mengla, Xishuangbanna, Southwest China for a three
year interval. b) Isotope measurements of the dry season (November to April) fog water and rain water. c)
A linear regression of monthly fog drip amount against the frequency of fog occurrence indicates that the
fog frequency could be used to represent the total amount of fog water intercepted by plant canopy. Data
are provided by Liu et al. (2007).

We therefore are convinced that fog moisture can be a significant source of moisture in
the montane forests of Thailand during the winter dry season and contributes significantly
to the δ
18
O signature of soil moisture. The cellulose results at Doi Chiang Dao exhibit a
71

decreasing trend of 3.5‰ in the δ
18
O annual maxima. We interpret it to suggest that the
montane forest of northern Thailand has experienced a transition from a fog-dominated
soil moisture condition during the winter dry season to a condition where soil moisture is
now dominantly controlled by precipitation.

Mountain fog or cloud cover is a result of orographic lift. Moist air from the surrounding
area blows upward along the slope, accompanied by a decrease in temperature due to
orographic lifting and a decrease in saturated water vapor pressure. Once the relative
humidity reaches 100%, water droplets condense to form fog/cloud. This level is the LCL,
or the cloud base. LCL/cloud base varies with temperature and moisture content of the air,
and could be as low as 700 m during wet summer (Bruijnzeel et al., 2005). Using GCM
simulation under 2xCO
2
conditions, Still et al. (1999) suggested warmer tropical SSTs
would increase the moisture content of the atmosphere and shift the adiabatic lapse rate
towards a more moist condition, amplifying the warming at higher altitude and raising the
LCL. The height of orographic cloud bank formation in the dry season is lifted and this
reduces the frequency of cloud contact in tropical montane forests, resulting in less
horizontal precipitation and enhanced evapotranspiration. They further estimated that in a
2xCO
2
world, warmth index and absolute humidity surfaces both move upward by 200-
300 m at four cloud forest locations. The tropical high elevation sites may already be
showing enhanced warming (Foster, 2001). For example, Diaz and Graham (1996)
related a 100-meter upward shift of tropical glaciers and freezing heights with SST
warming since the late 1970s.
72

Figure 4.12. Monthly SST/T2m anomalies averaged over the region of 10-25 ° N, 95-110 ° E show a
warming trend in the 20th century. Data is from National Climatic Data Center’s Global Historical
Climatology Network Gridded Products, accessed through the KNMI climate explorer
(http://climexp.knmi.nl).

Similarly, humidity also affects orographic cloud formation. Lawton et al. (2001) used
the Colorado State University (CSU) Regional Atmospheric Modeling System (RAMS)
and suggested that deforestation could reduce evapotranspiration and thus the moisture
content of the air mass. When this less moist air mass flows up the slopes of adjacent
mountains, LCL rises and the cloud base is lifted. In the same study, they used Landsat
and Geostationary Operational Environmental Satellite imagery of Costa Rica’s
Caribbean lowlands and showed that the deforested areas remained relatively cloud free
during dry season compared to forested areas. Also using CSU RAMS, Ray et al. (2006)
estimated that deforestation in Costa Rica has decreased the fog/cloud cover in the
montane region by ~5-13% and raised the cloud base by ~25-75 m.

73

Figure 4.13. Dry season (November to April) fog frequency at six meteorological stations in northern
Thailand. Refer to Fig. 4.1 for the location of these meteorological stations.

An atmospheric warming trend is evident in Mainland Southeast Asia throughout the
20th century (Fig. 4.12). During this same period the highlands in northern Thailand have
been increasingly deforested to make way for agriculture and provide commercial
logging. In the 1930s there was approximately 70% forest cover over northern Thailand
whereas today there is only 13% (Delang, 2002; Hirsch, 1990). Meanwhile,
meteorological records from surrounding stations in northern Thailand already indicate a
decrease in dry season fog frequency in the late 20th century (Fig. 4.13). The frequency
of fog occurrence is conceivably translated to the total amount of fog water input, as
illustrated by a linear relationship between the two using the measurements from Liu et al.
(2007) (Fig. 4.11c). We therefore surmise that at ~1500 m, our site in the montane forest
74

of Doi Chiang Dao has experienced a progressive reduction in fog/cloud moisture due to
the combined effects of warming and deforestation. On the other hand, no long-term
trend is evident in dry season rainfall amounts. This transition from a fog-dominated dry
season soil moisture status to a condition that primarily relies on rainfall could account
for the observed decreasing trend in dry season δ
18
O we observe in the cellulose record.
The fog/cloud base has risen to higher elevations and this has left the montane forests
depleted in moisture during the dry season.

4.5. Conclusions
The subannual oxygen isotopic composition of tree ring cellulose has been analyzed for
Pinus kesiya from the tropical montane forest of Doi Chiang Dao spanning from 1922 to
2000. The δ
18
O values exhibit regular annual cycles, which we interpret to reflect
primarily the seasonal differences in the isotopic composition of soil moisture. Maximum
δ
18
O values occurring near ring boundaries and minimum δ
18
O values in the middle of
the rings correspond to the winter dry season and the summer rainy season, respectively.

We demonstrate the use of our cellulose δ
18
O annual mean to infer monsoon strength, as
it correlates significantly with rainfall amount in both India and Mainland Southeast Asia
during different rainy months. There is no long-term trend, in either instrumental
precipitation measurements or our cellulose record, to show an increase of monsoon
strength with warming in the 20th century as projected by some climate models. Our
75

cellulose record indicates a weakening relationship between monsoon and ENSO since
1980.

The cellulose δ
18
O annual maxima reflect the soil moisture conditions in the beginning of
the winter dry season. Their progressive decreasing trend is tentatively attributed to a
decreasing fog/cloud water input in the montane forest, a possible consequence of
atmospheric warming as well as deforestation. This implies a drying water budget in the
winter dry season, with possible negative effects on the stream flows originating from the
highlands of northern Thailand.

76

Chapter Five

Indo-Pacific Warm Pool Convection and ENSO Since 1867

Summary
The Indo-Pacific Warm Pool (IPWP) is a major source of heat and moisture to the
atmosphere and thus strongly influences the global climate. In this study, we investigate
how moisture fluxes from the IPWP influence the stable isotope signature of precipitation
over Southeast Asia by analyzing the oxygen isotopic composition (δ
18
O) of tree
cellulose from southern Cambodia. The cellulose δ
18
O record, spanning AD 1867-2006,
documents a regular seasonal cycle with an average amplitude of ~4‰ that is primarily
controlled by seasonal differences in the isotopic composition of precipitation. Using the
outputs from an isotope-enabled atmospheric model, we illustrate how the δ
18
O of
precipitation at our site is predominantly controlled by the amount of rainout that occurs
over the moisture source region, the IPWP. This is verified by strong correlations of our
cellulose δ
18
O record with instrumental measurements of precipitation and outgoing
longwave radiation over the IPWP, suggesting that the cellulose δ
18
O could be used to
reconstruct the convection intensity over the IPWP. Spectral analysis of the cellulose
δ
18
O reveals significant peaks at 2-7 years corresponding to ENSO frequencies. The
variability of the cellulose δ
18
O record on the ENSO band exhibits characteristics that
match existing coral δ
18
O records from the tropical Pacific, with reduced amplitude of
variability in the 1920s through the 1960s, a period of weak ENSO activity.
77

5.1. Introduction
The IPWP is a major heat and moisture source to the atmosphere’s convective
overturning in both the Hadley circulation and the Walker circulation. Variable heat
exchange between the surface ocean and the atmosphere in the tropical Pacific on
interannual timescales associated with ENSO has a strong influence on climatic
conditions globally (Mcphaden and Picaut, 1990). Climate modeling as well as
paleoclimate studies also suggests that changing temperatures within the tropical warm
pool may have been an important influence on climate changes from decadal to
millennial timescales (Clement et al., 2001; Linsley and Thunell, 1990; Stott et al., 2002;
Timmermann et al., 1999). In efforts to document how the tropical hydrological cycle
changes with global warming, model simulations and reanalysis data for the 20th century
provide somewhat contradictory results, with regard to whether it is strengthening (Mitas
and Clement, 2005) or weakening (Tanaka et al., 2005). Unfortunately, instrumental
measurements for the tropical surface oceans are sparse prior to 1950, and satellite
observations barely extend beyond the past three decades (Chen et al., 2002; Wielicki et
al., 2002). Longer, higher resolution records derived from proxies that can capture the
hydrologic variability could extend the instrumental records and help resolve these
discrepancies.

Past studies utilizing marine sediment proxies (foraminiferal stable isotope and Mg/Ca
records) and speleothem isotope records have documented millennial to centennial scale
changes in tropical temperatures and moisture fluxes that were coincident with high
78

latitude climate variability, and this may be indicative of how the warm pool in the
Pacific can modulate energy in the global climate system (Newton et al., 2006; Oppo et
al., 2009; Partin et al., 2007; Stott et al., 2002; Visser et al., 2003). Corals in the tropical
oceans have provided high-resolution information about the sea surface conditions in the
past few centuries, and this has improved our understanding of the ENSO-related
variability (Asami et al., 2005; Charles et al., 2003; Charles et al., 1997; Cole et al., 2000;
Cole et al., 1993; Quinn et al., 1996; Quinn et al., 1998; Urban et al., 2000). In an attempt
to augment these oceanographic records with a terrestrial counterpart that has high
temporal resolution, we investigate how the isotopic composition of tropical moisture is
conveyed from the ocean to the land by analyzing the isotopic composition of cellulose
extracted from the annual rings of tropical trees.

In this study, we have analyzed the oxygen isotopic composition (δ
18
O) of tree cellulose
for the past 140 years from trees growing in a tropical forest in Cambodia where the
regional climate is sensitive to the oceanic and atmospheric behavior within IPWP
(Buckley et al., 2010). At this study location the tree cellulose records the δ
18
O of rain
water that is transferred to soil moisture. By sampling the annual tree rings at subannual
resolution we reconstruct the δ
18
O of precipitation during different stages of the rainy
season. We demonstrate that the precipitation δ
18
O at this location as inferred from the
cellulose record is influenced by the strength of atmospheric convection over the IPWP
as well as ENSO activities. We then compare our cellulose δ
18
O record to existing coral
δ
18
O records in the tropical Pacific Ocean and discuss their similar variabilities.
79

5.2. Materials and Methods

Figure 5.1. a) Map of Southeast Asia showing the sampling site Kirirom and the nearby meteorological
station Phnom Penh. Boxed region represents the Indo-Pacific Warm Pool. b) Scanned image of a tree core
sample showing the annual ring structures. c) Climatology at the meteorological station of Phnom Penh,
with temperature in curve, and precipitation in bars.

Our study site is Kirirom National Park (675 m, 11.29 º N, 104.25 º E; Fig. 5.1a) in
southern Cambodia. At this location in Southeast Asia, there is strong seasonality in
precipitation (Fig. 5.1b). During the boreal winter from December to March there is very
little or no precipitation. The months of May to October are the rainy season. The onset
of the Indian Summer Monsoon typically occurs in May, with the development of the
land-sea thermal contrast and a significant increase in both heat and moisture during the
month of April. The strong southwesterly monsoon winds carry large amounts of
80

moisture from the tropical Indian Ocean and the Bay of Bengal to Mainland Southeast
Asia. This southwesterly wind pattern generally lasts until mid-September, after which
the Indian Summer Monsoon retreats. Mainland Southeast Asia is then dominated by
easterly winds that transport moisture from the South China Sea and the Maritime
Continent region (Fig. 5.2), and this leads to the peak in precipitation between September
and October (Fig. 5.1b). The precipitation that falls over Kirirom during these two rainy
periods has distinctly different isotopic compositions, which reflect their different
moisture sources (Aggarwal et al., 2004).

Figure 5.2. The long term mean wind vectors at 850 mbar level for the rainy months of a) June-July-
August, which represents the Indian Summer Monsoon season, and b) October-November, which
represents the rainy period after the Indian Summer Monsoon retreats. Also shown in color for each rainy
period is the spatial correlation between the precipitation δ
18
O at Kirirom and the field of precipitation
amount. Only correlation above 90% significance level is shown. The data for wind vectors, precipitation
δ
18
O and precipitation amount are all from IsoGSM model outputs.

Kirirom is the southernmost location in Mainland Southeast Asia where true pines are
found. Sample cores of Merkus pine (Pinus merkusii Junghuhn & De Vriese) were
collected in 2009. Consistent with the rainfall pattern, Merkus pine grows rapidly during
the wet season from May to October. The cambial activity declines gradually as the dry
81

season starts in November, and becomes dormant until the end of the dry season March-
April (Pumijumnong and Wanyaphet, 2006). This growth pattern results in clear ring
structures. Each annual ring begins with a light colored earlywood that is characterized
by large tracheid cells with thin walls and large lumens, and lower in density than the
thicker walled latewood cells with small lumens (Fig. 5.1c). In some years, there are
missing rings and false rings due to unusual growth. In spite of that, Merkus pine has
been successfully crossdated in Thailand and Laos (Buckley et al., 2007; DArrigo et al.,
1997; Pumijumnong and Eckstein, 2011). The cores used in this study were crossdated in
the Tree Ring Lab at Lamont-Doherty Earth Observatory. For isotope analysis, we
selected three cores based on the criteria of small numbers of missing or false rings and
regular ring boundaries (Leavitt et al., 2010).

The cores selected were drilled from three individual trees that were growing a few
kilometers apart, thereafter identified as KRPM09A, KRPM10A and KRPM15B. Each
core was sliced parallel to ring boundaries using a microtome. Subannual samples of each
ring were obtained by carefully spacing discrete slices over the width of an annual ring.
The wood samples were then processed using a modified Brendel method (Gaudinski et
al., 2005) to extract α-cellulose. The cellulose samples were analyzed for their oxygen
isotopic ratio (δ
18
O) using a Thermo Finnigam TC/EA coupled with a Delta V Advantage
IRMS. Results were reported in δ notation relative to vSMOW. The analytical precision,
based on repeated measurements of interspaced cellulose standards (IAEA cellulose and
baker cellulose), was ±0.3‰.
82

The subannual sampling strategy allows us to examine the δ
18
O of tree cellulose
produced at monthly to weekly time resolution. The δ
18
O

of cellulose is primarily a
function of the δ
18
O of soil moisture, which a tree obtains through its root system, as well
as the relative humidity of the ambient environment during growth, which controls the
rate of evapotranspiration and its associated isotope fractionation (Sternberg, 2009). The
trees we sampled were growing at ridge lines where rain water drains rapidly from the
soil and thus there is minimal groundwater storage. This means the water used by the
trees to synthesize cellulose is the water that falls more-or-less simultaneously with tree
growth and cellulose production. During the rainy season, high relative humidity
suppresses the evapotranspiration, so the δ
18
O of cellulose is mainly controlled by the
δ
18
O of rainwater. In the tropics, the rainy season is characterized by isotopically depleted
(more negative δ
18
O) rainwater due to the so-called isotope amount effect (Araguas-
Araguas et al., 1998). In contrast to the rainy season, the dry season precipitation is more
isotopically enriched (more positive δ
18
O), and lower humidity enhances the
evapotranspiration, which leads to a further enrichment in the δ
18
O of tree cellulose
(Evans and Schrag, 2004). By analyzing cellulose at subannual resolution, we capture
these seasonal variations in δ
18
O and extract the climatological and ecological influences
in different seasons.
83

Figure 5.3. a) Subannual cellulose δ
18
O measurements of the three cores KRPM15B (red), KRPM10A (blue) and KRPM09A (green),
continued in b.

84

5.3. Results
We analyzed Core KRPM15B from 1867 to 2006. Cores KRPM10A and KRPM09A
were analyzed discontinuously for several intervals to replicate the continuous record of
KRPM15B, and also because the other intervals were broken in small pieces and were
difficult to slice. All three cores correspond with one another very well in terms of both
intraannual and interannual variabilities (Fig. 5.3). The most depleted δ
18
O value occurs
at the center of each ring, where the ring grows fast during the rainy season, and the most
enriched δ
18
O value occurs near the ring boundary, where the ring growth slows down or
even stops during the dry season.

Figure 5.4. a) Intraannual variation of the cellulose δ
18
O composited from all the individual annual rings of
all three cores. Horizontal axis represents the distance to the ring boundary with respect to the width of the
ring. Anomalies are taken by subtracting annual means from the raw δ
18
O values to get rid of the
interannual variation. b) Same but for precipitation δ
18
O from GNIP observations in Bangkok. c) Same but
for precipitation δ
18
O from monthly IsoGSM outputs.

This intraannual variation in cellulose δ
18
O is primarily reflective of the seasonal
difference in precipitation δ
18
O as well as relative humidity. A composite of the intra-ring
δ
18
O variation pattern from all individual rings reveals an annual cycle with mean
amplitude of ~4‰ (Fig. 5.4a). We compare this with composites of the seasonal cycle of
85

precipitation δ
18
O from two data sources. First, we select instrumental measurements of
rainwater δ
18
O from Bangkok as part of the GNIP dataset. Bangkok is located about 450
km to the northwest of Kirirom (Fig. 5.1a) and is the nearest GNIP station with a
relatively long and complete record that dates back to 1968. We also select precipitation
δ
18
O simulated by an isotope-enabled atmospheric model IsoGSM (Yoshimura et al.,
2008), which has published data from 1979 to 2008. For this comparison we utilize the
model outputs of precipitation δ
18
O at the grid point nearest to Kirirom. Both GNIP and
IsoGSM precipitation δ
18
O exhibits similar seasonal pattern (Fig. 5.4b and c). During the
dry season from November to April, the precipitation is isotopically enriched. This rain
water, together with a further isotopic enrichment associated with enhanced
evapotranspiration leads to δ
18
O values of tree cellulose that are the most enriched in an
annual ring. From May to early-September, this region receives large amounts of rainfall
from the Indian Summer Monsoon moisture, and the precipitation δ
18
O is depleted due to
the amount effect of the monsoon rainfall. The precipitation is even more isotopically
depleted in mid-September through October, when Indian Summer Monsoon retreats and
the moisture source is diverted to the South China Sea-Maritime Continent region (Fig.
5.2). We therefore attribute the most isotopically depleted part of the tree ring, i.e. the
cellulose δ
18
O annual minimum value, to the growth that uses the most isotopically
depleted rain water during October. The interannual variability of the Kirirom cellulose
δ
18
O annual minima correlates significantly with the precipitation δ
18
O in October from
both GNIP and IsoGSM datasets (Table 5.1).

86

Table 5.1. Correlation coefficients between the cellulose δ
18
O annual minimum values (first row) and the
precipitation δ
18
O values in October (first column)
a

KRPM09A
b
KRPM10A KRPM15B KRPM average
IsoGSM Kirirom - 0.60 0.49 0.60
GNIP Bangkok - 0.53 0.64 0.63

a
All correlation coefficients are above 99% significance level.
b
For KRPM09A, there are not enough overlapping data with the precipitation δ
18
O.

Table 5.2. Correlation coefficients between the cellulose δ
18
O values of any two cores and the EPS values
a

Monthly
values
Monthly
anomalies
Annual
minima
Annual mean
KRPM09A vs. 10A 0.76 0.42 0.64 0.53
KRPM09A vs. 15B 0.73 0.36 0.67 0.59
KRPM10A vs. 15B 0.75 0.46 0.57 0.49
EPS 0.90 0.68 0.84 0.78

a
All correlation coefficients are above 99% significance level.

It is difficult to assess how much tree ring growth has occurred in the rainy season versus
in the dry season. In order to generate continuous timeseries, we develop a simplified age
model for the cellulose δ
18
O by assigning October to the cellulose δ
18
O annual minima
and February to the cellulose δ
18
O annual maxima. From these tie points, adjacent
samples are linearly interpolated to monthly resolution. The monthly interpolated series
for all three cores are correlated to assess the reproducibility. Correlation coefficients are
calculated for monthly interpolated δ
18
O values, monthly anomalies after subtracting the
long term mean for each month, annual minimum (October) values, and annual mean
values. We also calculated the Expressed Population Signal (EPS) to evaluate the
strength of the common signals (Wigley et al., 1984). The correlation coefficients and
EPS values are listed in Table 5.2. They are strong and significant, thus indicating good
reproducibility among the three cores.
87

Figure 5.5. a) Monthly interpolated cellulose δ
18
O averaged from three cores. b) Anomalies of October
cellulose δ
18
O after subtracting the long-term mean. Also shown are recent ENSO events.

The monthly interpolated cellulose δ
18
O from all three cores are then averaged to produce
a single timeseries (Fig. 5.5a). No conspicuous long term trend is detected in the cellulose
δ
18
O. However, there is an interannual variability that appears to be ENSO-related. For
example, in El Niñ o years of 1891, 1925, 1972, 1977, 1982, 1994, 1997 and 2002 (Gergis
and Fowler, 2009), the cellulose record exhibits smaller annual cycles. In particular, the
δ
18
O annual minima in these years are more enriched compared to adjacent years.
Conversely, La Niñ a years of 1886, 1917, 1922, 1973, 1988, 1995, and 1998 (Gergis and
Fowler, 2009) are marked by cellulose δ
18
O annual minima that are more depleted. In
addition to these interannual differences, there are also notable decadal changes such as
88

the 1976-1977 shift towards more enriched δ
18
O values, which coincides with the climate
regime shift in the Pacific Ocean (Deser et al., 2004; Mantua and Hare, 2002).

The cellulose δ
18
O annual maximum values, which we interpret as reflecting values
associated with growth conditions during February, do not have significant correlation
with any climate data, possibly due to complication of leaf evaporative enrichment during
the dry season (Roden et al., 2000). Moreover, it is likely that the trees become dormant
or grow extremely slowly during the dry months, in which case, the interpolated δ
18
O
values for the winter dry months in our record may not accurately represent these months.
The more depleted cellulose δ
18
O values associated with the wet summer months are
governed by a simpler mechanism that primarily involves the δ
18
O of precipitation and
the associated isotope amount effect. This is because the trees grow faster during the
rainy months, developing majority of the material in the annual rings, and high humidity
reduces the influence of fractionation associated with evapotransporation. Hence the most
isotopically depleted portion of the annual ring, as resulted from our high-resolution
sampling, more reliably reflects the true growth during the rainy months and is more
easily interpreted as climate signals. Indeed, warm and cold ENSO events are associated
with less and more depleted cellulose δ
18
O annual minima, respectively, as illustrated
previously. For this reason, we take out only the cellulose δ
18
O annual minima, which are
interpreted to reflect rainfall in October, and calculate the anomalies with respect to the
long-term mean through 1867-2006 (Fig. 5.5b). Most recent El Niñ o events appear as
positive anomalies, and La Niñ a years as negative anomalies. In the following, we
89

discuss how ENSO is recorded in our cellulose record through convection over the IPWP
region, using model outputs from IsoGSM as well as observations from both our
cellulose δ
18
O record and instrumental climate datasets.

5.4. Discussion
5.4.1. Convective activity over the warm pool
With its warmest surface water, the IPWP supplies large amounts of heat and moisture to
the atmosphere through its intense convection. During the processes of condensation and
precipitation, oxygen isotopes fractionate. Heavier isotopes (D,
18
O) preferentially rain
out and leave the remaining atmospheric moisture more isotopically depleted. Therefore,
stronger convective activity, i.e. more cloud formation and heavier precipitation, would
result in more isotopically depleted atmospheric moisture. The convection intensity over
the IPWP is further influenced by the oscillation of the atmospheric Walker circulation
that is related to ENSO variability. During normal or La Niñ a conditions, the ascending
limb of the Walker circulation is located over the IPWP. The intensive cloud formation
and heavy rainout result in isotopically depleted atmospheric moisture over the IPWP.
During El Niñ o, however, the strongest convection shifts eastward along with the
eastward flow of the warm surface water. This suppresses convection and precipitation
over the IPWP. Atmospheric water vapor over the IPWP thus remains isotopically
enriched.

Atmospheric moisture evaporated from the IPWP is responsible for wet season
precipitation at our site of Kirirom in the coastal region of Cambodia. During the Indian
90

Summer Monsoon months from May to mid-September, westerly winds transport
moisture from the eastern tropical Indian Ocean and the Bay of Bengal, the western
component of the IPWP (Fig. 5.2a). During the later rainy period from mid-September to
October-November, winds over Cambodia shift to easterlies, drawing moisture from the
South China Sea-Maritime Continent region, which is the eastern side of the IPWP (Fig.
5.2b). The precipitation that falls at Kirirom therefore carries an isotopic signature that is
similar to the IPWP atmospheric moisture, which is further determined by the intensity of
convection and precipitation over the IPWP. We employ the model outputs of IsoGSM to
test this idea. A spatial correlation between the timeseries of precipitation δ
18
O at Kirirom
and the precipitation amount over the IPWP region is calculated for the two rainy periods
as described above. These are plotted in Figure 5.2 along with the long-term mean wind
vectors at the 850 mbar level. For both rainy periods, the precipitation δ
18
O at Kirirom
correlates negatively with the precipitation amount over most parts of the IPWP. In
particular, the moisture source region that is upwind of air at the Kirirom site during each
of the rainy periods determines the isotopic composition of rainwater at Kirirom. For
example, during October-November, after the Indian Summer Monsoon retreats and
when the easterlies dominate, the precipitation δ
18
O at Kirirom correlates best with the
precipitation amount to its east and northeast, over the South China Sea-Maritime
Continent region.

In summary, the IsoGSM model outputs reinforce our assertion that the intensity of
convection and the amount of rainout occurring over the IPWP region determines the
91

isotopic composition of the rain water at Kirirom, which is further transmitted to the
cellulose of growing trees. On an interannual basis, convective uplift over the IPWP is
influenced by ENSO variability. This explains why we observe a strong ENSO signal in
our cellulose record (Fig. 5.5b). On a seasonal basis, the moisture source region shifts in
different months between different parts of the IPWP. Ideally, our monthly interpolated
cellulose δ
18
O could track these seasonal shifts. In the following, we conduct further
correlation analysis using the Kirirom cellulose record along with instrumental datasets to
verify the above observations from the IsoGSM model outputs.

Figure 5.6. The difference in precipitation δ
18
O between June-July-August mean, when the moisture source
is the Indian Summer Monsoon, and October, when the moisture source is the South China Sea-Maritime
Continent. Data are from Bangkok GNIP record (a) and IsoGSM simulation at the grid point near Kirirom
(b).

We use CMAP precipitation and NOAA interpolated Outgoing Long-wave Radiation
(OLR) as two instrumental proxies for convection over the IPWP (Johnson and Xie, 2010;
Newman et al., 2000). Both measure the convection intensity integrated through the
atmospheric column, and are the longest available observational datasets of this kind that
92

extend back to the 1970s. In these records stronger convective activity over the IPWP is
expressed as heavier precipitation and less OLR (due to more clouds). However, our
monthly interpolated cellulose δ
18
O does not correlate with CMAP or OLR in any other
months other than October. We suspect our monthly interpolation strategy is flawed due
to uncertainties in the growth behavior of the trees and associated artifacts that stem from
our slicing subannual samples. It is therefore difficult to identify the individual cellulose
values for each individual month based on a linear interpolation technique. Nevertheless,
we believe the most depleted isotope values associated with October precipitation are
well resolved in the cellulose δ
18
O annual minima.

GNIP observations as well as IsoGSM model outputs have shown that October rainfall at
our site in the southern part of Mainland Southeast Asia is distinctly depleted in heavier
isotopes compared to the earlier Indian Summer Monsoon rainy season from May to mid-
September, due to their different moisture sources. The magnitude of this isotopic
difference is ~4‰ and remains stable on interannual basis (Fig. 5.6). Other studies such
as the work carried out by Aggarwal et al. (2004) have also noted that the moisture
source of the western Pacific Ocean-Maritime Continent region is more isotopically
depleted compared to the eastern tropical Indian Ocean-Bay of Bengal. Therefore, we
believe the Kirirom cellulose δ
18
O annual minima are a robust representation of the
rainfall δ
18
O that falls around October, when moisture is from the western Pacific Ocean-
Maritime Continent region. The cellulose δ
18
O annual minima correlate strongly with
both CMAP (negatively) and ORL (positively) over the western Pacific-Maritime
93

Continent region in October to December (Fig. 5.7). This is in agreement with the
relationship indicated by the IsoGSM model outputs, suggesting that the cellulose δ
18
O
has reasonably well preserved the information about the convection intensity over the
IPWP.

Figure 5.7. Spatial correlation of October Kirirom cellulose δ
18
O values with the October-November-
December mean of a) CMAP precipitation, and b) NOAA interpolated OLR. Only correlation above 90%
significance level is shown. Box in a shows the Niñ o-4 region and triangles in b show the sites of tropical
Pacific coral δ
18
O records, see Table 5.3 for details of the sites.

94

The correlation is also strong, but with opposite sign between cellulose δ
18
O at Kirirom
and precipitation over the central equatorial Pacific, the Niñ o-4 region (Fig. 5.7a),
suggesting an influence of ENSO on the IPWP convection. The Niñ o-4 SST index for
October correlates positively with Kirirom cellulose δ
18
O in October (R=0.56, Fig. 5.8).
Ten-year low-pass filters of these timeseries reveal that they also exhibit similar patterns
of low-frequency variability, particularly after the 1920s. The decreased similarity prior
to 1920 may be attributed to the decreased accuracy of observed SSTs in the earlier part
of the record as they were interpolated from rather sparse observations (Kaplan et al.,
1998). Another possible explanation lies in the uncertainty in the ENSO mechanism and
variability. We interpret the Kirirom cellulose record as a proxy for precipitation over the
IPWP, whereas Niñ o-4 is an index for ENSO and SST in the central equatorial Pacific.
The atmospheric connection that links the hydrology of IPWP to ENSO might have
changed in the past. Moreover, whether ENSO expresses itself more in the central Pacific
or eastern Pacific is under debate (Ashok et al., 2007; Kao and Yu, 2009). According to
the cellulose δ
18
O record, there is no overall trend in the past 140 years. However, the
1880s through the 1910s is an interval with more enriched δ
18
O values. These
observations possibly indicate no trend in the frequency and magnitude of ENSO in the
past 140 years, but the 1880s through the 1910s were under a background condition that
was more El Niñ o-like. Cautions need to be taken when making these interpretations as
uncertainties exist in the geochemical measurements of cellulose δ
18
O. The
reconstruction network needs to be expanded to include more similar studies in order to
validate our interpretations.
95

Figure 5.8. Correlation between Kirirom cellulose δ
18
O October values and Niñ o-4 SST index for October
(R=0.56). Thick lines are the 10-year low-pass filters. Shaded bars highlight the similar decadal variations
between the two timeseries.

5.4.2. Comparison with tropical corals
Corals in the surface water of tropical oceans, particularly in the western and central
tropical Pacific, have been used extensively to reconstruct sea surface conditions and
ENSO activities. The δ
18
O of coral skeletons varies as a function of both SST and the
δ
18
O of ambient seawater, the latter of which is related to precipitation (Cobb et al., 2003;
Quinn et al., 2006). During El Niñ o, the center of anomalously warm SSTs and high
precipitation migrates towards the central equatorial Pacific. This leads to an isotopic
depletion in the central Pacific corals. La Niñ a corresponds to cool and dry conditions
and thus more enriched coral δ
18
O values in the central Pacific. Conversely, corals in the
western Pacific warm pool region are isotopically enriched during El Niñ o and are more
depleted during La Niña. We took advantage of existing coral δ
18
O records from both the
96

central and western tropical Pacific regions to compare with the Kirirom cellulose δ
18
O
record.

Table 5.3. List of coral δ
18
O records in the tropical Pacific Ocean, and the correlation coefficients (R) of
their October to December mean values with Kirirom cellulose October values
a

No.
b
Lat Long Site Age R Reference
1 13.60 144.84 Guam 1790-2000 0.13 Asami et al. [2005]
2 1.50 124.83 Bunaken 1860-1990 0.40 Charles et al. [2003]
3 -8.25 115.50 Bali 1782-1990 0.09 Charles et al. [2003]
4 5.87 -162.13 Palmyra 1886-1998 -0.22 Cobb et al. [2003]
5 1.50 173.00 Tarawa 1894-1990 -0.38 Cole et al. [1993]
6 2.00 -157.30 Kiritimati 1938-1993 -0.44 Evans et al. [1999]
7 -15.00 167.00 Vanuatu 1806-1979 0.12 Quinn et al. [1996]
8 -22.48 166.47 Amedee 1657-1992 0.16 Quinn et al. [1998]
9 -4.18 151.98 Rabaul 1867-1997 0.03 Quinn et al. [2006]
10 -5.22 145.82 Madang95 1922-1991 0.12 Tudhope et al. [1995]
11 -5.22 145.82 Madang01 1880-1993 0.27 Tudhope et al. [2001]
12 -4.15 144.88 Laing 1884-1993 0.29 Tudhope et al. [2001]
13 -6.08 147.60 Huon 1977-1995 0.33 Tudhope et al. [2001]
14 1.00 173.00 Maiana 1840-1994 -0.37 Urban et al. [2000]

a
In bold are the eight corals records that correlate significantly with Kirirom cellulose record.
b
Correspond to numbers in Figure 7b.

Fourteen coral δ
18
O records are found within the IPWP and the central Pacific regions
(Table 5.3, Fig. 5.7b), most of which were sampled and analyzed at monthly resolution.
For consistency, we have also interpolated coral records with lower resolution to monthly
resolution. From each record we derive an estimate of October-November-December
(OND) mean coral δ
18
O (except for Vanuatu coral δ
18
O, which is in annual resolution,
and the annual δ
18
O is used instead), and correlate that to Kirirom October cellulose δ
18
O.
Eight coral records exhibit significant correlation with the Kirirom cellulose record
(Table 5.3). The central Pacific corals (No. 4, 5, 6 and 14 on Fig. 5.7b and Table 5.3)
97

correlate negatively with Kirirom cellulose δ
18
O, whereas western and southwestern
Pacific corals (No. 2, 8, 11 and 12) correlate positively with the cellulose. These
correlations reflect locations where corals record different relationships to hydrological
conditions over the IPWP. Corals that are located in the transitional region on the
correlation map (No. 1, 7, 9, 10 and 13) do not show significant correlation with the
cellulose record, as expected. Surprisingly, the Bali coral δ
18
O record (No. 3), which is
situated right in the center of the IPWP where both CMAP and OLR strongly correlate
with the Kirirom cellulose δ
18
O (Fig. 5.7b), does not show good correlation.

Most of the central Pacific coral δ
18
O records indicate a decreasing trend over the second
half of the 20th century (Fig. 5.9), which has been argued to be a possible manifestation
of the 20th century SST warming (Cobb et al., 2003; Quinn et al., 1998). However, there
is no such trend in the Kirirom cellulose record (Fig. 5.5). We attribute this to the fact
that Kirirom cellulose δ
18
O mirrors precipitation variability over the IPWP. The small
magnitude of the warming would have a minor influence on convective intensity because
the SST threshold for tropical convection might co-vary with SSTs (Johnson and Xie,
2010). Western Pacific corals generally have weaker correlation than central Pacific
corals with the Kirirom record. This is likely due to the fact that coral δ
18
O contains both
precipitation and temperature influences. In the central Pacific, both precipitation and
SST co-vary with ENSO, which affects the hydrological conditions over the western
Pacific.
98

Figure 5.9. The monthly values of the five coral δ
18
O records that best correlate with the Kirirom cellulose
δ
18
O. Tarawa, Maiana, and Palmyra corals are from the central Pacific, and Bunaken and Madang corals
are from the western Pacific.

Most of the coral records exhibit strong variance at ENSO frequencies as reported by the
authors. We applied a power spectral analysis to the Kirirom cellulose δ
18
O record to
assess its major periodicities. Monthly interpolated cellulose δ
18
O was used instead of the
October values in order to ensure a sufficiently high resolution to capture the ENSO 2-7
year recurrence. Similar to the corals, the cellulose δ
18
O exhibits prominent variance on
the 2-7 year band (Fig. 5.10). We select five coral records that correlate best with our
99

cellulose record and also have significantly long time spans (Tarawa, Maiana, and
Palmyra from the central Pacific; Bunaken and Madang from the western Pacific). We
then filter the monthly cellulose δ
18
O as well as the five monthly coral δ
18
O records using
a 2-7 year window to examine their variability associated with ENSO (Fig. 5.11). The
band-pass filter of the cellulose δ
18
O varies in anti-phase with the three central Pacific
coral δ
18
O and in phase with the two western Pacific coral δ
18
O records. Another
common feature observed from the band-pass filters of all the six records is a reduced
amplitude of variability between the 1920s and the 1960s, which is a well-recognized
period with weak ENSO variability (Quinn et al., 2006).

Figure 5.10. Power spectral density of the monthly Kirirom cellulose δ
18
O showing major periodicities at
2.5, 3.6, 6, and 13.5 years.

100

Figure 5.11. 2-7 year band-pass filters of the five coral δ
18
O records and the Kirirom cellulose δ
18
O record.
The central Pacific coral records (Tarawa, Maiana, and Palmyra) correlate negatively with the Kirirom
cellulose δ
18
O, therefore their y-axes are reversed. The western Pacific coral records (Bunaken and Madang)
correlate positively with the cellulose record. Decreased variability between 1920s and 1960s (interval
between the shaded bars) appears to be the common feature of all the records.

In addition to the interannual variability, there is also indication of a decadal mode at
~13.5 year cycle revealed by the power spectral analysis (Fig. 5.9). Similar decadal
variability has been documented in coral records ranging from the Pacific Ocean (Asami
et al., 2005; Quinn et al., 1996; Quinn et al., 1998) to the Indian Ocean (Charles et al.,
2003; Charles et al., 1997). Latif and Barnett (1994) suggested this decadal pattern might
be related to an internal climate oscillation within the Pacific basin such as the Pacific
101

Decadal Oscillation (PDO). For instance, the 1976-77 shift seen in our cellulose record as
well as in many coral records is a transition in the PDO. By comparing the 6 years after
the 1976-77 transition to the 6 years before the transition, Graham (1995) showed from
both observations and a model simulation that the transition lead to a drier condition in
the maritime continent and a wetter conditions in the central equatorial Pacific. This is in
agreement with our cellulose record, which suggests an isotopic enrichment after the
transition. However, the mechanism behind this decadal variability as commonly seen in
the tropical oceans still requires further investigation.

5.5. Conclusions and implications
In this study, we have analyzed the δ
18
O of tree cellulose for an evergreen species Pinus
merkusii from a tropical forest in Cambodia in subannual resolution for the period AD
1867-2006. The cellulose δ
18
O exhibits regular seasonal cycle which is primarily
attributed to the seasonal difference in the δ
18
O of precipitation. At this location in
Southeast Asia, precipitation is influenced by two moisture sources, an early rainy period
co-occurring with the Indian Summer Monsoon, and a late rainy period brought by
easterlies from the South China Sea and the Maritime Continent. We are able to identify
in the cellulose record the δ
18
O associated with the latter rainy period because of its
distinctly depleted isotopic signature. This δ
18
O signal is further used to infer past
changes in the hydrological cycle based on understandings of the “amount effect”, an
inverse relationship between the δ
18
O and the amount of precipitation in the tropics
(Araguas-Araguas et al., 1998).
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Recent studies have suggested that the amount effect should better be interpreted to
reflect the total amount of rainout that occurs upstream and particularly over the moisture
source region (Joswiak et al., 2010; Kurita et al., 2009; Pausata et al., 2011; Vuille et al.,
2005; Yuan et al., 2004). Consistent with this interpretation, our cellulose δ
18
O
demonstrates high degree of correlations with precipitation and OLR over the IPWP,
which is the moisture source region for our site. We therefore argue that our cellulose
record documents convective intensity over the IPWP. On an interannual basis,
convection over the IPWP is modulated by ENSO. Our cellulose record compares well
with ENSO indices as well as coral δ
18
O records from the tropical Pacific Ocean that
have been used to reconstruct ENSO.

Our study suggests tree cellulose δ
18
O from tropical coastal regions is a robust, high-
resolution terrestrial proxy for hydrological conditions over tropical oceans, and could
potentially be used to reconstruct ENSO. As a terrestrial proxy, it complements the
marine proxy of coral, and it also possesses the advantage of precise chronology.
However, the growth patterns of trees must be better constrained in order to extend this
application to monthly or seasonal resolution using sub-ring measurements. In addition,
over most of the low elevation tropics, trees do not exhibit prominent growth bands that
reflect annual growth behavior. Still, promising work has been done using tropical trees
without visible ring structures (Anchukaitis and Evans, 2010). We therefore believe that
103

our study will motivate additional work on trees in reconstructing tropical climate
variability.

104

Chapter Six

Rapid Warming of the Tibetan Plateau and Monsoon
Strengthening

Summary
Stable isotopes of trees are studied on the Tibetan Plateau to investigate hydroclimate
changes with multiple moisture sources. At present, the southern Tibetan Plateau is
influenced by the summer monsoon and its precipitation δ
18
O exhibits amount effect,
whereas the northern Tibetan Plateau is dominated by westerlies carrying continental
recycled moisture and displays temperature effect in its precipitation δ
18
O. We analyzed
the cellulose δ
18
O in annual resolution for tree samples collected from two sites on the
plateau that form a latitudinal transect. The results were well replicated from multiple tree
cores at the same site. The δ
18
O timeseries from the northerly site correlates positively
with May to June temperature and negatively with May to August relative humidity.
Decadal variations in the past 500 years indicate cold and/or wet episodes such as 1590-
1620 and 1890-1910, and the late 20th century stands out as the warmest and/or driest
period. During the instrumental period the annual cellulose δ
18
O values at the southerly
site are indicative of a rainfall amount effect. We interpret the δ
18
O differences between
the two sites as an indicator of the monsoon’s spatial reach over the plateau. We observe
a more regionally expanded summer monsoon over the plateau since the 1940s compared
to the past two centuries.

105

6.1. Introduction
The Tibetan Plateau (TP) provides heat to the mid-troposphere and plays a pivotal role in
creating the land-sea thermal contrast that is believed to be the driving force of the
summer monsoon flow (Wang et al., 2008). Surface warming over the TP would
therefore strengthen the land-sea thermal contrast and enhance the summer monsoon flow
from both India and East Asia. Instrumental records from the TP, which are only
available for the past few decades, document warming during the late 20th century that is
greater than the global or hemispheric mean (Duan and Wu, 2006; Liu and Chen, 2000).
This enhanced warming over the TP is believed to be an altitudinal effect where the
upper troposphere has warmed more rapidly than the lower troposphere (Diaz and
Graham, 1996). Yet despite the enhanced warming over the TP , the monsoon winds in
East Asia are reported to have weakened in recent decades (Ding et al., 2008; Wang,
2001), and the Indian Summer Monsoon precipitation over the southern TP also has
decreased (Duan et al., 2006; Wu, 2005). These weakened aspects of the monsoon are
counter-intuitive since the strength of the summer monsoon is a function of the
temperature/pressure gradient between the land and ocean, and should be positively
related to warming of the TP and the Asian landmass (Webster et al., 1998). The recent
changes may therefore be somewhat unique when compared with monsoon variability
prior to the anthropogenic era (Anderson et al., 2002; Clemens and Prell, 2007; Overpeck
et al., 1996). On the other hand, the instrumental period for which temperature and
precipitation over the TP are available is short and much of what has been learned about
106

past monsoon variability has been gleamed from proxies that do not measure temperature
or precipitation directly.

In this study we evaluate whether or not the recent atmospheric warming and decreased
monsoon rainfall is unique from previous periods. In particular, we apply a new
methodology to recover both temperature and precipitation histories at high elevation
sites on the TP, which extends instrumental records beyond the 20th century. We
compare these extended proxy records to their late 20th century counterparts in order to
assess whether temperatures over the TP are consistently amplified relative to the global
mean during past several centuries and whether monsoon strength has changed during the
late 20th century compared to previous centuries. There have been previous studies that
utilized proxies such as ice cores (Thompson et al., 1989; Thompson et al., 2006;
Thompson et al., 1997; Thompson et al., 2000), lake sediments (Ji et al., 2005; Morrill et
al., 2006; Zhang et al., 2003a) as well as tree ring widths and densities (Cook et al., 2010;
Li et al., 2008; Liang et al., 2008; Shao et al., 2005) to reconstruct pre-20th century
climate on the TP. However, there are critical gaps in the spatial array of data from the
TP and a scarcity of inter-comparison studies. This has led to ambiguous interpretations
of what the pre-20th century temperature history has been over the TP and also how
precipitation varied in relation to the temperature history (Bao et al., 2003; Brauning and
Mantwill, 2004). Here we utilize the oxygen isotopic composition (δ
18
O) of tree cellulose
from annual rings of long-lived trees that grow at sites along a north-south transect from
the central to northern TP. This transect provides a more complete spatial representation
107

of temperature and precipitation across the plateau, and allows for precise inter-
comparison between sites. Data from these sites are combined with an existing record
from the southeast TP (Shi et al., 2011). The three sites form a latitudinal transect that
allows us to infer past changes in the interplay of different moisture sources including the
summer monsoon on the TP, as well as hydroclimate reconstructions at each different
locations. The results are further discussed to resolve the relationship between
temperature and monsoon circulation on the TP.

6.2. Oxygen isotopes on the Tibetan Plateau
6.2.1. Precipitation δ
18
O

Figure 6.1. a) Map of the Tibetan Plateau showing tree sampling sites XDC and TDB of this study. The
other square is the tree cellulose site of Bomi (Shi et al., 2011). Ice core sites are represented by triangles.
Arrows show the atmospheric circulation pattern in the summer rainy season. Shaded region approximates
the present northward extent of the summer monsoon influence. b) This map corresponds to the boxed
region in a, showing our two tree sites in squares and their nearby meteorological stations in filled circles.
Another square to the north of XDC represents the tree cellulose site in the study of Liu et al. (2009).

108

Throughout most of the tropics and the monsoon region, the oxygen isotopic composition
of precipitation varies inversely with the amount of rainfall, the amount effect, wherein
the heavy isotopes are preferentially distilled from the vapor and the remaining
precipitation becomes increasingly depleted in δ
18
O as rainout proceeds (Araguas-
Araguas et al., 1998). On the other hand, at higher latitudes and at higher elevations, the
isotopic fractionation increases as temperature decreases and thus, the δ
18
O of
precipitation is more depleted at cooler temperatures (Dansgaard, 1964). These two
isotope effects influence the summer precipitation in different parts of the TP. In the
south, the Indian Summer Monsoon carries moisture that originates from the tropical
Indian Ocean and from the Bay of Bengal northeastward towards the TP. Much of this
moisture is precipitated along the southern slopes of the Himalayas. The remaining
monsoon moisture makes its way to the southern part of the plateau through the great
river valleys in the east (Fig. 6.1). The monsoon moisture becomes progressively
depleted in δ
18
O along this moisture pathway due to the amount effect. The topographic
lift and progressive rain-out results in δ
18
O values of precipitation as low as ~ -20‰ over
southern part of the TP. (Tian et al., 2003; Zhang et al., 2001). The northern TP is far
from the influence of the summer monsoon moisture. Precipitation here is derived
primarily from recycled continental moisture that is delivered by mid-latitude westerlies.
The recycled moisture originates from the evaporation of surface water, which is
generally more isotopically enriched (Hsieh et al., 1998). Instrumental observations yield
precipitation δ
18
O values that are typically ~ -5‰ in the northern part of the plateau (Tian
et al., 2001), distinctly different from that in the southern TP. In this mid-latitude region
109

without monsoon influence, the precipitation δ
18
O exhibits a positive correlation with
temperature (Thompson et al., 2003). In summary, instrumental observations from the
past few decades reveal two moisture sources on the TP during the summer rainy season.
Southern TP is influenced by the Indian Summer Monsoon that is characterized by
amount effect and depleted precipitation δ
18
O, whereas precipitation in northern TP
derives from continental recycled moisture that is isotopically enriched and exhibits
temperature effect.

6.2.2. Ice core δ
18
O
Several ice cores from the TP have been analyzed for δ
18
O (Fig. 6.1). The isotopic values
in the Dunde ice core from the northern TP (Thompson et al., 1989), Guliya ice core from
the western TP (Thompson et al., 1997), Puruogangri ice core from the central TP
(Thompson et al., 2006), and Malan ice cap from Kunlun Mountains in the northern TP
(Ninglian et al., 2003) well correlate with instrumental temperature records. In contrast, a
70-year ice core record from Tanggula Mountains from the central plateau (Joswiak et
al., 2010) exhibits no correlation with air temperatures. However, the δ
18
O values from
this core correlate well with upstream precipitation amount over the Indian subcontinent,
the amount effect. The δ
18
O values in the Dasuopu ice core located in the Himalayas
(Thompson et al., 2000) are also influenced by the precipitation amount effect. But over
the longer-term history this record appears to be recording temperature changes as well
(Thompson et al., 2000).

110

Figure 6.2. a) Ice core δ
18
O in decadal resolution for the past millennium from Dunde (red), Puruogangri
(green), and Dasuopu (blue). b) Annual cellulose δ
18
O averaged from the different cores at the same site for
XDC (red), TDB (green), and the annual cellulose δ
18
O from a previous study in Bomi (blue). Bold black
lines are 40-year low-pass filter.

Here we use the Dunde, the Puruogangri, and the Dasuopu ice cores to illustrate the
latitudinal distribution of oxygen isotopes across the TP over the last millennium (Fig.
6.2a). The Dunde ice core in the north exhibits the most enriched δ
18
O values, about 10‰
more enriched than the southerly Dasuopu ice core. And the δ
18
O of Puruogangri ice core
in the central TP fluctuates between values that are either similar to Dasuopu or Dunde
(Fig. 6.2a). All three ice core records are affected by temperature changes over the past
111

millennia (Thompson et al., 2003). But based on these records alone, it is not clear how
monsoon variability would be expressed in the isotopic variability. For example, a
stronger monsoon would expand the region over which the amount effect influences the
precipitation δ
18
O. In this sense, the fluctuations in δ
18
O observed in the Puruogangri core
may be indicative of such monsoon variability. Adding additional records across the
region, particularly to the eastern portions of the plateau, where the great valleys serve as
a conduit of the summer monsoon moisture, would clarify how the monsoon amount
effect has affected the δ
18
O variability observed in the ice core records. The oxygen
isotopic composition of tree cellulose can provide additional spatial coverage and thereby
extend our understanding of how monsoon variability has influenced the hydrology over
the plateau over the past several centuries.

6.2.3. Tree cellulose δ
18
O
The oxygen in tree cellulose stems from soil water that is taken up through the tree’s
roots during growth, therefore the δ
18
O of tree cellulose is primarily related to the δ
18
O of
precipitation that falls at the tree site (Sternberg, 2009) with a possible lag due to soil
infiltration and mixing. During growth, the water that is transported to the leaves for
photosynthesis is subject to evaporative isotopic enrichment depending on the relative
humidity of the ambient environment. The final product of photosynthesis, cellulose,
therefore carries an isotopic effect that is negatively related to relative humidity (Roden
et al., 2000). We first evaluate the relative importance of precipitation δ
18
O vs. relative
humidity in the cellulose δ
18
O by comparing the cellulose measurements with
112

instrumental climate parameters in the late 20th century. We then assess how amount
effect and temperature effect would manifest in the isotopic composition of the
precipitation at different latitudes on the TP as inferred from the cellulose δ
18
O. The
cellulose δ
18
O timeseries provides insights into the hydroclimate history of each location.
The inter-comparison between different sites will be used to infer past changes in the
spatial influence of the summer monsoon by referencing to two characteristics of
monsoon moisture, i.e. the depleted δ
18
O values and the amount effect.

6.3. Methods
We have analyzed cellulose from Qilian juniper (Sabina przewalskii) trees from two sites
on the eastern TP (Fig. 6.1). Site TDB (34.79° N, 100.81° E, 3500m) is located in
Animaqing Mountains in the central part of the eastern TP. The other site XDC (38.07° N,
100.25° E, 3500m) is located in the middle of Qilian Mountain, which is the northern
limit of the TP. Qilian juniper from this region have been cross dated and the tree ring
widths have been used previously to reconstruct precipitation, temperature and stream
flow over the past two thousand years (Gou et al., 2007; Gou et al., 2008; Li et al., 2008;
Shao et al., 2005; Sheppard et al., 2004; Zhang et al., 2003b). In the current study
multiple cores were obtained from living Qilian juniper trees. After cross dating, we
selected four cores from each site for isotope analysis. Annual wood samples were cut
from each core and were then ground to a powder. The α-cellulose was extracted from
each sample using the modified Brendal method (Gaudinski et al., 2005). The oxygen
isotopic ratios were measured with a Thermo Finnigan TC/EA coupled with a Delta V
113

Advantage IRMS. The oxygen isotopic ratios are expressed in per mil units of δ
18
O with
respect to vSMOW. The precision of analytical measurements was 0.3‰ based on
repeated measurements of international standards.

6.4. Results
6.4.1. Reproducibility

Figure 6.3. Annual measurements of cellulose δ
18
O for the four tree cores from site TDB (a) and XDC (b).

The δ
18
O values of annual cellulose samples are shown in Figure 6.3 from four tree cores
at each sampling site. The isotope chronology for Site TDB extends to 1800 AD. The
chronology for Site XDC extends to 1497 AD. Some cores were not analyzed
continuously either because there are missing intervals or the rings were too narrow or
were not sufficiently distinguishable. Visually, the δ
18
O stratigraphies from each of the
cores at the same site are well matched with one another. A linear correlation coefficient
114

between any two cores at the same site is greater than 0.67 except for cores TDB05A and
TDB28A, which have only 9 overlapping years (Table 6.1 and 6.2). To further evaluate
the strength of a common signal shared among cores from a single site, we adopt the
Expressed Population Signal (EPS) (Wigley et al., 1984) defined as

̂ ( ) ̂
where n is the number of replicated records, and ̂ is the mean of correlation coefficient
between all possible pairs of records. An EPS value larger than 0.85 is believed to
indicate good replication. The EPS value for the four cores at TDB site is 0.92 (0.94 after
excluding the correlation between TDB05A and TDB28A), and 0.91 for the XDC cores,
suggesting that our δ
18
O is well replicated. The four cores at each site are then averaged
to get a single timeseries of annual cellulose δ
18
O (Fig. 6.2b).

Table 6.1. Correlation coefficients between the cellulose δ
18
O values of different cores at XDC

R 47A 32A 42A 44A
47A 1.00 0.67 0.74 0.70
32A

1.00 0.77 0.69
42A

1.00 0.74
44A 1.00

Table 6.2. Correlation coefficients between the cellulose δ
18
O values of different cores at TDB

R 05A 27A 28A 99A
05A 1.00 0.79 0.48 0.78
27A

1.00 0.88 0.88
28A

1.00 0.92
99A 1.00

115

6.4.2. The δ
18
O relationship to climate parameters
Previous studies, and our field experience, indicate that the junipers growing at high-
elevations on the TP carry out most of their annual growth during the summer months
between May and August (Liang et al., 2006; Rossi et al., 2007). Low relative humidity
during the growth season should act to enrich the leaf water δ
18
O and further the cellulose
δ
18
O, and vice versa. During the growing season the trees utilize meteorological water
that has precipitated during the previous seasons (Liu et al., 2009; Treydte et al., 2006;
Xu et al., 2011). Consequently, the δ
18
O of cellulose should also be a function of the δ
18
O
of precipitation averaged from the previous seasons.

To evaluate how precipitation amount, temperature and changing relative humidity
influence the isotopic record from these trees, the averaged annual timeseries of cellulose
δ
18
O at each site are compared with climate parameters at nearby meteorological stations.
For TDB, three meteorological stations Tongde (AD 1954-1998), Zeku (AD 1958-1990)
and Henan (AD 1959-2011) are almost at equal distance (~60 km) from the sampling site,
whereas site XDC is ~10 km to the south of Qilian (AD 1956-2011) meteorological
station (Fig. 6.1). We correlate cellulose δ
18
O at TDB and XDC with monthly
temperature, precipitation, and relative humidity data from their respective nearby
meteorological stations. Because precipitation accumulated through previous season prior
to the growth could be used as the source water for tree growth, we calculate the
correlation coefficient between our annual cellulose δ
18
O and the climate parameters for
each month from the January of previous year to the current year’s December (Fig. 6.4).
116

Figure 6.4. Correlation between cellulose δ
18
O and climate parameters for different months from previous
year (-) to the current year. TDB cellulose δ
18
O is correlated with the climate parameters from its nearest
three meteorological stations Tongde (a), Zeku (b) and Henan (c); and XDC cellulose δ
18
O is correlated
with the climate parameters from its nearest meteorological station Qilian (d). Solid lines represent 95%
significance level.

For the southerly TDB site, the annual cellulose δ
18
O values exhibit significant positive
correlations with November-December temperatures of the previous year at two of the
117

nearby meteorological stations, Tongde and Zeku (Fig. 6.4a and b). However, the
correlation coefficients with temperature are negative for all months at the third
meteorological station Henan (Fig. 6.4c). The correlations between cellulose δ
18
O and
relative humidity are similar to those between cellulose δ
18
O and precipitation at all three
meteorological stations (Fig. 6.4a, b and c). We interpret this to reflect the influence
precipitation has on local humidity (e.g. more rainfall leads to higher humidity). Relative
humidity and precipitation from August to November of the previous year are negatively
correlated with cellulose δ
18
O at all three meteorological stations. There are also
correlations, albeit weaker, with relative humidity and precipitation during spring to
summer months of the current year (Fig. 6.4a, b and c). We sum up the total precipitation
from August of the previous year to July of the current year at each of the three nearby
meteorological stations. Their correlations with the TDB cellulose δ
18
O are strongly
negative (r = -0.62, -0.42, and -0.69 for Tongde, Zeku and Henan, respectively). This
supports our supposition that these trees use precipitation that integrates moisture from
the previous season. If we take cellulose δ
18
O to be a surrogate for precipitation δ
18
O, the
negative correlation with precipitation amount, particularly during the summer months,
would imply that the δ
18
O of rainwater in TDB area is dominantly influenced by the
amount effect as expressed in summer monsoon rainfall during for the past five decades.

The cellulose δ
18
O at the northerly XDC site however, exhibits weaker correlation with
the monthly climate parameters at the Qilian meteorological station (Fig. 6.4d). The
prominent feature is the negative correlation between cellulose δ
18
O and relative
118

humidity during May to August of the current year, which is the growth season. The
correlation between May to August mean relative humidity and XDC cellulose δ
18
O is r =
-0.57, underscoring the effect of relative humidity has on the isotopic enrichment of leaf
water during the growth season. There is also positive correlation with May and June
temperatures of the same year, the May-June mean temperature correlates with XDC
cellulose δ
18
O at r = 0.45. This might be an indication of the temperature effect on
precipitation δ
18
O at this northerly site.

6.5. Discussion
6.5.1. Comparison with a previous study
Previously, Liu et al. (2009) studied the cellulose δ
18
O of Qinghai spruce (Picea
crassifolia) at a location which is only ~50 km to the north of XDC (Fig. 6.1b). They
found a correlation with November to February temperature. However, their δ
18
O values
are dramatically different from ours, particularly their large interannual variability of up
to 8‰ during the 1940s to 1970s, which is absent from out results (Fig. 6.5a). Their
record also exhibits a negative trend from the 1870s to the 1930s, whereas no trend is
evident in our record. We doubt whether the large amplitude of variability observed in
their record is reflective of the climate variables. Their tree site is located on the north
slope of the Qilian Mountain, which is the northern limit of the plateau (Fig. 6.5b). The
isotopic composition of surface water over the lowlands in the north of the plateau may
be quite different from surface moisture on the plateau. Winds from the north that pick up
the surface moisture in the lowlands and pass through the Liu et al. (2009) site might
119

cause quite different isotopic signatures in the precipitation from winds that transport
moisture northward from the plateau. The large interannual shifts as well as long-term
trends in their record might be affected by these dynamics, instead of representing the
mean climatological conditions on the plateau. On the other hand, different methods of
sample processing in their study might also be responsible for the discrepancies. In their
study, Liu et al. (2009) pooled annual wood samples from eight cores before milling and
only generated one annual timeseries of δ
18
O. This technique does not guarantee
replication if the cores were not properly dated. Moreover, a different cellulose extraction
method (Green, 1963; Loader et al., 1997) was adopted in their study. If the different
extraction methods are the culprit, this raises serious questions to the evaluation and
interpretation of previous cellulose isotope results. Overall, more research and analysis
need to be done to resolve the discrepancies between their results and ours.

Figure 6.5. a) The disagreement between our XDC cellulose δ
18
O (red) and the cellulose δ
18
O from a
previous study (Liu et al., 2009) that is only ~50 km away. b) A sketch showing the topographic profile
through our site XDC and the site of Liu et al. (2009).
120

6.5.2. Latitudinal gradient of δ
18
O
As described previously, three ice core records that form a latitudinal transect document
the spatial contrast in δ
18
O of precipitation on the TP, which is related to different
moisture sources (Fig. 6.2a). A similar pattern is therefore also expected in tree cellulose
δ
18
O. Recently, Shi et al. (2011) studied the cellulose δ
18
O of Linzhi spruce (Picea
likiangensis var. lintziensis) at Bomi in the southeast TP. Along with their record, our
cellulose δ
18
O records from XDC and TDB form a north-south transect that is located
along the summer monsoon northward pathway (Fig. 6.1). The cellulose δ
18
O values
exhibit a latitudinal gradient that resembles the ice cores, most depleted at the
southernmost site, Bomi, and most enriched at the northernmost site, XDC (Fig. 6.2b).
But the amplitude of this latitudinal gradient is smaller than that of the ice core records
(Fig. 6.2a). We interpret the larger δ
18
O gradient in the ice core records to reflect an
amplification that is associated with elevation differences because Dunde, Puruogangri,
and Dasuopu ice cores were cored at 5325m, 6072m, and 7200m, respectively. The uplift
of moist air and the colder temperature would have depleted the oxygen isotopes in
precipitation at the higher elevation sites. Conversely, all of the tree sites are at similar
and lower altitudes (3500 m for both XDC and TDB, 2760 m for Bomi). Hence, the δ
18
O
differences between the cellulose records are not reflecting an altitudinal effect. The
latitudinal range reflected in the three ice core records is also larger than that of the tree
sites. This may as well contribute to a greater δ
18
O gradient in the ice core records
compared to the tree records. On the other hand, unlike ice core δ
18
O, cellulose δ
18
O is
121

also influenced by relative humidity. Differences in relative humidity at each tree site
may also affect the magnitude of the latitudinal δ
18
O gradient documented from cellulose.
If relative humidity differences were responsible, the smaller latitudinal δ
18
O gradient in
the cellulose records would require that the northerly site is wetter than the southerly site.
However, this is not the case. The southern site is influenced by the summer monsoon
where the humidity is higher than it is to the north. The long-term mean values of
monthly relative humidity show that the southernmost meteorological station Bomi is
more humid in every month than the northern most station Qilian (Fig. 6.6a). Relative
humidity is therefore less likely to be the explanation of the smaller latitudinal gradient in
cellulose δ
18
O.

Figure 6.6. a) The long-term mean monthly relative humidity at Bomi, Tongde, Zeku, Henan and Qilian
meteorological station. b) The difference in growth season (May to August) relative humidity between
Tongde, Zeku, Henan, which represent TDB tree site, and Qilian, the nearby meteorological station of
XDC tree site.

We use the cellulose δ
18
O as a representation of precipitation δ
18
O gradient between the
tree sites. The Bomi cellulose δ
18
O is correlated with varying cloud cover, which reflects
regional precipitation amount. During the instrumental period of the past five decades,
the TDB cellulose δ
18
O is best correlated with instrumental precipitation amount of the
previous year. Besides effect of leaf evaporative enrichment due to relative humidity, the
122

XDC cellulose δ
18
O also shows correlation with temperature, indicating the temperature
effect on precipitation δ
18
O. We therefore believe that the cellulose δ
18
O records depict a
spatial pattern of precipitation δ
18
O and moisture source that is consistent with both
instrumental observations and ice core δ
18
O records, i.e. southern TP is associated with
depleted δ
18
O and amount effect of monsoon whereas northern TP is characterized by
enriched δ
18
O and temperature effect of westerlies.

6.5.3. Variability of monsoon circulation
Based on meteorological stations on the plateau that measure the δ
18
O of precipitation in
the past few decades, the dividing line between the isotope “amount effect” influence and
the “temperature effect” influence, i.e. the northward extent of the summer monsoon, is
drawn around 35° N in the central TP (Araguas-Araguas et al., 1998; Tian et al., 2007; Yu
et al., 2008) (Fig. 6.1). However, this northward extent might have changed under
different climate conditions. For example, the monsoon moisture shifted to 40° N during
the warmer early to mid-Holocene (Winkler and Wang, 1993). Inter-comparisons
between paleoclimate records from north to the south of the TP could bring insights into
understanding the monsoon variability.

The longer-term trends in δ
18
O of the Dasuopu ice core record have been interpreted to
reflect temperature over the plateau, despite the observation that the higher frequency
δ
18
O variability during the 20th century portion of the record is related to varying
amounts of monsoon precipitation (Tandong et al., 2007; Thompson et al., 2003). We
123

believe this argument is plausible if Dasuopu has always been under the influence of the
summer monsoon. However, sites in the central TP are located in the frontal regions of
the monsoon moisture, and should be sensitive to the variability of the monsoon strength.
In the central TP, both Puruogangri ice core and TDB cellulose appear to have larger
interannual and decadal variance in the δ
18
O values than their northerly and southerly
counterparts (Fig. 6.2). We suspect this feature implies changes of monsoon influence on
the TP. When summer monsoon winds are strong, moisture with characteristically
depleted δ
18
O values and associated amount effect shifts δ
18
O of precipitation (and
cellulose) lower across the central portion of the TP. On the other hand, at times when the
monsoon circulation weakens, the central TP is dominated by precipitation carried by
westerlies, which exhibits temperature effect and more enriched δ
18
O values. Thus, the
δ
18
O values of precipitation (and cellulose) in the central TP are more similar to the
values across the northern TP. We therefore suggest that intervals when TDB cellulose
δ
18
O values diverge from XDC cellulose δ
18
O should represent episodes of enhanced
summer monsoon (Fig. 6.2b).

The difference in cellulose δ
18
O between XDC and TDB remains small until ~1940,
when the two timeseries of cellulose δ
18
O start to diverge. This difference peaks around
the 1970s, and then decreases towards present time (Fig. 6.2b, Fig.6.7). It is likely that
the trees we study at both sites share the same growth pattern as well as physiological
responses as they are the same species growing at similar altitudes. Therefore the
difference in cellulose δ
18
O between XDC and TDB is most likely attributed to
124

differences in relative humidity and/or precipitation δ
18
O. In the late 20th century when
the instrumental measurements are available, the total amplitude of change in the δ
18
O
difference between XDC and TDB is ~2‰. Specifically, there is a long-term decreasing
trend of ~2‰ from the 1970s to 2000 (Fig. 6.7). According to the geochemical model of
cellulose δ
18
O (Roden et al., 2000; Sternberg, 2009), this requires the relative humidity
difference between the two sites to decrease by ~10% if the influence of precipitation
δ
18
O is ignored. However, there is no long-term trend in the relative humidity difference
between the two sites from the 1950s to present (Fig. 6.6b). The difference in cellulose
δ
18
O between the two sites (Fig. 6.7) is therefore attributed to the difference in
precipitation δ
18
O.

Figure 6.7. The difference of cellulose δ
18
O between XDC and TDB. Larger difference implicates stronger
summer monsoon. Bold black lines are 20-year low-pass filter.

Since XDC is located in a continental climatic region where the moisture is dominated by
continental recycled water and exhibits temperature isotope effect (Araguas-Araguas et
al., 1998; Tian et al., 2001), the isotopic difference in cellulose δ
18
O between XDC and
TDB may be a measure of summer monsoon strength. Based on this interpretation,
125

monsoon has been relatively strong from the 1940s to present compared to the past two
centuries (Fig. 6.7), in agreement with our observation that TDB cellulose δ
18
O exhibit
amount effect in the last five decades when instrumental records are available. Prior to
the 1940s, the diminished difference in δ
18
O between TDB and XDC indicate a less
influence of monsoon moisture or amount effect. This is also supported by Tanggula ice
core results (Joswiak and Yao, 2011), which indicates a transition from westerly moisture
regime to monsoon influence in the central part of the TP during the 1940s. The decade
of the 1800s also seems to have experienced stronger monsoon. Extension of these
records prior to 1800 is critical to examine whether monsoon was stronger during the
Little Ice Age, as suggested by other studies (Brauning and Mantwill, 2004; Zhang et al.,
2003a). Moreover, we observe a trend of monsoon weakening after 1970, which supports
a few observations that suggest both the Indian Summer Monsoon and the East Asian
summer monsoon circulations have been weakening in recent decades (Ding et al., 2008;
Duan et al., 2006; Wang, 2001; Wu, 2005).

6.5.4. Hydroclimate history of the northeast Tibetan Plateau
The XDC cellulose δ
18
O correlates negatively with relative humidity and positively with
temperature during the instrumental period. Therefore, low δ
18
O values are associated
with cold and/or wet conditions, and vice versa. The XDC record that extends back to
1497AD reveals 1590-1620 and 1890-1910 as the coldest and/or wettest episodes (Fig.
6.2b). An isotopically anomalous interval spanning 1590-1620 is also commonly
observed in speleothem δ
18
O records such as Wangxiang Cave in China (Zhang et al.,
126

2008) and caves in India (Sinha et al., 2011). Similarly, the anomalous interval of 1890-
1910 is also observed in Dayu Cave in China (Tan et al., 2009). These speleothems
exhibit more enriched δ
18
O values in these intervals, which have been interpreted to
reflect weaker monsoon rains. These speleothem records provide indirect evidence that
the XDC cellulose δ
18
O from the northeastern TP are not affected by summer monsoon,
otherwise the two intervals of 1590-1620 and 1890-1910 in the cellulose δ
18
O would
have followed the speleothems and been more isotopically enriched. On the contrary, the
monsoon strengths documented in the speleothem records are attributed to solar forcing
and temperature variability over the Eurasia landmass. Weakened monsoon during these
two intervals are associated with Eurasia cooling events such as the advances of Swiss
Apline glaciers (Zhang et al., 2008). We believe this is consistent with the cooling
observed in our XDC cellulose record.

In the XDC cellulose δ
18
O, the 20th century after 1930 stands out as more isotopically
enriched and is thus interpreted as the warmest and/or driest interval in the past 500 years
(Fig. 6.2b; Fig. 6.8). The problem remains differentiating between the temperature and
the humidity signals from the XDC cellulose δ
18
O. Empirically, the precipitation δ
18
O has
a sensitivity of ~0.5 to 0.7 ‰/°C in the northern TP (Tian et al., 2003; Zhang et al., 2001).
If we assume temperature is the only signal reflected in the cellulose δ
18
O values, the
XDC record implies a 3 to 4 ° C warming during the late 20th century compared to the
pre-industrial values over the northeast TP, which is in similar magnitude as reflected in
the Dunde ice core (Fig. 6.8). This is higher than the warming shown in the Northern
127

Hemisphere temperature reconstruction (Mann et al., 1999), therefore it might suggest an
amplified warming at higher elevations (Liu and Chen, 2000; Thompson et al., 2003). If
we assume this late 20th century warming seen in the XDC cellulose record represents a
general warming over the whole TP or even the larger Eurasian landmass, it corresponds
to the stronger monsoon influence during the late 20th century as observed from the TDB
cellulose record. However, this is no corresponding trend that explains the weakening of
monsoon since 1970.

Figure 6.8. XDC cellulose δ
18
O plotted with Northern Hemisphere temperature reconstruction and Dunde
ice core δ
18
O. Bold black lines are 40-year low-pass filter.

6.6. Conclusions and implications
Cellulose δ
18
O has been analyzed for Qilian juniper from two locations on the eastern
Tibetan Plateau. The northerly site XDC is located in the westerly-dominated region
128

where stable isotopes of precipitation are influenced by a temperature effect. At this site,
the cellulose δ
18
O record extends back to 1497 AD, and reveals coldest and/or wettest
climate conditions during 1590-1620 and 1890-1910, which correspond to weaker
monsoon as documented in several speleothem records. The late 20th century is the
warmest and/or driest episode during the past 500 years in this region. This warming
might be faster than the northern hemispheric mean temperature.

The other site TDB is located near the current northward extent of the summer monsoon
and extends back to 1800. Its cellulose δ
18
O shows larger interannual and decadal
variations than XDC, indicating time-varying influences from both westerlies and
monsoon. This record suggests summer monsoon precipitation has been the dominant
influence on the central Tibetan Plateau since the 1940s compared to previous time. The
stronger monsoon might be related to the rapid late 20th century warming as indicated in
the XDC record. However, a weakening trend of the monsoon is observed after 1970 that
seems unexplainable from the other cellulose record.

We believe tree cellulose δ
18
O is a good tool to examine the variability of temperature as
well as circulation patterns on the Tibetan Plateau for recent centuries. Compared to ice
cores, the annually resolved tree records can be precisely dated and are more widely
distributed over the plateau. However, more effort is needed to distinguish the mix of
signals in cellulose δ
18
O. For instance, a multi-proxy approach of analyzing both the
carbon and oxygen isotopes would help to elucidate this matter, and inter-comparison
129

between multiple sites like this study would give better spatial view of the climate history
on the plateau. We also believe more records of this kind are needed in order to resolve
the relationship between temperature and monsoon strength on the Tibetan Plateau.

130

Chapter Seven

Conclusions

Tree cellulose δ
18
O studies that are included in this dissertation were aimed to answer the
following questions related to the Indian Monsoon and ENSO as raised in the
Introduction Chapter.

i. How has the monsoon precipitation changed with the observed warming
trend?
There is a growing consensus that with global warming, the enhanced atmospheric
moisture content is the dominant effect on the monsoon and it results in stronger
monsoonal precipitation particularly in the tropical regions (IPCC, 2007). However,
instrumental records of rainfall over India do not indicate any significant trend in the past
130 years (Parthasarathy et al., 1994). The interannual variability of a tree cellulose δ
18
O
record from a montane forest site in northern Thailand exhibits negative correlation with
the rainfall over both India and Mainland Southeast Asia and is therefore interpreted to
reflect monsoon variability. Similar to the instrumental precipitation records, the
cellulose δ
18
O record does not exhibit any long-term trend in the 20th century to indicate
the effect of global warming. It should be noted that the cellulose δ
18
O explains less than
30% of the precipitation variance, and we must take caution using it as a proxy record for
monsoon. Other evidence is needed to corroborate the observation that there is no trend
in monsoonal precipitation associated with warming in South and Southeast Asia before
131

further investigations could be made to look into the disagreement between theories and
observations.

ii. Has the monsoon circulation varied in the same way as the monsoon
precipitation?
The monsoon circulation represents the strength of the monsoonal winds. In particular,
the strength of the monsoonal winds determines the northern extent of the monsoon
influence. One of the major factors that affect the strength of the monsoon circulation is
the land-sea thermal gradient. Global warming induces larger land-sea thermal gradient
(Douville et al., 2000). However, climate models show that the effect of this larger land-
sea thermal gradient is balanced by an increase in dry static stability associated with
tropical warming, which results in weaker monsoon as well as other tropical large-scale
circulations (Betts and Ridgway, 1989; Knutson and Manabe, 1995). Although no 20th
century trend is observed in the monsoonal precipitation in southern parts of the Indian
Monsoon region, tree cellulose δ
18
O records from sites on the Tibetan Plateau suggest the
monsoon influence has possibly shifted to a more northerly extent since 1940 as
compared to the past two centuries, which has brought the monsoon influence to a wider
geographic extent on the Tibetan Plateau. This increased monsoon flow possibly relates
to the warming of the 20th century, which would corroborate the land-sea thermal
gradient theory. However, the cellulose records also show evidence that indicates an
apparent weakening trend of the monsoon circulation after 1970. Although this
weakening aspect agrees with other reports (Wang, 2001; Wu, 2005), there currently is
132

no convincing explanation for this weakening. These results demonstrate that circulation
strength is a different measure of the monsoon from precipitation amount. They do not
vary in the same fashion, thus future investigations of monsoon dynamics need to
consider these two aspects.

iii. Is the influence of ENSO on the monsoon a stationary phenomenon?
ENSO is the dominant factor that affects the interannual variability of the monsoon, with
suppressed monsoon during El Niñ o events (Webster, 1995). The tree cellulose δ
18
O
record from northern Thailand that correlates with monsoon rainfall over India and
Mainland Southeast Asia reveals a weakening relationship between the Indian Monsoon
and ENSO after ~1970, in agreement with previous studies (Kumar et al., 1999;
Singhrattna et al., 2005). This weakening relationship suggests the influence of ENSO on
monsoon is non-stationary, which adds another complexity to monsoon prediction.

iv. How could tree cellulose δ
18
O be used to understand ENSO such as the mean
state of tropical Pacific, and the frequency and amplitude of ENSO events?
In this dissertation, a 140-year tree cellulose δ
18
O record from coastal Cambodia is used
as a proxy for surface hydrology over the IPWP. As the hydrological conditions over the
IPWP is closely related to ENSO variability, this high-resolution cellulose record is also
used to infer information about ENSO. Currently, there is no consensus with regard to the
influence of global climate on ENSO behavior, including the mean state of ENSO and the
frequency and amplitude of ENSO events. The 140-year cellulose record reveals no
133

overall trend in the mean δ
18
O values, which suggests no change in the mean state of
ENSO. However, the 1880s through 1910s are characterized by more positive cellulose
δ
18
O values. This corresponds to a relatively dry condition over IPWP, and possibly
suggests an El Niño-like tropical Pacific. But this interval does not particularly stand out
as a temperature anomaly in the global SST datasets (Brohan et al., 2006; Kaplan et al.,
1998; Smith et al., 2008) or SST reconstructions from tropical coral δ
18
O (Charles et al.,
2003; Cobb et al., 2003; Cole et al., 1993; Quinn et al., 2006; Tudhope et al., 2001;
Urban et al., 2000). On the one hand, cellulose δ
18
O is a proxy for precipitation over the
IPWP. There are uncertainties in the cellulose δ
18
O measurements. On the other hand,
early parts of the instrumental SSTs are interpreted from rather sparse observational
network and disagreement exists between different interpolation techniques (Emile-Geay
et al., in revision). Moreover, coral δ
18
O is not only a function of SST, but also of surface
hydrology. These uncertainties might explain the discrepancies among different types of
observations.

Besides mean state, frequency and amplitude are other parameters to describe ENSO
behavior. The tree cellulose δ
18
O record from Cambodia reveals that the 1920s through
1960s is an interval with smaller ENSO variability, consistent with the observations from
tropical coral δ
18
O records (Charles et al., 2003; Cobb et al., 2003; Cole et al., 1993;
Quinn et al., 2006; Tudhope et al., 2001; Urban et al., 2000). However, in the 140 years
that the cellulose δ
18
O record spans, there is no overall trend in the amplitude of the
interannual variability.
134

The time frame of the Cambodian cellulose study has not extended beyond the
instrumental period or the time period covered by most coral records, and therefore
cannot be utilized to assess the ENSO behavior under different climate backgrounds in
the past millennium such as the Medieval Warm Period or the Little Ice Age. However,
as a proxy calibration study it demonstrates the use of tree cellulose δ
18
O as a proxy for
hydrological variability of tropical oceans that is related to ENSO. As a terrestrial proxy,
tree cellulose δ
18
O augments the high-resolution reconstruction network consisting of
tropical coral δ
18
O. With the advantages such as precise chronology and easy sampling, it
is expected that similar tree cellulose studies will be inspired to extend the observations
back in time, where continuous observations with high temporal resolution are essential
to broaden our knowledge of ENSO.

135

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158

Appendix A. DCK subannual cellulose δ18O values

Core Year Color No. δ
18
O(‰) Age
DCK08A 2000 D 2 24.12 2000.86
DCK08A 2000 D 1 22.86 2000.71
DCK08A 2000 W 5 23.00 2000.57
DCK08A 2000 W 4 22.70 2000.43
DCK08A 2000 W 3 23.65 2000.29
DCK08A 2000 W 2 23.77 2000.14
DCK08A 2000 W 1 23.83 2000.00
DCK08A 1999 M 1 24.46 1999.80
DCK08A 1999 D 1 22.73 1999.60
DCK08A 1999 W 3 22.58 1999.40
DCK08A 1999 W 2 23.95 1999.20
DCK08A 1999 W 1 24.52 1999.00
DCK08A 1998 M 1 24.89 1998.75
DCK08A 1998 D 1 23.36 1998.50
DCK08A 1998 W 2 20.91 1998.25
DCK08A 1998 W 1 21.79 1998.00
DCK08A 1997 M 1 26.59 1997.86
DCK08A 1997 D 1 26.47 1997.71
DCK08A 1997 W 5 24.87 1997.57
DCK08A 1997 W 4 24.95 1997.43
DCK08A 1997 W 3 23.57 1997.29
DCK08A 1997 W 2 23.47 1997.14
DCK08A 1997 W 1 24.02 1997.00
DCK08A 1996 D 1 23.15 1996.83
DCK08A 1996 W 5 21.47 1996.67
DCK08A 1996 W 4 20.27 1996.50
DCK08A 1996 W 3 22.82 1996.33
DCK08A 1996 W 2 23.44 1996.17
DCK08A 1996 W 1 24.22 1996.00
DCK08A 1995 D 2 21.54 1995.80
DCK08A 1995 D 1 21.17 1995.60
DCK08A 1995 W 3 20.71 1995.40
DCK08A 1995 W 2 21.60 1995.20
DCK08A 1995 W 1 23.15 1995.00
DCK08A 1994 D 2 26.31 1994.86
DCK08A 1994 D 1 25.99 1994.71
DCK08A 1994 W 5 23.50 1994.57
DCK08A 1994 W 4 21.12 1994.43
DCK08A 1994 W 3 22.70 1994.29
DCK08A 1994 W 2 23.40 1994.14
DCK08A 1994 W 1 23.97 1994.00
DCK08A 1993 D 2 25.34 1993.86
159

DCK08A 1993 D 1 22.96 1993.71
DCK08A 1993 W 5 21.72 1993.57
DCK08A 1993 W 4 23.15 1993.43
DCK08A 1993 W 3 24.45 1993.29
DCK08A 1993 W 2 24.82 1993.14
DCK08A 1993 W 1 25.51 1993.00
DCK08A 1992 D 1 21.82 1992.67
DCK08A 1992 W 2 21.08 1992.33
DCK08A 1992 W 1 22.39 1992.00
DCK08A 1989 M 1 N/A 1991.00
DCK08A 1989 D 1 22.26 1989.83
DCK08A 1989 W 4 21.34 1989.67
DCK08A 1989 W 3 22.63 1989.50
DCK08A 1989 W 2 23.14 1989.33
DCK08A 1989 W 1 23.69 1989.17
DCK08A 1988 M 1 24.20 1989.00
DCK08A 1988 D 1 23.07 1988.86
DCK08A 1988 W 5 21.11 1988.71
DCK08A 1988 W 4 20.65 1988.57
DCK08A 1988 W 3 20.89 1988.43
DCK08A 1988 W 2 21.50 1988.29
DCK08A 1988 W 1 21.12 1988.14
DCK08A 1987 D 1 23.66 1988.00
DCK08A 1987 W 4 21.74 1987.80
DCK08A 1987 W 3 21.24 1987.60
DCK08A 1987 W 2 22.63 1987.40
DCK08A 1987 W 1 25.11 1987.20
DCK08A 1986 D 2 25.29 1987.00
DCK08A 1986 D 1 24.79 1986.75
DCK08A 1986 W 2 23.19 1986.50
DCK08A 1986 W 1 23.01 1986.25
DCK08A 1985 W 1 23.81 1986.00
DCK08A 1984 D 2 25.57 1985.00
DCK08A 1984 D 1 25.01 1984.83
DCK08A 1984 W 4 22.51 1984.67
DCK08A 1984 W 3 22.02 1984.50
DCK08A 1984 W 2 22.41 1984.33
DCK08A 1984 W 1 22.81 1984.17
DCK08A 1983 D 1 22.85 1984.00
DCK08A 1983 W 2 21.78 1983.67
DCK08A 1983 W 1 20.28 1983.33
DCK08A 1982 D 1 20.45 1983.00
DCK08A 1982 W 2 22.62 1982.67
DCK08A 1982 W 1 21.61 1982.33
DCK08A 1981 D 1 22.70 1982.00
DCK08A 1981 W 3 23.45 1981.75
DCK08A 1981 W 2 22.37 1981.50
DCK08A 1981 W 1 22.62 1981.25
160

DCK08A 1980 W 1 23.32 1981.00
DCK08A 1979 D 1 23.34 1980.00
DCK08A 1979 W 1 25.61 1979.50
DCK08A 1978 D 1 23.92 1979.00
DCK08A 1978 W 5 23.03 1978.83
DCK08A 1978 W 4 21.33 1978.67
DCK08A 1978 W 3 20.63 1978.50
DCK08A 1978 W 2 20.82 1978.33
DCK08A 1978 W 1 20.24 1978.17
DCK08A 1977 D 1 20.39 1978.00
DCK08A 1977 W 3 22.37 1977.75
DCK08A 1977 W 2 22.64 1977.50
DCK08A 1977 W 1 24.04 1977.25
DCK08A 1976 D 2 25.69 1977.00
DCK08A 1976 D 1 24.94 1976.83
DCK08A 1976 W 4 23.02 1976.67
DCK08A 1976 W 3 21.52 1976.50
DCK08A 1976 W 2 20.17 1976.33
DCK08A 1976 W 1 19.66 1976.17
DCK08A 1975 M 1 22.57 1976.00
DCK08A 1975 D 2 24.07 1975.90
DCK08A 1975 D 1 22.73 1975.80
DCK08A 1975 W 7 20.07 1975.70
DCK08A 1975 W 6 19.65 1975.60
DCK08A 1975 W 5 18.90 1975.50
DCK08A 1975 W 4 19.95 1975.40
DCK08A 1975 W 3 20.90 1975.30
DCK08A 1975 W 2 21.00 1975.20
DCK08A 1975 W 1 21.79 1975.10
DCK08A 1974 M 1 23.37 1975.00
DCK08A 1974 D 6 24.79 1974.93
DCK08A 1974 D 5 24.88 1974.86
DCK08A 1974 D 4 24.05 1974.79
DCK08A 1974 D 3 22.41 1974.71
DCK08A 1974 D 2 21.64 1974.64
DCK08A 1974 D 1 21.73 1974.57
DCK08A 1974 W 7 20.88 1974.50
DCK08A 1974 W 6 20.70 1974.43
DCK08A 1974 W 5 21.95 1974.36
DCK08A 1974 W 4 21.50 1974.29
DCK08A 1974 W 3 21.47 1974.21
DCK08A 1974 W 2 23.36 1974.14
DCK08A 1974 W 1 23.75 1974.07
DCK08A 1973 M 1 24.69 1974.00
DCK08A 1973 D 5 25.43 1973.93
DCK08A 1973 D 4 24.64 1973.86
DCK08A 1973 D 3 23.75 1973.79
DCK08A 1973 D 2 21.98 1973.71
161

DCK08A 1973 D 1 20.71 1973.64
DCK08A 1973 W 8 18.93 1973.57
DCK08A 1973 W 7 18.39 1973.50
DCK08A 1973 W 6 17.58 1973.43
DCK08A 1973 W 5 18.12 1973.36
DCK08A 1973 W 4 19.72 1973.29
DCK08A 1973 W 3 19.78 1973.21
DCK08A 1973 W 2 22.44 1973.14
DCK08A 1973 W 1 21.59 1973.07
DCK08A 1972 D 5 22.84 1973.00
DCK08A 1972 D 4 21.83 1972.89
DCK08A 1972 D 3 22.50 1972.78
DCK08A 1972 D 2 22.89 1972.67
DCK08A 1972 D 1 23.57 1972.56
DCK08A 1972 W 4 23.92 1972.44
DCK08A 1972 W 3 24.27 1972.33
DCK08A 1972 W 2 24.17 1972.22
DCK08A 1972 W 1 23.81 1972.11
DCK08A 1971 D 5 25.79 1972.00
DCK08A 1971 D 4 26.06 1971.88
DCK08A 1971 D 3 25.97 1971.75
DCK08A 1971 D 2 23.88 1971.63
DCK08A 1971 D 1 22.69 1971.50
DCK08A 1971 W 3 21.80 1971.38
DCK08A 1971 W 2 22.00 1971.25
DCK08A 1971 W 1 22.88 1971.13
DCK08A 1970 M 1 24.22 1971.00
DCK08A 1970 D 1 24.35 1970.75
DCK08A 1970 W 2 21.67 1970.50
DCK08A 1970 W 1 20.68 1970.25
DCK08A 1969 D 2 23.52 1970.00
DCK08A 1969 D 1 24.41 1969.75
DCK08A 1969 W 2 21.83 1969.50
DCK08A 1969 W 1 21.87 1969.25
DCK08A 1968 D 2 26.43 1969.00
DCK08A 1968 D 1 26.47 1968.75
DCK08A 1968 W 2 22.96 1968.50
DCK08A 1968 W 1 22.51 1968.25
DCK08A 1967 M 1 22.69 1968.00
DCK08A 1967 D 4 23.46 1967.93
DCK08A 1967 D 3 23.86 1967.86
DCK08A 1967 D 2 22.26 1967.79
DCK08A 1967 D 1 23.09 1967.71
DCK08A 1967 W 9 21.39 1967.64
DCK08A 1967 W 8 19.20 1967.57
DCK08A 1967 W 7 19.03 1967.50
DCK08A 1967 W 6 19.72 1967.43
DCK08A 1967 W 5 21.16 1967.36
162

DCK08A 1967 W 4 20.42 1967.29
DCK08A 1967 W 3 22.41 1967.21
DCK08A 1967 W 2 22.94 1967.14
DCK08A 1967 W 1 21.96 1967.07
DCK08A 1966 D 2 23.66 1967.00
DCK08A 1966 D 1 25.61 1966.86
DCK08A 1966 W 5 24.99 1966.71
DCK08A 1966 W 4 23.09 1966.57
DCK08A 1966 W 3 22.80 1966.43
DCK08A 1966 W 2 22.81 1966.29
DCK08A 1966 W 1 21.31 1966.14
DCK08A 1965 D 2 23.86 1966.00
DCK08A 1965 D 1 25.89 1965.91
DCK08A 1965 W 9 24.19 1965.82
DCK08A 1965 W 8 23.40 1965.73
DCK08A 1965 W 7 21.84 1965.64
DCK08A 1965 W 6 21.24 1965.55
DCK08A 1965 W 5 20.88 1965.45
DCK08A 1965 W 4 22.42 1965.36
DCK08A 1965 W 3 22.72 1965.27
DCK08A 1965 W 2 23.12 1965.18
DCK08A 1965 W 1 23.55 1965.09
DCK08A 1964 M 1 25.08 1965.00
DCK08A 1964 D 2 25.33 1964.88
DCK08A 1964 D 1 23.74 1964.75
DCK08A 1964 W 5 22.32 1964.63
DCK08A 1964 W 4 20.09 1964.50
DCK08A 1964 W 3 19.57 1964.38
DCK08A 1964 W 2 20.97 1964.25
DCK08A 1964 W 1 19.93 1964.13
DCK08A 1963 D 2 22.44 1964.00
DCK08A 1963 D 1 25.32 1963.83
DCK08A 1963 W 4 22.65 1963.67
DCK08A 1963 W 3 21.18 1963.50
DCK08A 1963 W 2 20.73 1963.33
DCK08A 1963 W 1 21.24 1963.17
DCK08A 1962 D 3 24.07 1963.00
DCK08A 1962 D 2 26.00 1962.90
DCK08A 1962 D 1 25.35 1962.80
DCK08A 1962 W 7 25.54 1962.70
DCK08A 1962 W 6 23.80 1962.60
DCK08A 1962 W 5 21.45 1962.50
DCK08A 1962 W 4 19.48 1962.40
DCK08A 1962 W 3 19.39 1962.30
DCK08A 1962 W 2 20.27 1962.20
DCK08A 1962 W 1 21.01 1962.10
DCK08A 1961 D 5 23.56 1962.00
DCK08A 1961 D 4 25.16 1961.92
163

DCK08A 1961 D 3 25.27 1961.83
DCK08A 1961 D 2 25.22 1961.75
DCK08A 1961 D 1 23.73 1961.67
DCK08A 1961 W 7 21.03 1961.58
DCK08A 1961 W 6 19.04 1961.50
DCK08A 1961 W 5 19.11 1961.42
DCK08A 1961 W 4 20.58 1961.33
DCK08A 1961 W 3 22.02 1961.25
DCK08A 1961 W 2 22.47 1961.17
DCK08A 1961 W 1 21.88 1961.08
DCK08A 1960 M 1 23.66 1961.00
DCK08A 1960 D 3 24.45 1960.93
DCK08A 1960 D 2 24.22 1960.87
DCK08A 1960 D 1 24.07 1960.80
DCK08A 1960 W 11 23.54 1960.73
DCK08A 1960 W 10 23.68 1960.67
DCK08A 1960 W 9 23.85 1960.60
DCK08A 1960 W 8 22.79 1960.53
DCK08A 1960 W 7 22.29 1960.47
DCK08A 1960 W 6 21.83 1960.40
DCK08A 1960 W 5 21.08 1960.33
DCK08A 1960 W 4 21.66 1960.27
DCK08A 1960 W 3 21.45 1960.20
DCK08A 1960 W 2 22.07 1960.13
DCK08A 1960 W 1 23.26 1960.07
DCK08A 1959 M 1 27.08 1960.00
DCK08A 1959 D 4 27.04 1959.89
DCK08A 1959 D 3 25.47 1959.78
DCK08A 1959 D 2 23.88 1959.67
DCK08A 1959 D 1 21.79 1959.56
DCK08A 1959 W 4 20.34 1959.44
DCK08A 1959 W 3 21.71 1959.33
DCK08A 1959 W 2 23.02 1959.22
DCK08A 1959 W 1 22.12 1959.11
DCK08A 1958 M 1 24.86 1959.00
DCK08A 1958 D 3 28.77 1958.92
DCK08A 1958 D 2 29.07 1958.83
DCK08A 1958 D 1 26.82 1958.75
DCK08A 1958 W 8 26.04 1958.67
DCK08A 1958 W 7 22.37 1958.58
DCK08A 1958 W 6 21.68 1958.50
DCK08A 1958 W 5 20.52 1958.42
DCK08A 1958 W 4 21.08 1958.33
DCK08A 1958 W 3 23.05 1958.25
DCK08A 1958 W 2 23.96 1958.17
DCK08A 1958 W 1 23.25 1958.08
DCK08A 1957 M 1 26.97 1958.00
DCK08A 1957 D 2 29.13 1957.94
164

DCK08A 1957 D 1 29.90 1957.88
DCK08A 1957 W 13 28.31 1957.81
DCK08A 1957 W 12 26.97 1957.75
DCK08A 1957 W 11 25.06 1957.69
DCK08A 1957 W 10 26.60 1957.63
DCK08A 1957 W 9 24.66 1957.56
DCK08A 1957 W 8 25.16 1957.50
DCK08A 1957 W 7 23.74 1957.44
DCK08A 1957 W 6 23.03 1957.38
DCK08A 1957 W 5 21.62 1957.31
DCK08A 1957 W 4 21.18 1957.25
DCK08A 1957 W 3 21.17 1957.19
DCK08A 1957 W 2 21.25 1957.13
DCK08A 1957 W 1 21.08 1957.06
DCK08A 1956 M 1 23.08 1957.00
DCK08A 1956 D 4 26.02 1956.93
DCK08A 1956 D 3 25.37 1956.87
DCK08A 1956 D 2 25.46 1956.80
DCK08A 1956 D 1 25.85 1956.73
DCK08A 1956 W 10 24.75 1956.67
DCK08A 1956 W 9 25.15 1956.60
DCK08A 1956 W 8 23.49 1956.53
DCK08A 1956 W 7 22.31 1956.47
DCK08A 1956 W 6 20.57 1956.40
DCK08A 1956 W 5 20.27 1956.33
DCK08A 1956 W 4 19.65 1956.27
DCK08A 1956 W 3 20.60 1956.20
DCK08A 1956 W 2 21.05 1956.13
DCK08A 1956 W 1 22.61 1956.07
DCK08A 1955 M 1 24.12 1956.00
DCK08A 1955 D 5 26.83 1955.93
DCK08A 1955 D 4 28.82 1955.87
DCK08A 1955 D 3 28.12 1955.80
DCK08A 1955 D 2 27.85 1955.73
DCK08A 1955 D 1 26.46 1955.67
DCK08A 1955 W 9 25.48 1955.60
DCK08A 1955 W 8 22.97 1955.53
DCK08A 1955 W 7 22.45 1955.47
DCK08A 1955 W 6 21.83 1955.40
DCK08A 1955 W 5 20.42 1955.33
DCK08A 1955 W 4 18.75 1955.27
DCK08A 1955 W 3 20.11 1955.20
DCK08A 1955 W 2 22.95 1955.13
DCK08A 1955 W 1 23.06 1955.07
DCK08A 1954 M 1 24.45 1955.00
DCK08A 1954 D 2 26.26 1954.93
DCK08A 1954 D 1 25.29 1954.86
DCK08A 1954 W 11 24.54 1954.79
165

DCK08A 1954 W 10 23.29 1954.71
DCK08A 1954 W 9 21.71 1954.64
DCK08A 1954 W 8 20.09 1954.57
DCK08A 1954 W 7 21.69 1954.50
DCK08A 1954 W 6 21.56 1954.43
DCK08A 1954 W 5 22.54 1954.36
DCK08A 1954 W 4 23.83 1954.29
DCK08A 1954 W 3 23.85 1954.21
DCK08A 1954 W 2 22.95 1954.14
DCK08A 1954 W 1 24.54 1954.07
DCK08A 1953 M 1 26.50 1954.00
DCK08A 1953 D 5 26.33 1953.94
DCK08A 1953 D 4 23.84 1953.88
DCK08A 1953 D 3 22.45 1953.82
DCK08A 1953 D 2 22.58 1953.76
DCK08A 1953 D 1 24.51 1953.71
DCK08A 1953 W 11 22.84 1953.65
DCK08A 1953 W 10 21.49 1953.59
DCK08A 1953 W 9 21.54 1953.53
DCK08A 1953 W 8 21.13 1953.47
DCK08A 1953 W 7 20.87 1953.41
DCK08A 1953 W 6 20.63 1953.35
DCK08A 1953 W 5 20.24 1953.29
DCK08A 1953 W 4 21.93 1953.24
DCK08A 1953 W 3 22.72 1953.18
DCK08A 1953 W 2 23.60 1953.12
DCK08A 1953 W 1 24.50 1953.06
DCK08A 1950 D 2 28.49 1953.00
DCK08A 1950 D 1 N/A 1952.00
DCK08A 1950 W 5 21.64 1950.86
DCK08A 1950 W 4 22.01 1950.71
DCK08A 1950 W 3 22.66 1950.57
DCK08A 1950 W 2 22.30 1950.43
DCK08A 1950 W 1 21.83 1950.29
DCK08A 1949 M 1 23.76 1950.14
DCK08A 1949 D 3 22.15 1950.00
DCK08A 1949 D 2 21.59 1949.89
DCK08A 1949 D 1 22.09 1949.78
DCK08A 1949 W 5 21.26 1949.67
DCK08A 1949 W 4 20.71 1949.56
DCK08A 1949 W 3 22.09 1949.44
DCK08A 1949 W 2 22.60 1949.33
DCK08A 1949 W 1 23.01 1949.22
DCK08A 1948 M 1 24.56 1949.11
DCK08A 1948 D 2 25.42 1949.00
DCK08A 1948 D 1 24.96 1948.90
DCK08A 1948 W 7 23.59 1948.80
DCK08A 1948 W 6 21.99 1948.70
166

DCK08A 1948 W 5 22.15 1948.60
DCK08A 1948 W 4 22.38 1948.50
DCK08A 1948 W 3 23.50 1948.40
DCK08A 1948 W 2 23.05 1948.30
DCK08A 1948 W 1 22.96 1948.20
DCK08A 1947 M 1 25.85 1948.10
DCK08A 1947 D 3 26.90 1948.00
DCK08A 1947 D 2 26.00 1947.92
DCK08A 1947 D 1 25.15 1947.85
DCK08A 1947 W 9 22.47 1947.77
DCK08A 1947 W 8 20.99 1947.69
DCK08A 1947 W 7 20.85 1947.62
DCK08A 1947 W 6 21.16 1947.54
DCK08A 1947 W 5 23.68 1947.46
DCK08A 1947 W 4 23.60 1947.38
DCK08A 1947 W 3 23.46 1947.31
DCK08A 1947 W 2 23.41 1947.23
DCK08A 1947 W 1 24.96 1947.15
DCK08A 1946 M 1 25.25 1947.08
DCK08A 1946 D 4 24.37 1947.00
DCK08A 1946 D 3 23.52 1946.92
DCK08A 1946 D 2 23.32 1946.85
DCK08A 1946 D 1 23.05 1946.77
DCK08A 1946 W 8 23.31 1946.69
DCK08A 1946 W 7 22.89 1946.62
DCK08A 1946 W 6 22.67 1946.54
DCK08A 1946 W 5 22.41 1946.46
DCK08A 1946 W 4 23.30 1946.38
DCK08A 1946 W 3 24.70 1946.31
DCK08A 1946 W 2 24.84 1946.23
DCK08A 1946 W 1 24.79 1946.15
DCK08A 1945 D 5 25.04 1946.08
DCK08A 1945 D 4 25.02 1946.00
DCK08A 1945 D 3 24.72 1945.93
DCK08A 1945 D 2 24.47 1945.87
DCK08A 1945 D 1 23.66 1945.80
DCK08A 1945 W 10 22.63 1945.73
DCK08A 1945 W 9 21.84 1945.67
DCK08A 1945 W 8 21.11 1945.60
DCK08A 1945 W 7 20.93 1945.53
DCK08A 1945 W 6 21.79 1945.47
DCK08A 1945 W 5 21.68 1945.40
DCK08A 1945 W 4 22.74 1945.33
DCK08A 1945 W 3 23.75 1945.27
DCK08A 1945 W 2 25.14 1945.20
DCK08A 1945 W 1 26.46 1945.13
DCK08A 1944 D 2 26.55 1945.07
DCK08A 1944 D 1 25.96 1945.00
167

DCK08A 1944 W 7 24.60 1944.89
DCK08A 1944 W 6 23.41 1944.78
DCK08A 1944 W 5 22.97 1944.67
DCK08A 1944 W 4 21.99 1944.56
DCK08A 1944 W 3 22.07 1944.44
DCK08A 1944 W 2 22.63 1944.33
DCK08A 1944 W 1 24.27 1944.22
DCK08A 1943 D 2 23.71 1944.11
DCK08A 1943 D 1 23.91 1944.00
DCK08A 1943 W 6 23.42 1943.88
DCK08A 1943 W 5 22.10 1943.75
DCK08A 1943 W 4 21.80 1943.63
DCK08A 1943 W 3 21.26 1943.50
DCK08A 1943 W 2 22.31 1943.38
DCK08A 1943 W 1 23.29 1943.25
DCK08A 1942 M 1 24.08 1943.13
DCK08A 1942 D 3 24.78 1943.00
DCK08A 1942 D 2 24.17 1942.88
DCK08A 1942 D 1 24.05 1942.75
DCK08A 1942 W 4 22.79 1942.63
DCK08A 1942 W 3 22.44 1942.50
DCK08A 1942 W 2 21.16 1942.38
DCK08A 1942 W 1 21.83 1942.25
DCK08A 1941 M 1 22.64 1942.13
DCK08A 1941 D 3 24.68 1942.00
DCK08A 1941 D 2 25.08 1941.88
DCK08A 1941 D 1 23.86 1941.75
DCK08A 1941 W 4 23.13 1941.63
DCK08A 1941 W 3 22.20 1941.50
DCK08A 1941 W 2 21.88 1941.38
DCK08A 1941 W 1 23.16 1941.25
DCK08A 1940 D 2 24.94 1941.13
DCK08A 1940 D 1 26.16 1941.00
DCK08A 1940 W 5 25.41 1940.86
DCK08A 1940 W 4 23.65 1940.71
DCK08A 1940 W 3 22.58 1940.57
DCK08A 1940 W 2 20.91 1940.43
DCK08A 1940 W 1 19.93 1940.29
DCK08A 1938 M 1 25.79 1940.14
DCK08A 1938 D 3 25.91 1940.00
DCK08A 1938 D 2 N/A 1939.00
DCK08A 1938 D 1 27.04 1938.90
DCK08A 1938 W 6 26.24 1938.80
DCK08A 1938 W 5 25.18 1938.70
DCK08A 1938 W 4 23.75 1938.60
DCK08A 1938 W 3 22.56 1938.50
DCK08A 1938 W 2 22.23 1938.40
DCK08A 1938 W 1 22.43 1938.30
168

DCK08A 1937 M 1 22.78 1938.20
DCK08A 1937 D 3 23.31 1938.10
DCK08A 1937 D 2 25.23 1938.00
DCK08A 1937 D 1 27.21 1937.94
DCK08A 1937 W 12 26.33 1937.88
DCK08A 1937 W 11 26.09 1937.81
DCK08A 1937 W 10 24.84 1937.75
DCK08A 1937 W 9 24.38 1937.69
DCK08A 1937 W 8 23.12 1937.63
DCK08A 1937 W 7 22.29 1937.56
DCK08A 1937 W 6 21.42 1937.50
DCK08A 1937 W 5 21.63 1937.44
DCK08A 1937 W 4 21.52 1937.38
DCK08A 1937 W 3 24.19 1937.31
DCK08A 1937 W 2 23.38 1937.25
DCK08A 1937 W 1 24.05 1937.19
DCK08A 1936 M 1 24.79 1937.13
DCK08A 1936 D 3 24.45 1937.06
DCK08A 1936 D 2 25.76 1937.00
DCK08A 1936 D 1 28.82 1936.89
DCK08A 1936 W 5 28.46 1936.78
DCK08A 1936 W 4 27.15 1936.67
DCK08A 1936 W 3 25.15 1936.56
DCK08A 1936 W 2 24.05 1936.44
DCK08A 1936 W 1 23.48 1936.33
DCK08A 1935 M 1 23.94 1936.22
DCK08A 1935 D 3 23.87 1936.11
DCK08A 1935 D 2 25.01 1936.00
DCK08A 1935 D 1 25.15 1935.92
DCK08A 1935 W 9 23.65 1935.85
DCK08A 1935 W 8 22.16 1935.77
DCK08A 1935 W 7 21.18 1935.69
DCK08A 1935 W 6 19.61 1935.62
DCK08A 1935 W 5 19.43 1935.54
DCK08A 1935 W 4 19.90 1935.46
DCK08A 1935 W 3 21.99 1935.38
DCK08A 1935 W 2 23.49 1935.31
DCK08A 1935 W 1 22.81 1935.23
DCK08A 1934 M 1 22.99 1935.15
DCK08A 1934 D 3 23.40 1935.08
DCK08A 1934 D 2 24.74 1935.00
DCK08A 1934 D 1 25.85 1934.92
DCK08A 1934 W 8 24.24 1934.83
DCK08A 1934 W 7 22.34 1934.75
DCK08A 1934 W 6 20.31 1934.67
DCK08A 1934 W 5 18.64 1934.58
DCK08A 1934 W 4 20.02 1934.50
DCK08A 1934 W 3 21.03 1934.42
169

DCK08A 1934 W 2 20.28 1934.33
DCK08A 1934 W 1 20.47 1934.25
DCK08A 1933 M 1 21.22 1934.17
DCK08A 1933 D 3 22.98 1934.08
DCK08A 1933 D 2 23.26 1934.00
DCK08A 1933 D 1 25.44 1933.91
DCK08A 1933 W 7 24.11 1933.82
DCK08A 1933 W 6 22.28 1933.73
DCK08A 1933 W 5 21.30 1933.64
DCK08A 1933 W 4 21.01 1933.55
DCK08A 1933 W 3 20.86 1933.45
DCK08A 1933 W 2 20.42 1933.36
DCK08A 1933 W 1 20.16 1933.27
DCK08A 1932 M 1 19.52 1933.18
DCK08A 1932 D 3 20.01 1933.09
DCK08A 1932 D 2 20.61 1933.00
DCK08A 1932 D 1 23.77 1932.88
DCK08A 1932 W 4 24.00 1932.75
DCK08A 1932 W 3 20.67 1932.63
DCK08A 1932 W 2 19.06 1932.50
DCK08A 1932 W 1 18.70 1932.38
DCK08A 1931 M 1 21.18 1932.25
DCK08A 1931 D 3 22.88 1932.13
DCK08A 1931 D 2 23.59 1932.00
DCK08A 1931 D 1 26.26 1931.91
DCK08A 1931 W 7 26.83 1931.82
DCK08A 1931 W 6 25.92 1931.73
DCK08A 1931 W 5 24.79 1931.64
DCK08A 1931 W 4 23.24 1931.55
DCK08A 1931 W 3 21.16 1931.45
DCK08A 1931 W 2 20.57 1931.36
DCK08A 1931 W 1 20.74 1931.27
DCK08A 1930 M 1 21.81 1931.18
DCK08A 1930 D 3 21.70 1931.09
DCK08A 1930 D 2 24.85 1931.00
DCK08A 1930 D 1 26.30 1930.86
DCK08A 1930 W 3 24.95 1930.71
DCK08A 1930 W 2 24.27 1930.57
DCK08A 1930 W 1 21.18 1930.43
DCK08A 1929 M 1 21.09 1930.29
DCK08A 1929 D 3 22.93 1930.14
DCK08A 1929 D 2 23.09 1930.00
DCK08A 1929 D 1 24.33 1929.91
DCK08A 1929 W 7 23.28 1929.82
DCK08A 1929 W 6 23.06 1929.73
DCK08A 1929 W 5 22.79 1929.64
DCK08A 1929 W 4 22.50 1929.55
DCK08A 1929 W 3 21.26 1929.45
170

DCK08A 1929 W 2 19.55 1929.36
DCK08A 1929 W 1 19.10 1929.27
DCK08A 1928 M 1 19.59 1929.18
DCK08A 1928 D 6 22.02 1929.09
DCK08A 1928 D 5 23.66 1929.00
DCK08A 1928 D 4 25.63 1928.93
DCK08A 1928 D 3 25.24 1928.87
DCK08A 1928 D 2 26.15 1928.80
DCK08A 1928 D 1 25.73 1928.73
DCK08A 1928 W 8 25.21 1928.67
DCK08A 1928 W 7 24.67 1928.60
DCK08A 1928 W 6 24.54 1928.53
DCK08A 1928 W 5 23.88 1928.47
DCK08A 1928 W 4 21.63 1928.40
DCK08A 1928 W 3 21.24 1928.33
DCK08A 1928 W 2 21.46 1928.27
DCK08A 1928 W 1 22.22 1928.20
DCK08A 1927 D 2 21.36 1928.13
DCK08A 1927 D 1 23.99 1928.07
DCK08A 1927 W 10 26.61 1928.00
DCK08A 1927 W 9 25.01 1927.92
DCK08A 1927 W 8 24.98 1927.83
DCK08A 1927 W 7 20.52 1927.75
DCK08A 1927 W 6 21.77 1927.67
DCK08A 1927 W 5 23.67 1927.58
DCK08A 1927 W 4 24.45 1927.50
DCK08A 1927 W 3 23.67 1927.42
DCK08A 1927 W 2 23.96 1927.33
DCK08A 1927 W 1 22.85 1927.25
DCK08A 1926 M 1 23.49 1927.17
DCK08A 1926 D 3 23.67 1927.08
DCK08A 1926 D 2 25.29 1927.00
DCK08A 1926 D 1 23.67 1926.93
DCK08A 1926 W 11 26.94 1926.87
DCK08A 1926 W 10 26.09 1926.80
DCK08A 1926 W 9 24.32 1926.73
DCK08A 1926 W 8 23.67 1926.67
DCK08A 1926 W 7 15.31 1926.60
DCK08A 1926 W 6 15.55 1926.53
DCK08A 1926 W 5 16.72 1926.47
DCK08A 1926 W 4 17.73 1926.40
DCK08A 1926 W 3 19.11 1926.33
DCK08A 1926 W 2 19.29 1926.27
DCK08A 1926 W 1 18.95 1926.20
DCK08A 1925 M 1 19.25 1926.13
DCK08A 1925 D 2 20.76 1926.07
DCK08A 1925 D 1 23.92 1926.00
DCK08A 1925 W 14 28.37 1925.94
171

DCK08A 1925 W 13 26.59 1925.88
DCK08A 1925 W 12 24.98 1925.82
DCK08A 1925 W 11 23.68 1925.76
DCK08A 1925 W 10 21.88 1925.71
DCK08A 1925 W 9 18.98 1925.65
DCK08A 1925 W 8 17.49 1925.59
DCK08A 1925 W 7 17.93 1925.53
DCK08A 1925 W 6 17.00 1925.47
DCK08A 1925 W 5 18.30 1925.41
DCK08A 1925 W 4 19.49 1925.35
DCK08A 1925 W 3 20.50 1925.29
DCK08A 1925 W 2 21.48 1925.24
DCK08A 1925 W 1 22.82 1925.18
DCK08A 1924 M 1 23.66 1925.12
DCK08A 1924 D 2 27.59 1925.06
DCK08A 1924 D 1 28.58 1925.00
DCK08A 1924 W 14 28.33 1924.94
DCK08A 1924 W 13 25.16 1924.88
DCK08A 1924 W 12 22.62 1924.82
DCK08A 1924 W 11 20.54 1924.76
DCK08A 1924 W 10 18.69 1924.71
DCK08A 1924 W 9 18.37 1924.65
DCK08A 1924 W 8 18.13 1924.59
DCK08A 1924 W 7 17.46 1924.53
DCK08A 1924 W 6 17.73 1924.47
DCK08A 1924 W 5 19.52 1924.41
DCK08A 1924 W 4 20.66 1924.35
DCK08A 1924 W 3 20.60 1924.29
DCK08A 1924 W 2 21.72 1924.24
DCK08A 1924 W 1 22.12 1924.18
DCK08A 1923 M 1 26.62 1924.12
DCK08A 1923 D 3 30.10 1924.06
DCK08A 1923 D 2 29.57 1924.00
DCK08A 1923 D 1 28.27 1923.95
DCK08A 1923 W 15 25.21 1923.89
DCK08A 1923 W 14 24.15 1923.84
DCK08A 1923 W 13 22.26 1923.79
DCK08A 1923 W 12 20.03 1923.74
DCK08A 1923 W 11 19.06 1923.68
DCK08A 1923 W 10 19.24 1923.63
DCK08A 1923 W 9 19.62 1923.58
DCK08A 1923 W 8 19.19 1923.53
DCK08A 1923 W 7 21.04 1923.47
DCK08A 1923 W 6 22.88 1923.42
DCK08A 1923 W 5 23.75 1923.37
DCK08A 1923 W 4 25.20 1923.32
DCK08A 1923 W 3 27.07 1923.26
DCK08A 1923 W 2 26.79 1923.21
172

DCK08A 1923 W 1 26.54 1923.16
DCK08A 1922 M 1 27.74 1923.11
DCK08A 1922 D 7 27.11 1923.05
DCK08A 1922 D 6 26.88 1923.00
DCK08A 1922 D 5 23.46 1922.92
DCK08A 1922 D 4 21.78 1922.85
DCK08A 1922 D 3 21.70 1922.77
DCK08A 1922 D 2 20.69 1922.69
DCK08A 1922 D 1 20.77 1922.62
DCK08A 1922 W 5 20.87 1922.54
DCK08A 1922 W 4 19.29 1922.46
DCK08A 1922 W 3 19.86 1922.38
DCK08A 1922 W 2 18.32 1922.31
DCK08A 1922 W 1 19.57 1922.23
DCK08B 1992 D 1 22.45 1992.67
DCK08B 1992 W 2 21.09 1992.33
DCK08B 1992 W 1 21.17 1992.00
DCK08B 1991 D N/A 23.14 1991.75
DCK08B 1991 W 3 22.60 1991.50
DCK08B 1991 W 2 22.96 1991.25
DCK08B 1991 W 1 24.75 1991.00
DCK08B 1990 D 1 23.85 1990.80
DCK08B 1990 W 4 22.04 1990.60
DCK08B 1990 W 3 21.75 1990.40
DCK08B 1990 W 2 22.63 1990.20
DCK08B 1990 W 1 22.81 1990.00
DCK08B 1989 D 2 22.33 1989.80
DCK08B 1989 D 1 20.76 1989.60
DCK08B 1989 W 3 21.17 1989.40
DCK08B 1989 W 2 22.33 1989.20
DCK08B 1989 W 1 22.72 1989.00
DCK08B 1953 D 4 N/A 1988.00
DCK08B 1953 D 3 25.14 1953.91
DCK08B 1953 D 2 24.91 1953.82
DCK08B 1953 D 1 23.09 1953.73
DCK08B 1953 W 7 21.62 1953.64
DCK08B 1953 W 6 20.96 1953.55
DCK08B 1953 W 5 20.99 1953.45
DCK08B 1953 W 4 20.31 1953.36
DCK08B 1953 W 3 21.43 1953.27
DCK08B 1953 W 2 22.51 1953.18
DCK08B 1953 W 1 23.24 1953.09
DCK08B 1952 D N/A 25.55 1953.00
DCK08B 1952 W 3 23.90 1952.75
DCK08B 1952 W 2 21.85 1952.50
DCK08B 1952 W 1 21.20 1952.25
DCK08B 1951 D 3 22.26 1952.00
173

DCK08B 1951 D 2 23.17 1951.86
DCK08B 1951 D 1 21.87 1951.71
DCK08B 1951 W 4 21.07 1951.57
DCK08B 1951 W 3 21.27 1951.43
DCK08B 1951 W 2 21.79 1951.29
DCK08B 1951 W 1 23.09 1951.14
DCK08B 1950 D 2 25.16 1951.00
DCK08B 1950 D 1 22.65 1950.83
DCK08B 1950 W 4 20.12 1950.67
DCK08B 1950 W 3 20.66 1950.50
DCK08B 1950 W 2 22.84 1950.33
DCK08B 1950 W 1 23.20 1950.17
DCK08B 1940 M N/A 23.19 1950.00
DCK08B 1940 D 2 N/A 1949.00
DCK08B 1940 D 1 26.35 1940.89
DCK08B 1940 W 6 25.58 1940.78
DCK08B 1940 W 5 22.95 1940.67
DCK08B 1940 W 4 23.45 1940.56
DCK08B 1940 W 3 22.90 1940.44
DCK08B 1940 W 2 21.93 1940.33
DCK08B 1940 W 1 21.36 1940.22
DCK08B 1939 D 3 22.84 1940.11
DCK08B 1939 D 2 25.86 1940.00
DCK08B 1939 D 1 25.77 1939.89
DCK08B 1939 W 6 23.71 1939.78
DCK08B 1939 W 5 22.83 1939.67
DCK08B 1939 W 4 22.47 1939.56
DCK08B 1939 W 3 21.42 1939.44
DCK08B 1939 W 2 21.43 1939.33
DCK08B 1939 W 1 24.22 1939.22
DCK08B 1938 M N/A 24.29 1939.11
DCK08B 1938 D 4 24.82 1939.00
DCK08B 1938 D 3 23.70 1938.86
DCK08B 1938 D 2 20.95 1938.71
DCK08B 1938 D 1 20.46 1938.57
DCK08B 1938 W 2 21.00 1938.43
DCK08B 1938 W 1 22.30 1938.29
DCK08C 1954 D 5 25.89 1954.97
DCK08C 1954 D 4 25.84 1954.95
DCK08C 1954 D 3 25.71 1954.92
DCK08C 1954 D 2 25.70 1954.89
DCK08C 1954 D 1 25.41 1954.87
DCK08C 1954 W 33 25.29 1954.84
DCK08C 1954 W 32 24.25 1954.82
DCK08C 1954 W 31 23.63 1954.79
DCK08C 1954 W 30 22.48 1954.76
DCK08C 1954 W 29 21.26 1954.74
174

DCK08C 1954 W 28 20.04 1954.71
DCK08C 1954 W 27 20.05 1954.68
DCK08C 1954 W 26 20.77 1954.66
DCK08C 1954 W 25 21.56 1954.63
DCK08C 1954 W 24 21.97 1954.61
DCK08C 1954 W 23 21.81 1954.58
DCK08C 1954 W 22 21.76 1954.55
DCK08C 1954 W 21 22.03 1954.53
DCK08C 1954 W 20 22.42 1954.50
DCK08C 1954 W 19 23.30 1954.47
DCK08C 1954 W 18 23.26 1954.45
DCK08C 1954 W 17 22.75 1954.42
DCK08C 1954 W 16 21.59 1954.39
DCK08C 1954 W 15 21.61 1954.37
DCK08C 1954 W 14 21.75 1954.34
DCK08C 1954 W 13 22.42 1954.32
DCK08C 1954 W 12 22.83 1954.29
DCK08C 1954 W 11 22.76 1954.26
DCK08C 1954 W 10 23.36 1954.24
DCK08C 1954 W 9 24.52 1954.21
DCK08C 1954 W 8 25.03 1954.18
DCK08C 1954 W 7 24.74 1954.16
DCK08C 1954 W 6 23.98 1954.13
DCK08C 1954 W 5 23.10 1954.11
DCK08C 1954 W 4 23.40 1954.08
DCK08C 1954 W 3 23.48 1954.05
DCK08C 1954 W 2 24.73 1954.03
DCK08C 1954 W 1 27.53 1954.00
DCK08C 1953 D 10 28.89 1953.97
DCK08C 1953 D 9 26.22 1953.93
DCK08C 1953 D 8 24.47 1953.90
DCK08C 1953 D 7 23.46 1953.87
DCK08C 1953 D 6 23.13 1953.83
DCK08C 1953 D 5 23.07 1953.80
DCK08C 1953 D 4 22.76 1953.77
DCK08C 1953 D 3 22.37 1953.73
DCK08C 1953 D 2 21.66 1953.70
DCK08C 1953 D 1 21.34 1953.67
DCK08C 1953 W 20 20.87 1953.63
DCK08C 1953 W 19 21.01 1953.60
DCK08C 1953 W 18 21.88 1953.57
DCK08C 1953 W 17 21.77 1953.53
DCK08C 1953 W 16 21.74 1953.50
DCK08C 1953 W 15 21.56 1953.47
DCK08C 1953 W 14 21.02 1953.43
DCK08C 1953 W 13 20.96 1953.40
DCK08C 1953 W 12 20.71 1953.37
DCK08C 1953 W 11 21.37 1953.33
175

DCK08C 1953 W 10 22.22 1953.30
DCK08C 1953 W 9 23.06 1953.27
DCK08C 1953 W 8 23.21 1953.23
DCK08C 1953 W 7 22.99 1953.20
DCK08C 1953 W 6 22.67 1953.17
DCK08C 1953 W 5 23.23 1953.13
DCK08C 1953 W 4 24.67 1953.10
DCK08C 1953 W 3 26.65 1953.07
DCK08C 1953 W 2 28.03 1953.03
DCK08C 1953 W 1 26.90 1953.00
DCK08C 1952 D 8 26.25 1952.92
DCK08C 1952 D 7 25.08 1952.85
DCK08C 1952 D 6 23.83 1952.77
DCK08C 1952 D 5 22.26 1952.69
DCK08C 1952 D 4 21.65 1952.62
DCK08C 1952 D 3 21.35 1952.54
DCK08C 1952 D 2 21.75 1952.46
DCK08C 1952 D 1 21.96 1952.38
DCK08C 1952 W 5 22.45 1952.31
DCK08C 1952 W 4 23.10 1952.23
DCK08C 1952 W 3 24.38 1952.15
DCK08C 1952 W 2 25.30 1952.08
DCK08C 1952 W 1 24.96 1952.00
DCK08C 1951 D 5 23.68 1951.93
DCK08C 1951 D 4 22.66 1951.87
DCK08C 1951 D 3 21.45 1951.80
DCK08C 1951 D 2 21.63 1951.73
DCK08C 1951 D 1 21.89 1951.67
DCK08C 1951 W 10 22.28 1951.60
DCK08C 1951 W 9 23.04 1951.53
DCK08C 1951 W 8 23.02 1951.47
DCK08C 1951 W 7 23.00 1951.40
DCK08C 1951 W 6 23.36 1951.33
DCK08C 1951 W 5 24.37 1951.27
DCK08C 1951 W 4 25.42 1951.20
DCK08C 1951 W 3 25.43 1951.13
DCK08C 1951 W 2 24.77 1951.07
DCK08C 1951 W 1 25.68 1951.00
DCK08C 1950 D 8 23.65 1950.94
DCK08C 1950 D 7 21.42 1950.88
DCK08C 1950 D 6 20.22 1950.82
DCK08C 1950 D 5 19.44 1950.76
DCK08C 1950 D 4 19.86 1950.71
DCK08C 1950 D 3 20.93 1950.65
DCK08C 1950 D 2 21.31 1950.59
DCK08C 1950 D 1 21.17 1950.53
DCK08C 1950 W 9 21.72 1950.47
DCK08C 1950 W 8 23.24 1950.41
176

DCK08C 1950 W 7 25.30 1950.35
DCK08C 1950 W 6 24.77 1950.29
DCK08C 1950 W 5 23.95 1950.24
DCK08C 1950 W 4 24.04 1950.18
DCK08C 1950 W 3 23.99 1950.12
DCK08C 1950 W 2 23.86 1950.06
DCK08C 1950 W 1 25.14 1950.00
DCK12A 2000 D N/A 23.13 2000.75
DCK12A 2000 W 3 23.15 2000.50
DCK12A 2000 W 2 23.67 2000.25
DCK12A 2000 W 1 23.56 2000.00
DCK12A 1999 D N/A 23.61 1999.50
DCK12A 1999 W N/A 25.02 1999.00
DCK12A 1998 D N/A 23.99 1998.50
DCK12A 1998 W 1 22.32 1998.00
DCK12A 1997 D N/A 23.60 1997.50
DCK12A 1997 W N/A 23.34 1997.00
DCK12A 1996 D N/A 21.71 1996.67
DCK12A 1996 W 2 22.26 1996.33
DCK12A 1996 W 1 23.95 1996.00
DCK12A 1995 D N/A 21.64 1995.50
DCK12A 1995 W 1 21.17 1995.00
DCK12A 1994 D N/A 21.85 1994.67
DCK12A 1994 W 2 21.61 1994.33
DCK12A 1994 W 1 23.03 1994.00
DCK12A 1993 D N/A 22.95 1993.67
DCK12A 1993 W 3 24.24 1993.33
DCK12A 1993 W 2 24.46 1993.00
DCK12A 1992 D N/A 20.86 1992.50
DCK12A 1992 W N/A 22.31 1992.00
DCK12A 1991 D N/A 22.95 1991.50
DCK12A 1991 W 1 23.68 1991.00
DCK12A 1990 D N/A 22.71 1990.67
DCK12A 1990 W 2 23.25 1990.33
DCK12A 1990 W 1 24.38 1990.00
DCK12A 1989 D N/A 21.81 1989.67
DCK12A 1989 W 2 22.80 1989.33
DCK12A 1989 W 1 23.16 1989.00
DCK12A 1988 D N/A 21.75 1988.75
DCK12A 1988 W 3 20.93 1988.50
DCK12A 1988 W 2 21.36 1988.25
DCK12A 1988 W 1 23.62 1988.00
DCK12A 1987 D 1 24.26 1987.88
DCK12A 1987 W 7 21.05 1987.75
DCK12A 1987 W 6 20.70 1987.63
DCK12A 1987 W 5 21.99 1987.50
DCK12A 1987 W 4 23.30 1987.38
177

DCK12A 1987 W 3 25.51 1987.25
DCK12A 1987 W 2 26.10 1987.13
DCK12A 1987 W 1 25.74 1987.00
DCK12A 1986 D N/A 24.51 1986.67
DCK12A 1986 W 2 23.92 1986.33
DCK12A 1986 W 1 25.21 1986.00
DCK12A 1985 D N/A 23.51 1985.50
DCK12A 1985 W N/A 23.67 1985.00
DCK12A 1984 D N/A 23.13 1984.80
DCK12A 1984 W 4 23.02 1984.60
DCK12A 1984 W 3 23.16 1984.40
DCK12A 1984 W 2 23.83 1984.20
DCK12A 1984 W 1 23.78 1984.00
DCK12A 1983 D 2 21.53 1983.75
DCK12A 1983 D 1 20.54 1983.50
DCK12A 1983 W 2 21.59 1983.25
DCK12A 1983 W 1 23.52 1983.00
DCK12A 1982 D N/A 22.44 1982.83
DCK12A 1982 W 5 23.68 1982.67
DCK12A 1982 W 4 24.19 1982.50
DCK12A 1982 W 3 23.75 1982.33
DCK12A 1982 W 2 23.95 1982.17
DCK12A 1982 W 1 22.82 1982.00
DCK12A 1981 D 2 22.52 1981.75
DCK12A 1981 D 1 22.19 1981.50
DCK12A 1981 W 2 23.21 1981.25
DCK12A 1981 W 1 23.21 1981.00
DCK12A 1980 D N/A 22.13 1980.67
DCK12A 1980 W 2 22.05 1980.33
DCK12A 1980 W 1 23.66 1980.00
DCK12A 1979 D 2 25.71 1979.80
DCK12A 1979 D 1 24.36 1979.60
DCK12A 1979 W 3 23.90 1979.40
DCK12A 1979 W 2 23.46 1979.20
DCK12A 1979 W 1 24.47 1979.00
DCK12A 1978 D 3 23.60 1978.88
DCK12A 1978 D 2 22.23 1978.75
DCK12A 1978 D 1 21.42 1978.63
DCK12A 1978 W 5 21.43 1978.50
DCK12A 1978 W 4 21.34 1978.38
DCK12A 1978 W 3 20.88 1978.25
DCK12A 1978 W 2 20.99 1978.13
DCK12A 1978 W 1 23.75 1978.00
DCK12A 1977 D N/A 22.59 1977.83
DCK12A 1977 W 5 22.21 1977.67
DCK12A 1977 W 4 23.03 1977.50
DCK12A 1977 W 3 24.22 1977.33
DCK12A 1977 W 2 25.82 1977.17
178

DCK12A 1977 W 1 25.64 1977.00
DCK12A 1976 D 2 22.72 1976.88
DCK12A 1976 D 1 21.07 1976.75
DCK12A 1976 W 6 20.97 1976.63
DCK12A 1976 W 5 22.97 1976.50
DCK12A 1976 W 4 24.62 1976.38
DCK12A 1976 W 3 25.47 1976.25
DCK12A 1976 W 2 26.33 1976.13
DCK12A 1976 W 1 23.60 1976.00
DCK12A 1975 D 2 20.35 1975.88
DCK12A 1975 D 1 20.44 1975.75
DCK12A 1975 W 6 21.40 1975.63
DCK12A 1975 W 5 22.12 1975.50
DCK12A 1975 W 4 22.58 1975.38
DCK12A 1975 W 3 24.63 1975.25
DCK12A 1975 W 2 23.99 1975.13
DCK12A 1975 W 1 22.91 1975.00
DCK12A 1974 D N/A 22.37 1974.90
DCK12A 1974 W 9 22.59 1974.80
DCK12A 1974 W 8 23.08 1974.70
DCK12A 1974 W 7 22.73 1974.60
DCK12A 1974 W 6 22.78 1974.50
DCK12A 1974 W 5 24.01 1974.40
DCK12A 1974 W 4 24.68 1974.30
DCK12A 1974 W 3 24.89 1974.20
DCK12A 1974 W 2 25.03 1974.10
DCK12A 1974 W 1 23.34 1974.00
DCK12A 1973 D 2 20.22 1973.92
DCK12A 1973 D 1 19.14 1973.83
DCK12A 1973 W 10 19.56 1973.75
DCK12A 1973 W 9 19.95 1973.67
DCK12A 1973 W 8 20.90 1973.58
DCK12A 1973 W 7 22.59 1973.50
DCK12A 1973 W 6 23.02 1973.42
DCK12A 1973 W 5 23.47 1973.33
DCK12A 1973 W 4 23.81 1973.25
DCK12A 1973 W 3 23.82 1973.17
DCK12A 1973 W 2 24.16 1973.08
DCK12A 1973 W 1 24.24 1973.00
DCK12A 1972 D 2 25.87 1972.92
DCK12A 1972 D 1 23.93 1972.85
DCK12A 1972 W 11 22.99 1972.77
DCK12A 1972 W 10 22.47 1972.69
DCK12A 1972 W 9 23.11 1972.62
DCK12A 1972 W 8 23.65 1972.54
DCK12A 1972 W 7 23.96 1972.46
DCK12A 1972 W 6 24.43 1972.38
DCK12A 1972 W 5 25.07 1972.31
179

DCK12A 1972 W 4 25.54 1972.23
DCK12A 1972 W 3 25.17 1972.15
DCK12A 1972 W 2 24.69 1972.08
DCK12A 1972 W 1 25.57 1972.00
DCK12A 1971 D 2 25.95 1971.93
DCK12A 1971 D 1 24.35 1971.87
DCK12A 1971 W 13 23.08 1971.80
DCK12A 1971 W 12 22.62 1971.73
DCK12A 1971 W 11 22.14 1971.67
DCK12A 1971 W 10 21.77 1971.60
DCK12A 1971 W 9 21.69 1971.53
DCK12A 1971 W 8 22.54 1971.47
DCK12A 1971 W 7 23.45 1971.40
DCK12A 1971 W 6 23.49 1971.33
DCK12A 1971 W 5 23.37 1971.27
DCK12A 1971 W 4 23.62 1971.20
DCK12A 1971 W 3 24.08 1971.13
DCK12A 1971 W 2 24.71 1971.07
DCK12A 1971 W 1 25.19 1971.00
DCK12A 1970 D 2 23.77 1970.90
DCK12A 1970 D 1 21.71 1970.80
DCK12A 1970 W 8 21.15 1970.70
DCK12A 1970 W 7 21.33 1970.60
DCK12A 1970 W 6 20.75 1970.50
DCK12A 1970 W 5 20.91 1970.40
DCK12A 1970 W 4 22.83 1970.30
DCK12A 1970 W 3 23.94 1970.20
DCK12A 1970 W 2 24.20 1970.10
DCK12A 1970 W 1 24.07 1970.00
DCK12A 1969 D 2 25.46 1969.89
DCK12A 1969 D 1 24.67 1969.78
DCK12A 1969 W 7 22.93 1969.67
DCK12A 1969 W 6 21.81 1969.56
DCK12A 1969 W 5 21.29 1969.44
DCK12A 1969 W 4 21.84 1969.33
DCK12A 1969 W 3 22.64 1969.22
DCK12A 1969 W 2 23.56 1969.11
DCK12A 1969 W 1 24.32 1969.00
DCK12A 1968 D 2 24.08 1968.86
DCK12A 1968 D 1 24.13 1968.71
DCK12A 1968 W 5 23.99 1968.57
DCK12A 1968 W 4 23.07 1968.43
DCK12A 1968 W 3 23.52 1968.29
DCK12A 1968 W 2 23.98 1968.14
DCK12A 1968 W 1 26.66 1968.00
DCK12A 1967 D 2 23.72 1967.88
DCK12A 1967 D 1 20.57 1967.75
DCK12A 1967 W 6 21.55 1967.63
180

DCK12A 1967 W 5 23.01 1967.50
DCK12A 1967 W 4 23.37 1967.38
DCK12A 1967 W 3 23.02 1967.25
DCK12A 1967 W 2 24.10 1967.13
DCK12A 1967 W 1 25.57 1967.00
DCK12A 1966 D 2 24.61 1966.90
DCK12A 1966 D 1 24.36 1966.80
DCK12A 1966 W 8 23.93 1966.70
DCK12A 1966 W 7 22.73 1966.60
DCK12A 1966 W 6 22.35 1966.50
DCK12A 1966 W 5 23.06 1966.40
DCK12A 1966 W 4 23.54 1966.30
DCK12A 1966 W 3 23.17 1966.20
DCK12A 1966 W 2 23.10 1966.10
DCK12A 1966 W 1 24.03 1966.00
DCK12A 1965 D 3 25.17 1965.90
DCK12A 1965 D 2 24.21 1965.80
DCK12A 1965 D 1 23.35 1965.70
DCK12A 1965 W 7 22.89 1965.60
DCK12A 1965 W 6 22.79 1965.50
DCK12A 1965 W 5 23.30 1965.40
DCK12A 1965 W 4 24.68 1965.30
DCK12A 1965 W 3 25.27 1965.20
DCK12A 1965 W 2 25.84 1965.10
DCK12A 1965 W 1 25.97 1965.00
DCK12A 1964 D 2 24.11 1964.92
DCK12A 1964 D 1 22.16 1964.85
DCK12A 1964 W 11 21.36 1964.77
DCK12A 1964 W 10 21.58 1964.69
DCK12A 1964 W 9 22.39 1964.62
DCK12A 1964 W 8 22.60 1964.54
DCK12A 1964 W 7 22.69 1964.46
DCK12A 1964 W 6 22.00 1964.38
DCK12A 1964 W 5 21.68 1964.31
DCK12A 1964 W 4 21.92 1964.23
DCK12A 1964 W 3 22.70 1964.15
DCK12A 1964 W 2 23.56 1964.08
DCK12A 1964 W 1 24.41 1964.00
DCK12A 1963 D 2 24.20 1963.88
DCK12A 1963 D 1 22.96 1963.75
DCK12A 1963 W 6 22.83 1963.63
DCK12A 1963 W 5 22.74 1963.50
DCK12A 1963 W 4 22.60 1963.38
DCK12A 1963 W 3 22.74 1963.25
DCK12A 1963 W 2 22.91 1963.13
DCK12A 1963 W 1 24.85 1963.00
DCK12A 1962 D 2 24.48 1962.89
DCK12A 1962 D 1 21.59 1962.78
181

DCK12A 1962 W 7 20.58 1962.67
DCK12A 1962 W 6 21.98 1962.56
DCK12A 1962 W 5 22.64 1962.44
DCK12A 1962 W 4 21.69 1962.33
DCK12A 1962 W 3 23.31 1962.22
DCK12A 1962 W 2 24.76 1962.11
DCK12A 1962 W 1 24.10 1962.00
DCK12A 1961 D N/A 21.40 1961.80
DCK12A 1961 W 4 22.20 1961.60
DCK12A 1961 W 3 22.88 1961.40
DCK12A 1961 W 2 23.65 1961.20
DCK12A 1961 W 1 24.33 1961.00
DCK12A 1960 D N/A 21.92 1960.80
DCK12A 1960 W 4 22.65 1960.60
DCK12A 1960 W 3 23.12 1960.40
DCK12A 1960 W 2 23.13 1960.20
DCK12A 1960 W 1 24.01 1960.00
DCK12A 1959 D N/A 22.43 1959.80
DCK12A 1959 W 4 23.09 1959.60
DCK12A 1959 W 3 22.99 1959.40
DCK12A 1959 W 2 22.88 1959.20
DCK12A 1959 W 1 24.50 1959.00
DCK12A 1958 D N/A 22.32 1958.80
DCK12A 1958 D N/A 23.04 1958.60
DCK12A 1958 W 3 22.09 1958.40
DCK12A 1958 W 2 23.98 1958.20
DCK12A 1958 W 1 24.04 1958.00
DCK12A 1957 D N/A 22.58 1957.67
DCK12A 1957 W 2 21.94 1957.33
DCK12A 1957 W 1 22.62 1957.00
DCK12A 1956 D N/A 22.18 1956.67
DCK12A 1956 W 2 22.27 1956.33
DCK12A 1956 W 1 21.73 1956.00
DCK12A 1955 D N/A 21.30 1955.50
DCK12A 1955 W N/A 22.08 1955.00
DCK12A 1954 D N/A 22.61 1954.67
DCK12A 1954 W 2 22.89 1954.33
DCK12A 1954 W 1 22.12 1954.00
DCK12A 1953 D N/A 21.40 1953.67
DCK12A 1953 W 2 22.09 1953.33
DCK12A 1953 W 1 22.80 1953.00
DCK12A 1952 D 2 21.90 1952.67
DCK12A 1952 D 1 22.40 1952.33
DCK12A 1952 W N/A 23.23 1952.00
DCK12A 1951 D 3 22.63 1951.86
DCK12A 1951 D 2 21.73 1951.71
DCK12A 1951 D 1 22.67 1951.57
DCK12A 1951 W 4 23.00 1951.43
182

DCK12A 1951 W 3 22.68 1951.29
DCK12A 1951 W 2 23.23 1951.14
DCK12A 1951 W 1 24.53 1951.00
DCK12A 1950 D N/A 21.83 1950.86
DCK12A 1950 W 6 21.02 1950.71
DCK12A 1950 W 5 21.88 1950.57
DCK12A 1950 W 4 24.07 1950.43
DCK12A 1950 W 3 24.53 1950.29
DCK12A 1950 W 2 24.13 1950.14
DCK12A 1950 W 1 24.16 1950.00
DCK12A 1949 D 2 21.36 1949.91
DCK12A 1949 D 1 21.20 1949.82
DCK12A 1949 W 9 21.63 1949.73
DCK12A 1949 W 8 22.48 1949.64
DCK12A 1949 W 7 23.36 1949.55
DCK12A 1949 W 6 23.29 1949.45
DCK12A 1949 W 5 23.10 1949.36
DCK12A 1949 W 4 24.04 1949.27
DCK12A 1949 W 3 24.81 1949.18
DCK12A 1949 W 2 25.91 1949.09
DCK12A 1949 W 1 26.63 1949.00
DCK12A 1948 M N/A 26.28 1948.93
DCK12A 1948 D 3 23.96 1948.87
DCK12A 1948 D 2 23.08 1948.80
DCK12A 1948 D 1 22.60 1948.73
DCK12A 1948 W 11 22.87 1948.67
DCK12A 1948 W 10 22.91 1948.60
DCK12A 1948 W 9 23.01 1948.53
DCK12A 1948 W 8 23.19 1948.47
DCK12A 1948 W 7 23.64 1948.40
DCK12A 1948 W 6 24.73 1948.33
DCK12A 1948 W 5 25.19 1948.27
DCK12A 1948 W 4 25.50 1948.20
DCK12A 1948 W 3 26.10 1948.13
DCK12A 1948 W 2 26.39 1948.07
DCK12A 1948 W 1 28.90 1948.00
DCK12A 1947 D 2 27.87 1947.94
DCK12A 1947 D 1 26.78 1947.88
DCK12A 1947 W 15 25.50 1947.82
DCK12A 1947 W 14 22.26 1947.76
DCK12A 1947 W 13 21.42 1947.71
DCK12A 1947 W 12 21.40 1947.65
DCK12A 1947 W 11 20.17 1947.59
DCK12A 1947 W 10 20.17 1947.53
DCK12A 1947 W 9 20.68 1947.47
DCK12A 1947 W 8 22.93 1947.41
DCK12A 1947 W 7 24.68 1947.35
DCK12A 1947 W 6 24.48 1947.29
183

DCK12A 1947 W 5 23.89 1947.24
DCK12A 1947 W 4 22.71 1947.18
DCK12A 1947 W 3 22.86 1947.12
DCK12A 1947 W 2 23.58 1947.06
DCK12A 1947 W 1 25.24 1947.00
DCK12A 1946 D 3 25.32 1946.93
DCK12A 1946 D 2 23.86 1946.87
DCK12A 1946 D 1 22.43 1946.80
DCK12A 1946 W 12 22.45 1946.73
DCK12A 1946 W 11 22.54 1946.67
DCK12A 1946 W 10 23.35 1946.60
DCK12A 1946 W 9 22.91 1946.53
DCK12A 1946 W 8 22.60 1946.47
DCK12A 1946 W 7 22.89 1946.40
DCK12A 1946 W 6 23.57 1946.33
DCK12A 1946 W 5 24.65 1946.27
DCK12A 1946 W 4 25.07 1946.20
DCK12A 1946 W 3 25.04 1946.13
DCK12A 1946 W 2 24.98 1946.07
DCK12A 1946 W 1 25.86 1946.00
DCK12A 1945 D 3 25.61 1945.94
DCK12A 1945 D 2 25.21 1945.88
DCK12A 1945 D 1 24.00 1945.82
DCK12A 1945 W 14 22.48 1945.76
DCK12A 1945 W 13 20.64 1945.71
DCK12A 1945 W 12 20.54 1945.65
DCK12A 1945 W 11 21.53 1945.59
DCK12A 1945 W 10 22.07 1945.53
DCK12A 1945 W 9 22.01 1945.47
DCK12A 1945 W 8 21.90 1945.41
DCK12A 1945 W 7 22.92 1945.35
DCK12A 1945 W 6 23.72 1945.29
DCK12A 1945 W 5 24.84 1945.24
DCK12A 1945 W 4 25.18 1945.18
DCK12A 1945 W 3 25.27 1945.12
DCK12A 1945 W 2 26.66 1945.06
DCK12A 1945 W 1 28.77 1945.00
DCK12A 1944 D 3 26.32 1944.93
DCK12A 1944 D 2 23.97 1944.86
DCK12A 1944 D 1 22.36 1944.79
DCK12A 1944 W 11 22.10 1944.71
DCK12A 1944 W 10 22.37 1944.64
DCK12A 1944 W 9 22.73 1944.57
DCK12A 1944 W 8 23.34 1944.50
DCK12A 1944 W 7 23.54 1944.43
DCK12A 1944 W 6 23.51 1944.36
DCK12A 1944 W 5 22.86 1944.29
DCK12A 1944 W 4 22.71 1944.21
184

DCK12A 1944 W 3 23.16 1944.14
DCK12A 1944 W 2 24.49 1944.07
DCK12A 1944 W 1 25.33 1944.00
DCK12A 1943 D 3 24.44 1943.92
DCK12A 1943 D 2 22.91 1943.83
DCK12A 1943 D 1 22.00 1943.75
DCK12A 1943 W 9 21.12 1943.67
DCK12A 1943 W 8 21.23 1943.58
DCK12A 1943 W 7 22.57 1943.50
DCK12A 1943 W 6 23.60 1943.42
DCK12A 1943 W 5 24.07 1943.33
DCK12A 1943 W 4 23.72 1943.25
DCK12A 1943 W 3 24.59 1943.17
DCK12A 1943 W 2 25.22 1943.08
DCK12A 1943 W 1 25.28 1943.00
DCK12A 1942 D 3 23.61 1942.90
DCK12A 1942 D 2 22.57 1942.80
DCK12A 1942 D 1 21.40 1942.70
DCK12A 1942 W 7 20.66 1942.60
DCK12A 1942 W 6 21.58 1942.50
DCK12A 1942 W 5 22.76 1942.40
DCK12A 1942 W 4 23.21 1942.30
DCK12A 1942 W 3 23.12 1942.20
DCK12A 1942 W 2 23.16 1942.10
DCK12A 1942 W 1 24.48 1942.00
DCK12A 1941 D 2 23.39 1941.83
DCK12A 1941 D 1 22.84 1941.67
DCK12A 1941 W 4 23.19 1941.50
DCK12A 1941 W 3 23.69 1941.33
DCK12A 1941 W 2 24.80 1941.17
DCK12A 1941 W 1 25.98 1941.00
DCK12A 1940 D 2 24.08 1940.80
DCK12A 1940 D 1 21.93 1940.60
DCK12A 1940 W 3 22.31 1940.40
DCK12A 1940 W 2 24.85 1940.20
DCK12A 1940 W 1 25.35 1940.00
DCK12A 1939 D 2 24.16 1939.86
DCK12A 1939 D 1 23.19 1939.71
DCK12A 1939 W 5 22.09 1939.57
DCK12A 1939 W 4 22.03 1939.43
DCK12A 1939 W 3 22.63 1939.29
DCK12A 1939 W 2 24.45 1939.14
DCK12A 1939 W 1 25.36 1939.00
DCK12A 1938 D 2 25.88 1938.91
DCK12A 1938 D 1 23.46 1938.82
DCK12A 1938 W 9 21.73 1938.73
DCK12A 1938 W 8 21.09 1938.64
DCK12A 1938 W 7 21.13 1938.55
185

DCK12A 1938 W 6 21.54 1938.45
DCK12A 1938 W 5 22.12 1938.36
DCK12A 1938 W 4 22.74 1938.27
DCK12A 1938 W 3 23.40 1938.18
DCK12A 1938 W 2 23.16 1938.09
DCK12A 1938 W 1 24.19 1938.00
DCK12A 1937 D 2 25.79 1937.91
DCK12A 1937 D 1 24.54 1937.82
DCK12A 1937 W 9 21.27 1937.73
DCK12A 1937 W 8 20.90 1937.64
DCK12A 1937 W 7 22.59 1937.55
DCK12A 1937 W 6 23.90 1937.45
DCK12A 1937 W 5 23.31 1937.36
DCK12A 1937 W 4 23.07 1937.27
DCK12A 1937 W 3 23.68 1937.18
DCK12A 1937 W 2 24.34 1937.09
DCK12A 1937 W 1 25.12 1937.00
DCK12A 1936 D 3 28.68 1936.92
DCK12A 1936 D 2 28.51 1936.83
DCK12A 1936 D 1 25.84 1936.75
DCK12A 1936 W 9 24.38 1936.67
DCK12A 1936 W 8 23.60 1936.58
DCK12A 1936 W 7 23.72 1936.50
DCK12A 1936 W 6 23.64 1936.42
DCK12A 1936 W 5 23.46 1936.33
DCK12A 1936 W 4 23.31 1936.25
DCK12A 1936 W 3 23.45 1936.17
DCK12A 1936 W 2 24.43 1936.08
DCK12A 1936 W 1 26.57 1936.00
DCK12A 1935 D 4 25.32 1935.94
DCK12A 1935 D 3 24.33 1935.88
DCK12A 1935 D 2 23.40 1935.81
DCK12A 1935 D 1 22.67 1935.75
DCK12A 1935 W 12 21.56 1935.69
DCK12A 1935 W 11 20.88 1935.63
DCK12A 1935 W 10 20.86 1935.56
DCK12A 1935 W 9 22.23 1935.50
DCK12A 1935 W 8 23.81 1935.44
DCK12A 1935 W 7 24.95 1935.38
DCK12A 1935 W 6 25.17 1935.31
DCK12A 1935 W 5 25.00 1935.25
DCK12A 1935 W 4 24.32 1935.19
DCK12A 1935 W 3 23.65 1935.13
DCK12A 1935 W 2 24.11 1935.06
DCK12A 1935 W 1 25.23 1935.00
DCK12A 1934 D 5 26.66 1934.93
DCK12A 1934 D 4 25.40 1934.87
DCK12A 1934 D 3 24.10 1934.80
186

DCK12A 1934 D 2 22.48 1934.73
DCK12A 1934 D 1 20.53 1934.67
DCK12A 1934 W 10 19.98 1934.60
DCK12A 1934 W 9 20.69 1934.53
DCK12A 1934 W 8 21.45 1934.47
DCK12A 1934 W 7 21.57 1934.40
DCK12A 1934 W 6 21.33 1934.33
DCK12A 1934 W 5 20.55 1934.27
DCK12A 1934 W 4 21.13 1934.20
DCK12A 1934 W 3 22.34 1934.13
DCK12A 1934 W 2 22.93 1934.07
DCK12A 1934 W 1 23.43 1934.00
DCK12A 1933 D 3 25.59 1933.93
DCK12A 1933 D 2 24.12 1933.86
DCK12A 1933 D 1 23.47 1933.79
DCK12A 1933 W 11 22.82 1933.71
DCK12A 1933 W 10 21.86 1933.64
DCK12A 1933 W 9 21.73 1933.57
DCK12A 1933 W 8 22.22 1933.50
DCK12A 1933 W 7 21.77 1933.43
DCK12A 1933 W 6 21.70 1933.36
DCK12A 1933 W 5 21.92 1933.29
DCK12A 1933 W 4 22.32 1933.21
DCK12A 1933 W 3 23.21 1933.14
DCK12A 1933 W 2 24.18 1933.07
DCK12A 1933 W 1 25.31 1933.00
DCK12A 1932 D 2 26.90 1932.94
DCK12A 1932 D 1 25.88 1932.88
DCK12A 1932 W 14 23.65 1932.81
DCK12A 1932 W 13 21.62 1932.75
DCK12A 1932 W 12 21.56 1932.69
DCK12A 1932 W 11 20.98 1932.63
DCK12A 1932 W 10 21.41 1932.56
DCK12A 1932 W 9 22.40 1932.50
DCK12A 1932 W 8 24.83 1932.44
DCK12A 1932 W 7 24.85 1932.38
DCK12A 1932 W 6 24.05 1932.31
DCK12A 1932 W 5 23.69 1932.25
DCK12A 1932 W 4 24.74 1932.19
DCK12A 1932 W 3 26.61 1932.13
DCK12A 1932 W 2 27.25 1932.06
DCK12A 1932 W 1 29.20 1932.00
DCK12A 1931 D 3 29.70 1931.94
DCK12A 1931 D 2 29.05 1931.88
DCK12A 1931 D 1 28.78 1931.81
DCK12A 1931 W 13 27.64 1931.75
DCK12A 1931 W 12 25.94 1931.69
DCK12A 1931 W 11 24.20 1931.63
187

DCK12A 1931 W 10 23.12 1931.56
DCK12A 1931 W 9 22.37 1931.50
DCK12A 1931 W 8 22.74 1931.44
DCK12A 1931 W 7 23.40 1931.38
DCK12A 1931 W 6 24.05 1931.31
DCK12A 1931 W 5 24.14 1931.25
DCK12A 1931 W 4 24.24 1931.19
DCK12A 1931 W 3 23.97 1931.13
DCK12A 1931 W 2 24.48 1931.06
DCK12A 1931 W 1 26.60 1931.00
DCK12A 1930 D 3 28.39 1930.92
DCK12A 1930 D 2 27.30 1930.83
DCK12A 1930 D 1 26.16 1930.75
DCK12A 1930 W 9 23.31 1930.67
DCK12A 1930 W 8 22.17 1930.58
DCK12A 1930 W 7 23.58 1930.50
DCK12A 1930 W 6 24.99 1930.42
DCK12A 1930 W 5 24.69 1930.33
DCK12A 1930 W 4 23.88 1930.25
DCK12A 1930 W 3 23.29 1930.17
DCK12A 1930 W 2 23.61 1930.08
DCK12A 1930 W 1 25.57 1930.00
DCK12A 1929 D 4 28.01 1929.95
DCK12A 1929 D 3 27.80 1929.89
DCK12A 1929 D 2 26.37 1929.84
DCK12A 1929 D 1 25.75 1929.79
DCK12A 1929 W 15 25.62 1929.74
DCK12A 1929 W 14 25.18 1929.68
DCK12A 1929 W 13 24.11 1929.63
DCK12A 1929 W 12 22.76 1929.58
DCK12A 1929 W 11 21.45 1929.53
DCK12A 1929 W 10 21.65 1929.47
DCK12A 1929 W 9 22.49 1929.42
DCK12A 1929 W 8 23.23 1929.37
DCK12A 1929 W 7 25.01 1929.32
DCK12A 1929 W 6 25.67 1929.26
DCK12A 1929 W 5 25.42 1929.21
DCK12A 1929 W 4 25.20 1929.16
DCK12A 1929 W 3 24.99 1929.11
DCK12A 1929 W 2 24.96 1929.05
DCK12A 1929 W 1 26.55 1929.00
DCKx1 1965 D 5 25.09 1965.92
DCKx1 1965 D 4 23.94 1965.85
DCKx1 1965 D 3 22.97 1965.77
DCKx1 1965 D 2 22.18 1965.69
DCKx1 1965 D 1 22.11 1965.62
DCKx1 1965 W 8 21.98 1965.54
188

DCKx1 1965 W 7 22.06 1965.46
DCKx1 1965 W 6 21.88 1965.38
DCKx1 1965 W 5 N/A 1965.31
DCKx1 1965 W 4 24.42 1965.23
DCKx1 1965 W 3 24.59 1965.15
DCKx1 1965 W 2 25.18 1965.08
DCKx1 1965 W 1 25.15 1965.00
DCKx1 1964 D 3 24.77 1964.88
DCKx1 1964 D 2 21.25 1964.75
DCKx1 1964 D 1 19.78 1964.63
DCKx1 1964 W 5 20.16 1964.50
DCKx1 1964 W 4 21.05 1964.38
DCKx1 1964 W 3 21.99 1964.25
DCKx1 1964 W 2 21.51 1964.13
DCKx1 1964 W 1 20.74 1964.00
DCKx1 1963 D 2 23.60 1963.86
DCKx1 1963 D 1 22.52 1963.71
DCKx1 1963 W 5 21.31 1963.57
DCKx1 1963 W 4 22.44 1963.43
DCKx1 1963 W 3 22.15 1963.29
DCKx1 1963 W 2 21.95 1963.14
DCKx1 1963 W 1 24.72 1963.00
DCKx1 1962 D 5 26.24 1962.92
DCKx1 1962 D 4 25.56 1962.85
DCKx1 1962 D 3 24.02 1962.77
DCKx1 1962 D 2 20.88 1962.69
DCKx1 1962 D 1 20.99 1962.62
DCKx1 1962 W 8 20.14 1962.54
DCKx1 1962 W 7 21.01 1962.46
DCKx1 1962 W 6 21.94 1962.38
DCKx1 1962 W 5 22.00 1962.31
DCKx1 1962 W 4 22.49 1962.23
DCKx1 1962 W 3 N/A 1962.15
DCKx1 1962 W 2 25.47 1962.08
DCKx1 1962 W 1 24.11 1962.00
DCKx1 1961 D 8 26.51 1961.96
DCKx1 1961 D 7 26.31 1961.91
DCKx1 1961 D 6 25.66 1961.87
DCKx1 1961 D 5 25.30 1961.83
DCKx1 1961 D 4 23.29 1961.78
DCKx1 1961 D 3 22.29 1961.74
DCKx1 1961 D 2 20.78 1961.70
DCKx1 1961 D 1 21.00 1961.65
DCKx1 1961 W 15 19.66 1961.61
DCKx1 1961 W 14 19.86 1961.57
DCKx1 1961 W 13 20.17 1961.52
DCKx1 1961 W 12 20.79 1961.48
DCKx1 1961 W 11 20.91 1961.43
189

DCKx1 1961 W 10 21.30 1961.39
DCKx1 1961 W 9 20.90 1961.35
DCKx1 1961 W 8 21.47 1961.30
DCKx1 1961 W 7 21.83 1961.26
DCKx1 1961 W 6 21.71 1961.22
DCKx1 1961 W 5 22.30 1961.17
DCKx1 1961 W 4 22.55 1961.13
DCKx1 1961 W 3 22.63 1961.09
DCKx1 1961 W 2 23.56 1961.04
DCKx1 1961 W 1 24.43 1961.00
DCKx1 1960 D 5 24.00 1960.92
DCKx1 1960 D 4 24.48 1960.85
DCKx1 1960 D 3 24.62 1960.77
DCKx1 1960 D 2 22.92 1960.69
DCKx1 1960 D 1 21.59 1960.62
DCKx1 1960 W 8 21.42 1960.54
DCKx1 1960 W 7 20.33 1960.46
DCKx1 1960 W 6 19.69 1960.38
DCKx1 1960 W 5 20.58 1960.31
DCKx1 1960 W 4 22.25 1960.23
DCKx1 1960 W 3 21.94 1960.15
DCKx1 1960 W 2 21.98 1960.08
DCKx1 1960 W 1 23.36 1960.00
DCKx1 1959 D 5 25.97 1959.94
DCKx1 1959 D 4 25.49 1959.88
DCKx1 1959 D 3 25.28 1959.82
DCKx1 1959 D 2 25.04 1959.76
DCKx1 1959 D 1 24.22 1959.71
DCKx1 1959 W 12 23.19 1959.65
DCKx1 1959 W 11 21.75 1959.59
DCKx1 1959 W 10 20.75 1959.53
DCKx1 1959 W 9 19.98 1959.47
DCKx1 1959 W 8 19.93 1959.41
DCKx1 1959 W 7 20.72 1959.35
DCKx1 1959 W 6 22.53 1959.29
DCKx1 1959 W 5 23.22 1959.24
DCKx1 1959 W 4 22.25 1959.18
DCKx1 1959 W 3 22.00 1959.12
DCKx1 1959 W 2 22.10 1959.06
DCKx1 1959 W 1 23.60 1959.00
DCKx1 1958 D 4 28.04 1958.93
DCKx1 1958 D 3 26.42 1958.86
DCKx1 1958 D 2 24.39 1958.79
DCKx1 1958 D 1 21.62 1958.71
DCKx1 1958 W 10 22.18 1958.64
DCKx1 1958 W 9 21.59 1958.57
DCKx1 1958 W 8 20.81 1958.50
DCKx1 1958 W 7 20.22 1958.43
190

DCKx1 1958 W 6 20.77 1958.36
DCKx1 1958 W 5 21.02 1958.29
DCKx1 1958 W 4 22.91 1958.21
DCKx1 1958 W 3 23.68 1958.14
DCKx1 1958 W 2 23.43 1958.07
DCKx1 1958 W 1 23.38 1958.00
DCKx1 1957 D 1 24.16 1957.80
DCKx1 1957 W 4 21.79 1957.60
DCKx1 1957 W 3 21.15 1957.40
DCKx1 1957 W 2 21.22 1957.20
DCKx1 1957 W 1 23.20 1957.00
DCKx1 1956 D 3 25.26 1956.92
DCKx1 1956 D 2 24.61 1956.85
DCKx1 1956 D 1 23.26 1956.77
DCKx1 1956 W 10 21.89 1956.69
DCKx1 1956 W 9 21.21 1956.62
DCKx1 1956 W 8 20.44 1956.54
DCKx1 1956 W 7 20.65 1956.46
DCKx1 1956 W 6 21.25 1956.38
DCKx1 1956 W 5 19.12 1956.31
DCKx1 1956 W 4 21.11 1956.23
DCKx1 1956 W 3 21.40 1956.15
DCKx1 1956 W 2 22.18 1956.08
DCKx1 1956 W 1 23.09 1956.00
DCKx1 1955 D 2 24.63 1955.86
DCKx1 1955 D 1 22.77 1955.71
DCKx1 1955 W 5 21.85 1955.57
DCKx1 1955 W 4 20.59 1955.43
DCKx1 1955 W 3 20.60 1955.29
DCKx1 1955 W 2 22.19 1955.14
DCKx1 1955 W 1 23.69 1955.00
DCKx1 1954 D 2 24.14 1954.91
DCKx1 1954 D 1 22.41 1954.82
DCKx1 1954 W 9 20.46 1954.73
DCKx1 1954 W 8 21.10 1954.64
DCKx1 1954 W 7 21.69 1954.55
DCKx1 1954 W 6 22.11 1954.45
DCKx1 1954 W 5 21.69 1954.36
DCKx1 1954 W 4 21.14 1954.27
DCKx1 1954 W 3 20.51 1954.18
DCKx1 1954 W 2 20.82 1954.09
DCKx1 1954 W 1 22.12 1954.00
DCKx1 1953 D 6 22.55 1953.93
DCKx1 1953 D 5 21.34 1953.87
DCKx1 1953 D 4 21.63 1953.80
DCKx1 1953 D 3 20.73 1953.73
DCKx1 1953 D 2 20.78 1953.67
DCKx1 1953 D 1 21.34 1953.60
191

DCKx1 1953 W 9 21.36 1953.53
DCKx1 1953 W 8 20.95 1953.47
DCKx1 1953 W 7 21.12 1953.40
DCKx1 1953 W 6 21.11 1953.33
DCKx1 1953 W 5 22.63 1953.27
DCKx1 1953 W 4 23.10 1953.20
DCKx1 1953 W 3 23.06 1953.13
DCKx1 1953 W 2 24.71 1953.07
DCKx1 1953 W 1 26.64 1953.00
DCKx1 1952 D 7 27.08 1952.94
DCKx1 1952 D 6 27.00 1952.88
DCKx1 1952 D 5 25.55 1952.82
DCKx1 1952 D 4 23.19 1952.76
DCKx1 1952 D 3 22.23 1952.71
DCKx1 1952 D 2 21.66 1952.65
DCKx1 1952 D 1 21.70 1952.59
DCKx1 1952 W 10 21.97 1952.53
DCKx1 1952 W 9 21.83 1952.47
DCKx1 1952 W 8 22.22 1952.41
DCKx1 1952 W 7 22.49 1952.35
DCKx1 1952 W 6 22.63 1952.29
DCKx1 1952 W 5 22.71 1952.24
DCKx1 1952 W 4 23.29 1952.18
DCKx1 1952 W 3 24.26 1952.12
DCKx1 1952 W 2 25.08 1952.06
DCKx1 1952 W 1 25.10 1952.00
DCKx1 1951 D 6 24.59 1951.93
DCKx1 1951 D 5 23.27 1951.86
DCKx1 1951 D 4 22.89 1951.79
DCKx1 1951 D 3 22.15 1951.71
DCKx1 1951 D 2 20.86 1951.64
DCKx1 1951 D 1 20.02 1951.57
DCKx1 1951 W 8 20.70 1951.50
DCKx1 1951 W 7 21.14 1951.43
DCKx1 1951 W 6 21.32 1951.36
DCKx1 1951 W 5 21.97 1951.29
DCKx1 1951 W 4 22.49 1951.21
DCKx1 1951 W 3 21.90 1951.14
DCKx1 1951 W 2 22.30 1951.07
DCKx1 1951 W 1 24.89 1951.00
DCKx2 1958 D 10 N/A 1958.95
DCKx2 1958 D 9 N/A 1958.90
DCKx2 1958 D 8 N/A 1958.85
DCKx2 1958 D 7 N/A 1958.80
DCKx2 1958 D 6 N/A 1958.75
DCKx2 1958 D 5 N/A 1958.70
DCKx2 1958 D 4 N/A 1958.65
192

DCKx2 1958 D 3 N/A 1958.60
DCKx2 1958 D 2 N/A 1958.55
DCKx2 1958 D 1 22.49 1958.50
DCKx2 1958 W 10 21.52 1958.45
DCKx2 1958 W 9 20.95 1958.40
DCKx2 1958 W 8 19.99 1958.35
DCKx2 1958 W 7 21.63 1958.30
DCKx2 1958 W 6 23.16 1958.25
DCKx2 1958 W 5 23.41 1958.20
DCKx2 1958 W 4 22.21 1958.15
DCKx2 1958 W 3 23.27 1958.10
DCKx2 1958 W 2 25.02 1958.05
DCKx2 1958 W 1 26.89 1958.00
DCKx2 1957 D 4 25.91 1957.92
DCKx2 1957 D 3 23.68 1957.83
DCKx2 1957 D 2 22.14 1957.75
DCKx2 1957 D 1 21.31 1957.67
DCKx2 1957 W 8 21.15 1957.58
DCKx2 1957 W 7 21.04 1957.50
DCKx2 1957 W 6 21.57 1957.42
DCKx2 1957 W 5 21.95 1957.33
DCKx2 1957 W 4 23.42 1957.25
DCKx2 1957 W 3 23.61 1957.17
DCKx2 1957 W 2 24.06 1957.08
DCKx2 1957 W 1 22.62 1957.00
DCKx2 1956 D 2 21.07 1956.83
DCKx2 1956 D 1 20.91 1956.67
DCKx2 1956 W 4 21.24 1956.50
DCKx2 1956 W 3 21.87 1956.33
DCKx2 1956 W 2 21.89 1956.17
DCKx2 1956 W 1 22.51 1956.00
DCKx2 1955 D 3 21.79 1955.90
DCKx2 1955 D 2 20.75 1955.80
DCKx2 1955 D 1 19.81 1955.70
DCKx2 1955 W 7 19.46 1955.60
DCKx2 1955 W 6 20.19 1955.50
DCKx2 1955 W 5 21.50 1955.40
DCKx2 1955 W 4 22.99 1955.30
DCKx2 1955 W 3 23.89 1955.20
DCKx2 1955 W 2 23.93 1955.10
DCKx2 1955 W 1 23.86 1955.00
DCKx2 1954 D 8 24.07 1954.96
DCKx2 1954 D 7 22.05 1954.92
DCKx2 1954 D 6 20.76 1954.88
DCKx2 1954 D 5 20.37 1954.83
DCKx2 1954 D 4 20.41 1954.79
DCKx2 1954 D 3 21.25 1954.75
DCKx2 1954 D 2 21.84 1954.71
193

DCKx2 1954 D 1 22.38 1954.67
DCKx2 1954 W 16 22.31 1954.63
DCKx2 1954 W 15 21.88 1954.58
DCKx2 1954 W 14 21.55 1954.54
DCKx2 1954 W 13 21.75 1954.50
DCKx2 1954 W 12 21.94 1954.46
DCKx2 1954 W 11 22.20 1954.42
DCKx2 1954 W 10 22.60 1954.38
DCKx2 1954 W 9 22.98 1954.33
DCKx2 1954 W 8 23.70 1954.29
DCKx2 1954 W 7 24.06 1954.25
DCKx2 1954 W 6 24.29 1954.21
DCKx2 1954 W 5 23.86 1954.17
DCKx2 1954 W 4 23.71 1954.13
DCKx2 1954 W 3 23.81 1954.08
DCKx2 1954 W 2 22.88 1954.04
DCKx2 1954 W 1 23.08 1954.00
DCKx2 1953 D 11 23.61 1953.96
DCKx2 1953 D 10 22.85 1953.91
DCKx2 1953 D 9 22.39 1953.87
DCKx2 1953 D 8 21.61 1953.83
DCKx2 1953 D 7 20.58 1953.78
DCKx2 1953 D 6 20.57 1953.74
DCKx2 1953 D 5 N/A 1953.70
DCKx2 1953 D 4 N/A 1953.65
DCKx2 1953 D 3 N/A 1953.61
DCKx2 1953 D 2 N/A 1953.57
DCKx2 1953 D 1 N/A 1953.52
DCKx2 1953 W 12 N/A 1953.48
DCKx2 1953 W 11 N/A 1953.43
DCKx2 1953 W 10 N/A 1953.39
DCKx2 1953 W 9 N/A 1953.35
DCKx2 1953 W 8 N/A 1953.30
DCKx2 1953 W 7 N/A 1953.26
DCKx2 1953 W 6 N/A 1953.22
DCKx2 1953 W 5 N/A 1953.17
DCKx2 1953 W 4 N/A 1953.13
DCKx2 1953 W 3 N/A 1953.09
DCKx2 1953 W 2 N/A 1953.04
DCKx2 1953 W 1 N/A 1953.00

194

Appendix B. DCK cellulose δ
18
O annual maxima, minima and
mean values

Year δ
18
Omax(‰) δ
18
Omin(‰) δ
18
Omean(‰)
1922 N/A 18.32 20.38
1923 27.74 19.06 23.79
1924 30.10 17.46 22.23
1925 28.58 17.00 22.31
1926 28.37 15.31 20.75
1927 26.94 20.52 23.61
1928 26.61 21.24 23.97
1929 26.35 20.27 23.39
1930 26.17 21.63 24.07
1931 27.35 21.47 24.36
1932 28.26 19.84 23.04
1933 25.45 20.62 22.22
1934 25.52 19.31 22.01
1935 26.26 20.15 22.97
1936 25.86 23.54 25.26
1937 28.75 21.16 23.80
1938 26.50 21.66 22.96
1939 26.46 21.73 23.43
1940 25.63 20.93 23.62
1941 26.07 22.36 23.89
1942 24.78 20.91 22.81
1943 25.03 21.19 23.14
1944 24.80 22.05 23.38
1945 27.66 20.73 23.64
1946 25.45 22.42 23.80
1947 25.29 20.51 23.41
1948 27.90 22.30 24.15
1949 26.02 20.96 23.01
1950 24.83 20.23 22.53
1951 25.03 20.54 22.76
1952 25.20 21.43 22.94
1953 27.78 20.49 22.50
1954 25.24 20.29 22.78
1955 24.82 19.60 22.47
1956 25.32 19.89 22.19
1957 25.11 21.13 22.97
1958 26.99 20.24 23.31
1959 28.55 20.13 23.12
1960 26.52 20.38 22.79
1961 24.47 20.03 22.57
195

1962 25.51 20.04 22.76
1963 25.69 21.55 22.81
1964 24.44 20.24 21.92
1965 25.49 21.85 23.64
1966 25.38 21.83 23.49
1967 25.59 19.80 22.43
1968 25.26 22.79 23.93
1969 25.40 21.56 23.40
1970 24.94 20.72 22.51
1971 24.77 21.75 23.58
1972 26.00 22.15 23.99
1973 24.36 18.36 21.61
1974 25.23 21.54 23.12
1975 24.75 19.63 21.77
1976 25.20 20.32 22.73
1977 25.76 22.21 23.80
1978 23.75 20.56 21.51
1979 24.47 23.46 24.57
1980 25.66 22.05 22.98
1981 23.21 22.28 22.86
1982 23.70 22.02 22.89
1983 23.07 20.41 21.32
1984 23.34 22.52 23.16
1985 24.62 23.51 24.58
1986 25.21 23.47 24.12
1987 25.70 20.97 23.39
1988 23.96 20.79 21.81
1989 23.68 21.57 22.44
1990 23.59 22.23 23.03
1991 24.21 22.60 23.34
1992 23.14 20.97 21.64
1993 24.99 22.33 23.94
1994 24.19 21.36 23.01
1995 24.08 20.71 21.52
1996 24.08 20.99 22.60
1997 24.02 23.47 24.16
1998 26.59 20.91 22.95
1999 24.95 22.58 23.98
2000 24.06 22.70 23.40
2001 24.12 N/A N/A

196

Appendix C. KRPM age-adjusted subannual cellulose δ
18
O
values

Core Age δ
18
O(‰)
KRPM09A 1869.75 23.84
KRPM09A 1869.81 24.02
KRPM09A 1869.86 25.79
KRPM09A 1869.92 27.69
KRPM09A 1869.97 28.53
KRPM09A 1870.03 29.55
KRPM09A 1870.08 30.21
KRPM09A 1870.25 29.48
KRPM09A 1870.42 26.11
KRPM09A 1870.58 24.31
KRPM09A 1870.75 23.88
KRPM09A 1870.83 25.10
KRPM09A 1870.92 26.51
KRPM09A 1871.00 27.51
KRPM09A 1871.08 28.39
KRPM09A 1871.42 23.65
KRPM09A 1871.75 22.80
KRPM09A 1871.83 23.67
KRPM09A 1871.92 25.12
KRPM09A 1872.00 26.91
KRPM09A 1872.08 27.54
KRPM09A 1872.42 23.57
KRPM09A 1872.75 22.53
KRPM09A 1872.82 24.30
KRPM09A 1872.88 26.03
KRPM09A 1872.95 27.62
KRPM09A 1873.02 28.98
KRPM09A 1873.08 29.81
KRPM09A 1873.25 25.72
KRPM09A 1873.42 24.02
KRPM09A 1873.58 23.38
KRPM09A 1873.75 23.38
KRPM09A 1873.82 23.62
KRPM09A 1873.88 25.13
KRPM09A 1873.95 26.41
KRPM09A 1874.02 28.13
KRPM09A 1874.08 28.74
KRPM09A 1874.42 24.19
KRPM09A 1874.75 21.74
KRPM09A 1874.82 22.28
197

KRPM09A 1874.88 24.17
KRPM09A 1874.95 24.95
KRPM09A 1875.02 25.70
KRPM09A 1875.08 25.73
KRPM09A 1875.42 25.19
KRPM09A 1875.75 24.21
KRPM09A 1875.92 27.26
KRPM09A 1876.08 26.86
KRPM09A 1876.75 22.91
KRPM09A 1876.86 23.19
KRPM09A 1876.97 25.27
KRPM09A 1877.08 26.26
KRPM09A 1877.75 23.46
KRPM09A 1877.86 24.30
KRPM09A 1877.97 26.12
KRPM09A 1878.08 28.46
KRPM09A 1878.42 24.69
KRPM09A 1878.75 23.66
KRPM09A 1878.92 25.54
KRPM09A 1879.08 27.10
KRPM09A 1879.25 26.67
KRPM09A 1879.42 24.05
KRPM09A 1879.58 24.20
KRPM09A 1879.75 24.23
KRPM09A 1879.86 24.85
KRPM09A 1879.97 26.11
KRPM09A 1880.08 27.66
KRPM09A 1880.42 24.85
KRPM09A 1880.75 23.02
KRPM09A 1882.00 N/A
KRPM09A 1883.00 N/A
KRPM09A 1884.00 N/A
KRPM09A 1885.08 27.32
KRPM09A 1885.25 24.38
KRPM09A 1885.42 23.77
KRPM09A 1885.58 23.74
KRPM09A 1885.75 23.68
KRPM09A 1885.86 24.06
KRPM09A 1885.97 25.66
KRPM09A 1886.08 28.65
KRPM09A 1886.42 24.10
KRPM09A 1886.75 23.76
KRPM09A 1886.82 24.05
KRPM09A 1886.88 24.29
KRPM09A 1886.95 24.92
KRPM09A 1887.02 26.22
KRPM09A 1887.08 28.12
KRPM09A 1887.75 23.59
198

KRPM09A 1887.83 25.47
KRPM09A 1887.92 25.40
KRPM09A 1888.00 24.66
KRPM09A 1888.08 27.45
KRPM09A 1888.42 26.19
KRPM09A 1888.75 24.44
KRPM09A 1888.86 25.30
KRPM09A 1888.97 26.56
KRPM09A 1889.08 27.24
KRPM09A 1889.31 23.55
KRPM09A 1889.53 22.10
KRPM09A 1889.75 21.93
KRPM09A 1889.83 22.04
KRPM09A 1889.92 23.54
KRPM09A 1890.00 25.12
KRPM09A 1890.08 26.27
KRPM09A 1890.25 25.82
KRPM09A 1890.42 24.44
KRPM09A 1890.58 23.27
KRPM09A 1890.75 22.62
KRPM09A 1890.83 23.47
KRPM09A 1890.92 24.91
KRPM09A 1891.00 26.53
KRPM09A 1891.08 27.59
KRPM09A 1891.42 26.57
KRPM09A 1891.75 24.35
KRPM09A 1891.80 24.57
KRPM09A 1891.85 25.45
KRPM09A 1891.89 25.87
KRPM09A 1891.94 26.10
KRPM09A 1891.99 26.95
KRPM09A 1892.04 29.00
KRPM09A 1892.08 30.10
KRPM09A 1892.31 29.58
KRPM09A 1892.53 26.60
KRPM09A 1892.75 23.17
KRPM09A 1892.86 24.52
KRPM09A 1892.97 25.13
KRPM09A 1893.08 27.10
KRPM09A 1893.25 26.27
KRPM09A 1893.42 24.26
KRPM09A 1893.58 24.66
KRPM09A 1893.75 24.10
KRPM09A 1893.86 24.79
KRPM09A 1893.97 26.62
KRPM09A 1894.08 27.85
KRPM09A 1894.22 26.01
KRPM09A 1894.35 25.26
199

KRPM09A 1894.48 24.57
KRPM09A 1894.62 23.53
KRPM09A 1894.75 22.78
KRPM09A 1894.81 23.08
KRPM09A 1894.86 23.55
KRPM09A 1894.92 25.50
KRPM09A 1894.97 27.67
KRPM09A 1895.03 29.30
KRPM09A 1895.08 29.65
KRPM09A 1895.19 26.88
KRPM09A 1895.31 24.12
KRPM09A 1895.42 23.64
KRPM09A 1895.53 24.01
KRPM09A 1895.64 24.47
KRPM09A 1895.75 23.68
KRPM09A 1895.82 24.84
KRPM09A 1895.88 27.17
KRPM09A 1895.95 28.37
KRPM09A 1896.02 28.73
KRPM09A 1896.08 29.52
KRPM09A 1897.00 N/A
KRPM09A 1898.00 N/A
KRPM09A 1900.00 N/A
KRPM09A 1914.08 27.00
KRPM09A 1914.31 25.22
KRPM09A 1914.53 24.67
KRPM09A 1914.75 24.44
KRPM09A 1914.82 25.65
KRPM09A 1914.88 27.03
KRPM09A 1914.95 27.40
KRPM09A 1915.02 28.41
KRPM09A 1915.08 29.40
KRPM09A 1915.31 26.87
KRPM09A 1915.53 23.69
KRPM09A 1915.75 23.46
KRPM09A 1915.86 24.73
KRPM09A 1915.97 26.58
KRPM09A 1916.08 27.86
KRPM09A 1916.42 23.97
KRPM09A 1916.75 23.43
KRPM09A 1916.92 24.74
KRPM09A 1917.08 26.72
KRPM09A 1917.31 24.97
KRPM09A 1917.53 22.59
KRPM09A 1917.75 22.21
KRPM09A 1917.92 24.59
KRPM09A 1918.08 26.04
KRPM09A 1918.75 24.23
200

KRPM09A 1918.81 24.80
KRPM09A 1918.86 25.67
KRPM09A 1918.92 26.70
KRPM09A 1918.97 27.23
KRPM09A 1919.03 28.61
KRPM09A 1919.08 29.19
KRPM09A 1919.42 24.49
KRPM09A 1919.75 24.33
KRPM09A 1919.83 24.58
KRPM09A 1919.92 26.75
KRPM09A 1920.00 27.96
KRPM09A 1920.08 28.19
KRPM09A 1920.25 26.43
KRPM09A 1920.42 26.16
KRPM09A 1920.58 25.16
KRPM09A 1920.75 24.47
KRPM09A 1920.82 24.60
KRPM09A 1920.88 25.33
KRPM09A 1920.95 25.63
KRPM09A 1921.02 26.94
KRPM09A 1921.08 29.27
KRPM09A 1921.42 25.50
KRPM09A 1921.75 23.85
KRPM09A 1921.83 23.88
KRPM09A 1921.92 24.46
KRPM09A 1922.00 26.50
KRPM09A 1922.08 27.68
KRPM09A 1922.25 26.56
KRPM09A 1922.42 25.84
KRPM09A 1922.58 24.45
KRPM09A 1922.75 22.68
KRPM09A 1922.92 23.17
KRPM09A 1923.08 25.32
KRPM09A 1923.75 22.99
KRPM09A 1923.86 23.99
KRPM09A 1923.97 25.50
KRPM09A 1924.08 27.81
KRPM09A 1924.31 24.73
KRPM09A 1924.53 23.55
KRPM09A 1924.75 23.51
KRPM09A 1924.86 24.20
KRPM09A 1924.97 26.44
KRPM09A 1925.08 27.53
KRPM09A 1925.31 26.11
KRPM09A 1925.53 25.73
KRPM09A 1925.75 24.80
KRPM09A 1925.83 25.20
KRPM09A 1925.92 27.34
201

KRPM09A 1926.00 28.04
KRPM09A 1926.08 28.56
KRPM09A 1926.42 23.67
KRPM09A 1926.75 22.07
KRPM09A 1926.82 23.20
KRPM09A 1926.88 24.54
KRPM09A 1926.95 25.03
KRPM09A 1927.02 26.46
KRPM09A 1927.08 27.87
KRPM09A 1927.31 27.36
KRPM09A 1927.53 24.41
KRPM09A 1927.75 24.25
KRPM09A 1927.86 25.17
KRPM09A 1927.97 26.46
KRPM09A 1928.08 27.81
KRPM09A 1928.31 27.71
KRPM09A 1928.53 25.61
KRPM09A 1928.75 24.54
KRPM09A 1928.92 25.67
KRPM09A 1929.08 27.99
KRPM09A 1929.25 27.32
KRPM09A 1929.42 26.32
KRPM09A 1929.58 25.36
KRPM09A 1929.75 24.66
KRPM09A 1929.86 25.76
KRPM09A 1929.97 27.22
KRPM09A 1930.08 28.46
KRPM09A 1930.42 27.39
KRPM09A 1930.75 25.63
KRPM09A 1931.08 26.06
KRPM09A 1931.42 21.74
KRPM09A 1931.75 21.73
KRPM09A 1931.86 24.01
KRPM09A 1931.97 26.46
KRPM09A 1932.08 28.04
KRPM09A 1932.31 24.82
KRPM09A 1932.53 23.44
KRPM09A 1932.75 22.86
KRPM09A 1932.82 22.94
KRPM09A 1932.88 23.99
KRPM09A 1932.95 25.77
KRPM09A 1933.02 26.69
KRPM09A 1933.08 27.03
KRPM09A 1933.75 22.93
KRPM09A 1933.86 23.69
KRPM09A 1933.97 26.16
KRPM09A 1934.08 27.74
KRPM09A 1934.42 25.30
202

KRPM09A 1934.75 25.09
KRPM09A 1934.86 25.90
KRPM09A 1934.97 27.65
KRPM09A 1935.08 28.71
KRPM09A 1935.22 28.36
KRPM09A 1935.35 25.36
KRPM09A 1935.48 25.29
KRPM09A 1935.62 24.04
KRPM09A 1935.75 23.91
KRPM09A 1935.92 25.15
KRPM09A 1936.08 26.61
KRPM09A 1936.42 24.96
KRPM09A 1936.75 23.90
KRPM09A 1936.83 24.98
KRPM09A 1936.92 27.01
KRPM09A 1937.00 27.52
KRPM09A 1937.08 28.61
KRPM09A 1937.42 25.32
KRPM09A 1937.75 23.64
KRPM09A 1937.86 25.03
KRPM09A 1937.97 27.09
KRPM09A 1938.08 28.47
KRPM09A 1938.42 24.97
KRPM09A 1938.75 23.62
KRPM09A 1938.92 24.12
KRPM09A 1939.08 27.58
KRPM09A 1939.31 27.51
KRPM09A 1939.53 26.40
KRPM09A 1939.75 23.95
KRPM09A 1940.08 26.73
KRPM09A 1965.00 N/A
KRPM09A 1968.08 28.60
KRPM09A 1968.25 26.72
KRPM09A 1968.42 25.80
KRPM09A 1968.58 24.72
KRPM09A 1968.75 23.90
KRPM09A 1968.86 26.05
KRPM09A 1968.97 27.64
KRPM09A 1969.08 27.72
KRPM09A 1969.25 26.30
KRPM09A 1969.42 24.65
KRPM09A 1969.58 23.48
KRPM09A 1969.75 23.06
KRPM09A 1969.86 23.66
KRPM09A 1969.97 24.98
KRPM09A 1970.08 25.49
KRPM09A 1970.31 24.72
KRPM09A 1970.53 24.04
203

KRPM09A 1970.75 23.15
KRPM09A 1970.86 24.05
KRPM09A 1970.97 25.60
KRPM09A 1971.08 26.08
KRPM09A 1971.31 25.82
KRPM09A 1971.53 24.77
KRPM09A 1971.75 23.78
KRPM09A 1971.86 23.93
KRPM09A 1971.97 26.36
KRPM09A 1972.08 27.00
KRPM09A 1972.25 25.73
KRPM09A 1972.42 26.05
KRPM09A 1972.58 24.99
KRPM09A 1972.75 23.93
KRPM09A 1972.86 24.64
KRPM09A 1972.97 25.67
KRPM09A 1973.08 27.94
KRPM09A 1973.22 25.62
KRPM09A 1973.35 25.48
KRPM09A 1973.48 24.63
KRPM09A 1973.62 23.81
KRPM09A 1973.75 21.48
KRPM09A 1973.86 22.44
KRPM09A 1973.97 25.19
KRPM09A 1974.08 25.61
KRPM09A 1974.19 24.61
KRPM09A 1974.31 24.02
KRPM09A 1974.42 24.94
KRPM09A 1974.53 25.43
KRPM09A 1974.64 23.95
KRPM09A 1974.75 22.12
KRPM09A 1974.86 24.65
KRPM09A 1974.97 25.13
KRPM09A 1975.08 25.35
KRPM09A 1975.25 24.77
KRPM09A 1975.42 24.09
KRPM09A 1975.58 23.13
KRPM09A 1975.75 21.30
KRPM09A 1975.81 23.13
KRPM09A 1975.86 26.18
KRPM09A 1975.92 26.48
KRPM09A 1975.97 24.34
KRPM09A 1976.03 26.08
KRPM09A 1976.08 26.97
KRPM09A 1976.19 26.78
KRPM09A 1976.31 26.42
KRPM09A 1976.42 26.16
KRPM09A 1976.53 26.01
204

KRPM09A 1976.64 25.09
KRPM09A 1976.75 23.78
KRPM09A 1976.79 25.43
KRPM09A 1976.83 25.20
KRPM09A 1976.88 24.45
KRPM09A 1976.92 24.94
KRPM09A 1976.96 26.72
KRPM09A 1977.00 28.60
KRPM09A 1977.04 28.40
KRPM09A 1977.08 29.05
KRPM09A 1977.18 27.91
KRPM09A 1977.27 26.54
KRPM09A 1977.37 26.55
KRPM09A 1977.46 25.73
KRPM09A 1977.56 26.19
KRPM09A 1977.65 26.19
KRPM09A 1977.75 25.69
KRPM09A 1977.82 25.70
KRPM09A 1977.88 25.89
KRPM09A 1977.95 26.26
KRPM09A 1978.02 27.13
KRPM09A 1978.08 28.41
KRPM09A 1978.19 27.42
KRPM09A 1978.31 26.63
KRPM09A 1978.42 25.71
KRPM09A 1978.53 25.43
KRPM09A 1978.64 24.89
KRPM09A 1978.75 24.85
KRPM09A 1978.82 25.11
KRPM09A 1978.88 25.21
KRPM09A 1978.95 25.14
KRPM09A 1979.02 26.47
KRPM09A 1979.08 28.88
KRPM09A 1982.00 N/A
KRPM10A 1880.08 25.89
KRPM10A 1880.75 25.22
KRPM10A 1881.08 27.38
KRPM10A 1881.42 25.15
KRPM10A 1881.75 23.66
KRPM10A 1882.08 26.54
KRPM10A 1882.42 25.36
KRPM10A 1882.75 23.33
KRPM10A 1883.08 27.35
KRPM10A 1883.42 25.80
KRPM10A 1883.75 25.00
KRPM10A 1884.08 26.88
KRPM10A 1884.75 25.31
205

KRPM10A 1884.92 25.52
KRPM10A 1885.08 29.28
KRPM10A 1885.42 25.70
KRPM10A 1885.75 25.26
KRPM10A 1886.08 28.53
KRPM10A 1886.42 23.69
KRPM10A 1886.75 21.82
KRPM10A 1887.08 26.85
KRPM10A 1887.42 24.85
KRPM10A 1887.75 24.48
KRPM10A 1888.08 27.19
KRPM10A 1888.42 26.28
KRPM10A 1888.75 25.88
KRPM10A 1889.08 27.70
KRPM10A 1889.42 25.11
KRPM10A 1889.75 24.12
KRPM10A 1890.08 27.63
KRPM10A 1890.42 25.92
KRPM10A 1890.75 24.52
KRPM10A 1891.08 26.75
KRPM10A 1891.75 25.14
KRPM10A 1891.92 26.55
KRPM10A 1892.08 29.33
KRPM10A 1892.42 26.41
KRPM10A 1892.75 24.20
KRPM10A 1893.08 26.62
KRPM10A 1893.42 24.70
KRPM10A 1893.75 24.30
KRPM10A 1894.08 27.04
KRPM10A 1894.42 25.43
KRPM10A 1894.75 23.81
KRPM10A 1895.08 26.50
KRPM10A 1895.42 24.84
KRPM10A 1895.75 24.36
KRPM10A 1896.08 26.87
KRPM10A 1896.75 26.23
KRPM10A 1896.92 26.28
KRPM10A 1897.08 28.90
KRPM10A 1897.42 24.83
KRPM10A 1897.75 23.24
KRPM10A 1898.08 25.83
KRPM10A 1898.42 24.51
KRPM10A 1898.75 23.81
KRPM10A 1899.08 27.03
KRPM10A 1899.75 24.58
KRPM10A 1899.92 25.83
KRPM10A 1900.08 28.20
KRPM10A 1900.42 26.60
206

KRPM10A 1900.75 25.65
KRPM10A 1901.08 28.42
KRPM10A 1901.75 25.04
KRPM10A 1901.92 25.42
KRPM10A 1902.08 28.85
KRPM10A 1902.42 26.57
KRPM10A 1902.75 25.35
KRPM10A 1903.08 27.79
KRPM10A 1903.75 24.58
KRPM10A 1903.92 24.90
KRPM10A 1904.08 27.78
KRPM10A 1904.42 26.49
KRPM10A 1904.75 24.72
KRPM10A 1905.08 28.10
KRPM10A 1905.42 25.96
KRPM10A 1905.75 25.19
KRPM10A 1906.08 28.22
KRPM10A 1906.75 26.06
KRPM10A 1906.92 26.49
KRPM10A 1907.08 29.05
KRPM10A 1907.42 26.38
KRPM10A 1907.75 26.01
KRPM10A 1908.08 27.26
KRPM10A 1908.42 26.16
KRPM10A 1908.75 25.39
KRPM10A 1909.08 27.37
KRPM10A 1909.42 25.82
KRPM10A 1909.75 24.29
KRPM10A 1909.82 24.38
KRPM10A 1909.88 24.40
KRPM10A 1909.95 24.66
KRPM10A 1910.02 26.77
KRPM10A 1910.08 27.19
KRPM10A 1910.25 26.96
KRPM10A 1910.42 25.67
KRPM10A 1910.58 23.98
KRPM10A 1910.75 23.36
KRPM10A 1910.86 24.78
KRPM10A 1910.97 26.33
KRPM10A 1911.08 27.27
KRPM10A 1911.75 25.43
KRPM10A 1911.86 26.35
KRPM10A 1911.97 28.93
KRPM10A 1912.08 29.82
KRPM10A 1912.22 29.71
KRPM10A 1912.35 29.56
KRPM10A 1912.48 27.16
KRPM10A 1912.62 27.00
207

KRPM10A 1912.75 24.90
KRPM10A 1912.80 25.57
KRPM10A 1912.85 26.17
KRPM10A 1912.89 27.57
KRPM10A 1912.94 28.40
KRPM10A 1912.99 29.26
KRPM10A 1913.04 30.44
KRPM10A 1913.08 30.70
KRPM10A 1913.18 29.01
KRPM10A 1913.27 26.77
KRPM10A 1913.37 27.36
KRPM10A 1913.46 27.00
KRPM10A 1913.56 26.95
KRPM10A 1913.65 25.47
KRPM10A 1913.75 24.64
KRPM10A 1913.80 25.87
KRPM10A 1913.85 26.02
KRPM10A 1913.89 26.91
KRPM10A 1913.94 27.90
KRPM10A 1913.99 27.91
KRPM10A 1914.04 28.97
KRPM10A 1914.08 29.66
KRPM10A 1914.31 28.74
KRPM10A 1914.53 26.35
KRPM10A 1914.75 24.85
KRPM10A 1914.80 25.68
KRPM10A 1914.85 26.91
KRPM10A 1914.89 27.04
KRPM10A 1914.94 27.09
KRPM10A 1914.99 27.66
KRPM10A 1915.04 28.67
KRPM10A 1915.08 28.90
KRPM10A 1915.25 25.97
KRPM10A 1915.42 25.64
KRPM10A 1915.58 23.71
KRPM10A 1915.75 23.15
KRPM10A 1915.81 23.45
KRPM10A 1915.86 23.86
KRPM10A 1915.92 24.79
KRPM10A 1915.97 26.12
KRPM10A 1916.03 28.37
KRPM10A 1916.08 29.45
KRPM10A 1916.19 28.73
KRPM10A 1916.31 24.62
KRPM10A 1916.42 24.77
KRPM10A 1916.53 23.36
KRPM10A 1916.64 22.88
KRPM10A 1916.75 22.46
208

KRPM10A 1916.79 22.85
KRPM10A 1916.83 25.02
KRPM10A 1916.88 26.35
KRPM10A 1916.92 26.24
KRPM10A 1916.96 26.55
KRPM10A 1917.00 26.95
KRPM10A 1917.04 27.09
KRPM10A 1917.08 27.96
KRPM10A 1917.19 27.69
KRPM10A 1917.31 25.39
KRPM10A 1917.42 24.30
KRPM10A 1917.53 23.23
KRPM10A 1917.64 22.54
KRPM10A 1917.75 21.72
KRPM10A 1917.81 22.12
KRPM10A 1917.86 23.19
KRPM10A 1917.92 23.84
KRPM10A 1917.97 24.85
KRPM10A 1918.03 26.30
KRPM10A 1918.08 27.87
KRPM10A 1918.16 26.55
KRPM10A 1918.23 25.83
KRPM10A 1918.31 25.32
KRPM10A 1918.38 26.26
KRPM10A 1918.45 26.19
KRPM10A 1918.53 24.76
KRPM10A 1918.60 25.18
KRPM10A 1918.68 26.05
KRPM10A 1918.75 24.48
KRPM10A 1918.86 27.69
KRPM10A 1918.97 28.16
KRPM10A 1919.08 28.30
KRPM10A 1918.92 N/A
KRPM10A 1919.00 N/A
KRPM10A 1920.00 N/A
KRPM10A 1921.00 N/A
KRPM10A 1922.00 N/A
KRPM10A 1923.00 N/A
KRPM10A 1924.00 N/A
KRPM10A 1925.00 N/A
KRPM10A 1926.00 N/A
KRPM10A 1927.00 N/A
KRPM10A 1928.00 N/A
KRPM10A 1929.00 N/A
KRPM10A 1930.00 N/A
KRPM10A 1931.00 N/A
KRPM10A 1932.00 N/A
KRPM10A 1933.00 N/A
209

KRPM10A 1934.00 N/A
KRPM10A 1935.00 N/A
KRPM10A 1936.00 N/A
KRPM10A 1937.00 N/A
KRPM10A 1938.00 N/A
KRPM10A 1939.00 N/A
KRPM10A 1939.10 N/A
KRPM10A 1939.20 N/A
KRPM10A 1939.30 N/A
KRPM10A 1939.40 N/A
KRPM10A 1939.50 N/A
KRPM10A 1939.60 N/A
KRPM10A 1939.70 N/A
KRPM10A 1940.08 28.99
KRPM10A 1940.31 28.20
KRPM10A 1940.53 26.23
KRPM10A 1940.75 25.43
KRPM10A 1940.83 26.15
KRPM10A 1940.92 26.72
KRPM10A 1941.00 28.37
KRPM10A 1941.08 29.25
KRPM10A 1941.22 27.72
KRPM10A 1941.35 27.52
KRPM10A 1941.48 26.44
KRPM10A 1941.62 24.85
KRPM10A 1941.75 23.79
KRPM10A 1941.83 24.77
KRPM10A 1941.92 25.73
KRPM10A 1942.00 26.44
KRPM10A 1942.08 28.28
KRPM10A 1942.18 28.24
KRPM10A 1942.27 27.41
KRPM10A 1942.37 26.19
KRPM10A 1942.46 24.93
KRPM10A 1942.56 24.61
KRPM10A 1942.65 24.37
KRPM10A 1942.75 23.97
KRPM10A 1942.83 24.24
KRPM10A 1942.92 24.79
KRPM10A 1943.00 26.15
KRPM10A 1943.08 27.93
KRPM10A 1943.19 27.77
KRPM10A 1943.31 25.61
KRPM10A 1943.42 24.48
KRPM10A 1943.53 24.89
KRPM10A 1943.64 25.30
KRPM10A 1943.75 24.59
KRPM10A 1943.86 25.41
210

KRPM10A 1943.97 27.10
KRPM10A 1944.08 27.51
KRPM10A 1944.25 27.23
KRPM10A 1944.42 25.96
KRPM10A 1944.58 24.88
KRPM10A 1944.75 24.73
KRPM10A 1944.92 25.22
KRPM10A 1945.08 26.75
KRPM10A 1945.18 26.65
KRPM10A 1945.27 26.71
KRPM10A 1945.37 25.09
KRPM10A 1945.46 24.73
KRPM10A 1945.56 25.20
KRPM10A 1945.65 24.77
KRPM10A 1945.75 24.69
KRPM10A 1945.92 26.18
KRPM10A 1946.08 28.18
KRPM10A 1946.22 27.73
KRPM10A 1946.35 25.88
KRPM10A 1946.48 25.16
KRPM10A 1946.62 24.58
KRPM10A 1946.75 23.78
KRPM10A 1946.82 24.67
KRPM10A 1946.88 25.59
KRPM10A 1946.95 26.70
KRPM10A 1947.02 27.08
KRPM10A 1947.08 27.66
KRPM10A 1947.42 26.00
KRPM10A 1947.75 23.93
KRPM10A 1947.83 24.07
KRPM10A 1947.92 26.92
KRPM10A 1948.00 26.72
KRPM10A 1948.08 27.63
KRPM10A 1948.42 25.28
KRPM10A 1948.75 24.32
KRPM10A 1948.83 24.97
KRPM10A 1948.92 27.37
KRPM10A 1949.00 28.69
KRPM10A 1949.08 30.25
KRPM10A 1949.31 26.00
KRPM10A 1949.53 23.65
KRPM10A 1949.75 23.42
KRPM10A 1949.82 23.64
KRPM10A 1949.88 26.22
KRPM10A 1949.95 27.42
KRPM10A 1950.02 28.45
KRPM10A 1950.08 28.74
KRPM10A 1950.19 27.96
211

KRPM10A 1950.31 25.91
KRPM10A 1950.42 23.98
KRPM10A 1950.53 23.64
KRPM10A 1950.64 24.35
KRPM10A 1950.75 23.46
KRPM10A 1950.82 24.41
KRPM10A 1950.88 25.93
KRPM10A 1950.95 28.19
KRPM10A 1951.02 28.90
KRPM10A 1951.08 29.02
KRPM10A 1951.25 27.12
KRPM10A 1951.42 26.17
KRPM10A 1951.58 24.47
KRPM10A 1951.75 22.39
KRPM10A 1951.81 23.24
KRPM10A 1951.86 23.61
KRPM10A 1951.92 23.52
KRPM10A 1951.97 24.92
KRPM10A 1952.03 26.76
KRPM10A 1952.08 27.65
KRPM10A 1952.25 27.16
KRPM10A 1952.42 25.08
KRPM10A 1952.58 24.78
KRPM10A 1952.75 23.65
KRPM10A 1952.86 25.33
KRPM10A 1952.97 26.48
KRPM10A 1953.08 26.76
KRPM10A 1953.22 26.51
KRPM10A 1953.35 26.02
KRPM10A 1953.48 24.85
KRPM10A 1953.62 24.66
KRPM10A 1953.75 24.36
KRPM10A 1953.92 25.51
KRPM10A 1954.08 26.31
KRPM10A 1954.25 24.79
KRPM10A 1954.42 23.68
KRPM10A 1954.58 24.09
KRPM10A 1954.75 22.98
KRPM10A 1954.83 23.35
KRPM10A 1954.92 25.34
KRPM10A 1955.00 27.17
KRPM10A 1955.08 27.96
KRPM10A 1955.18 27.71
KRPM10A 1955.27 25.56
KRPM10A 1955.37 24.80
KRPM10A 1955.46 24.69
KRPM10A 1955.56 24.29
KRPM10A 1955.65 23.18
212

KRPM10A 1955.75 23.16
KRPM10A 1955.82 23.27
KRPM10A 1955.88 23.63
KRPM10A 1955.95 25.42
KRPM10A 1956.02 26.59
KRPM10A 1956.08 26.63
KRPM10A 1956.22 25.75
KRPM10A 1956.35 25.24
KRPM10A 1956.48 24.77
KRPM10A 1956.62 24.24
KRPM10A 1956.75 22.41
KRPM10A 1956.81 23.81
KRPM10A 1956.86 24.32
KRPM10A 1956.92 25.34
KRPM10A 1956.97 26.63
KRPM10A 1957.03 27.63
KRPM10A 1957.08 28.38
KRPM10A 1957.19 27.73
KRPM10A 1957.31 25.96
KRPM10A 1957.42 25.02
KRPM10A 1957.53 24.40
KRPM10A 1957.64 24.47
KRPM10A 1957.75 23.69
KRPM10A 1957.83 24.58
KRPM10A 1957.92 26.01
KRPM10A 1958.00 27.18
KRPM10A 1958.08 27.69
KRPM10A 1958.25 27.07
KRPM10A 1958.42 25.81
KRPM10A 1958.58 24.56
KRPM10A 1958.75 25.01
KRPM10A 1958.92 23.75
KRPM10A 1958.83 N/A
KRPM10A 1959.00 N/A
KRPM10A 1960.08 26.80
KRPM10A 1960.75 24.02
KRPM10A 1960.86 23.42
KRPM10A 1960.97 26.05
KRPM10A 1961.08 27.40
KRPM10A 1961.31 27.24
KRPM10A 1961.53 25.40
KRPM10A 1961.75 24.36
KRPM10A 1961.92 24.98
KRPM10A 1962.08 26.20
KRPM10A 1962.42 25.05
KRPM10A 1962.75 23.62
KRPM10A 1962.92 25.31
KRPM10A 1963.08 27.70
213

KRPM10A 1963.31 24.60
KRPM10A 1963.53 24.80
KRPM10A 1963.75 24.56
KRPM10A 1963.86 25.27
KRPM10A 1963.97 26.81
KRPM10A 1964.08 27.77
KRPM10A 1964.42 24.90
KRPM10A 1964.75 24.61
KRPM10A 1964.92 26.49
KRPM10A 1965.08 27.02
KRPM10A 1965.42 25.81
KRPM10A 1965.75 24.49
KRPM10A 1965.92 24.68
KRPM10A 1966.08 26.52
KRPM10A 1966.42 26.17
KRPM10A 1966.75 25.26
KRPM10A 1966.92 25.64
KRPM10A 1967.08 25.51
KRPM10A 1967.25 24.76
KRPM10A 1967.42 25.51
KRPM10A 1967.58 25.41
KRPM10A 1967.75 25.33
KRPM10A 1967.92 26.91
KRPM10A 1968.08 27.82
KRPM10A 1968.31 26.30
KRPM10A 1968.53 25.96
KRPM10A 1968.75 24.80
KRPM10A 1968.82 24.87
KRPM10A 1968.88 27.79
KRPM10A 1968.95 29.08
KRPM10A 1969.02 28.94
KRPM10A 1969.08 28.95
KRPM10A 1969.22 27.22
KRPM10A 1969.35 26.34
KRPM10A 1969.48 24.62
KRPM10A 1969.62 23.15
KRPM10A 1969.75 22.72
KRPM10A 1969.80 23.43
KRPM10A 1969.85 24.89
KRPM10A 1969.89 25.37
KRPM10A 1969.94 26.82
KRPM10A 1969.99 27.68
KRPM10A 1970.04 27.87
KRPM10A 1970.08 28.25
KRPM10A 1970.19 26.43
KRPM10A 1970.31 25.08
KRPM10A 1970.42 24.79
KRPM10A 1970.53 24.84
214

KRPM10A 1970.64 23.16
KRPM10A 1970.75 22.85
KRPM10A 1970.82 23.42
KRPM10A 1970.88 24.19
KRPM10A 1970.95 25.35
KRPM10A 1971.02 27.32
KRPM10A 1971.08 27.61
KRPM10A 1971.25 26.16
KRPM10A 1971.42 25.12
KRPM10A 1971.58 23.48
KRPM10A 1971.75 23.42
KRPM10A 1971.81 23.56
KRPM10A 1971.86 25.56
KRPM10A 1971.92 26.29
KRPM10A 1971.97 26.62
KRPM10A 1972.03 27.65
KRPM10A 1972.08 28.09
KRPM10A 1972.22 26.10
KRPM10A 1972.35 26.62
KRPM10A 1972.48 25.52
KRPM10A 1972.62 24.28
KRPM10A 1972.75 24.10
KRPM10A 1972.92 25.97
KRPM10A 1973.08 25.54
KRPM10A 1973.31 25.54
KRPM10A 1973.53 24.29
KRPM10A 1973.75 22.15
KRPM10A 1973.86 24.40
KRPM10A 1973.97 24.71
KRPM10A 1974.08 25.75
KRPM10A 1974.42 24.61
KRPM10A 1974.75 22.52
KRPM10A 1974.92 24.70
KRPM10A 1975.08 26.27
KRPM10A 1975.19 26.25
KRPM10A 1975.31 25.22
KRPM10A 1975.42 24.77
KRPM10A 1975.53 24.60
KRPM10A 1975.64 22.38
KRPM10A 1975.75 21.89
KRPM10A 1975.92 25.72
KRPM10A 1976.08 26.73
KRPM10A 1976.22 25.57
KRPM10A 1976.35 26.17
KRPM10A 1976.48 25.26
KRPM10A 1976.62 25.21
KRPM10A 1976.75 24.98
KRPM10A 1976.92 25.53
215

KRPM10A 1977.08 27.73
KRPM10A 1977.22 27.72
KRPM10A 1977.35 27.03
KRPM10A 1977.48 26.00
KRPM10A 1977.62 25.69
KRPM10A 1977.75 25.49
KRPM10A 1977.86 25.58
KRPM10A 1977.97 27.05
KRPM10A 1978.08 27.39
KRPM10A 1978.31 26.25
KRPM10A 1978.53 25.06
KRPM10A 1978.75 24.47
KRPM10A 1978.82 24.73
KRPM10A 1978.88 24.97
KRPM10A 1978.95 24.75
KRPM10A 1979.02 26.15
KRPM10A 1979.08 28.27
KRPM10A 1979.17 28.14
KRPM10A 1979.25 27.34
KRPM10A 1979.33 25.81
KRPM10A 1979.42 25.40
KRPM10A 1979.50 25.39
KRPM10A 1979.58 26.59
KRPM10A 1979.67 24.70
KRPM10A 1979.75 24.59
KRPM10A 1980.08 26.82
KRPM10A 1980.16 25.53
KRPM10A 1980.23 24.41
KRPM10A 1980.31 24.99
KRPM10A 1980.38 25.18
KRPM10A 1980.45 25.22
KRPM10A 1980.53 25.12
KRPM10A 1980.60 25.75
KRPM10A 1980.68 24.14
KRPM10A 1980.75 23.44
KRPM10A 1980.86 26.02
KRPM10A 1980.97 26.05
KRPM10A 1981.08 26.22
KRPM10A 1981.25 26.25
KRPM10A 1981.42 24.99
KRPM10A 1981.58 24.66
KRPM10A 1981.75 24.15
KRPM10A 1981.86 24.54
KRPM10A 1981.97 26.49
KRPM10A 1982.08 27.27
KRPM10A 1982.42 25.88
KRPM10A 1982.75 25.60
KRPM10A 1982.79 25.76
216

KRPM10A 1982.83 25.87
KRPM10A 1982.88 26.69
KRPM10A 1982.92 26.00
KRPM10A 1982.96 26.04
KRPM10A 1983.00 26.04
KRPM10A 1983.04 25.67
KRPM10A 1983.08 26.16
KRPM10A 1983.42 25.63
KRPM10A 1983.75 24.32
KRPM10A 1983.83 25.52
KRPM10A 1983.92 25.19
KRPM10A 1984.00 26.47
KRPM10A 1984.08 27.52
KRPM10A 1984.42 25.30
KRPM10A 1984.75 24.17
KRPM10A 1985.08 26.71
KRPM10A 1985.17 26.30
KRPM10A 1985.25 26.66
KRPM10A 1985.33 26.69
KRPM10A 1985.42 26.21
KRPM10A 1985.50 26.13
KRPM10A 1985.58 25.89
KRPM10A 1985.67 24.01
KRPM10A 1985.75 22.85
KRPM10A 1985.82 23.45
KRPM10A 1985.88 25.74
KRPM10A 1985.95 26.26
KRPM10A 1986.02 25.85
KRPM10A 1985.93 N/A
KRPM10A 1986.00 N/A
KRPM10A 1987.08 27.27
KRPM10A 1987.18 27.19
KRPM10A 1987.27 24.87
KRPM10A 1987.37 24.60
KRPM10A 1987.46 24.81
KRPM10A 1987.56 24.64
KRPM10A 1987.65 23.95
KRPM10A 1987.75 23.87
KRPM10A 1987.83 24.47
KRPM10A 1987.92 25.55
KRPM10A 1988.00 25.54
KRPM10A 1988.08 25.89
KRPM10A 1988.16 25.61
KRPM10A 1988.23 25.68
KRPM10A 1988.31 24.74
KRPM10A 1988.38 24.46
KRPM10A 1988.45 24.79
KRPM10A 1988.53 24.51
217

KRPM10A 1988.60 24.37
KRPM10A 1988.68 22.69
KRPM10A 1988.75 20.93
KRPM10A 1988.81 22.26
KRPM10A 1988.86 24.41
KRPM10A 1988.92 25.92
KRPM10A 1988.97 26.19
KRPM10A 1989.03 26.46
KRPM10A 1989.08 26.96
KRPM10A 1989.14 26.39
KRPM10A 1989.20 25.37
KRPM10A 1989.27 24.74
KRPM10A 1989.33 25.80
KRPM10A 1989.39 25.71
KRPM10A 1989.45 25.23
KRPM10A 1989.51 25.07
KRPM10A 1989.57 25.30
KRPM10A 1989.63 25.23
KRPM10A 1989.69 24.15
KRPM10A 1989.75 23.74
KRPM10A 1989.82 25.58
KRPM10A 1989.88 26.28
KRPM10A 1989.95 26.38
KRPM10A 1990.02 26.71
KRPM10A 1990.08 27.40
KRPM10A 1990.18 26.80
KRPM10A 1990.27 26.74
KRPM10A 1990.37 26.36
KRPM10A 1990.46 26.35
KRPM10A 1990.56 25.80
KRPM10A 1990.65 24.71
KRPM10A 1990.75 24.19
KRPM10A 1990.86 24.82
KRPM10A 1990.97 25.98
KRPM10A 1991.08 27.05
KRPM10A 1991.16 26.68
KRPM10A 1991.23 26.49
KRPM10A 1991.31 25.78
KRPM10A 1991.38 24.87
KRPM10A 1991.45 25.11
KRPM10A 1991.53 25.19
KRPM10A 1991.60 24.85
KRPM10A 1991.68 24.39
KRPM10A 1991.75 23.76
KRPM10A 1991.83 24.01
KRPM10A 1991.92 25.80
KRPM10A 1992.00 28.51
KRPM10A 1992.08 28.73
218

KRPM10A 1992.19 27.91
KRPM10A 1992.31 26.71
KRPM10A 1992.42 27.62
KRPM10A 1992.53 26.46
KRPM10A 1992.64 25.11
KRPM10A 1992.75 24.60
KRPM10A 1992.78 24.92
KRPM10A 1992.81 25.17
KRPM10A 1992.84 26.03
KRPM10A 1992.87 26.42
KRPM10A 1992.90 25.98
KRPM10A 1992.93 25.26
KRPM10A 1992.96 25.46
KRPM10A 1992.99 25.84
KRPM10A 1993.02 26.09
KRPM10A 1993.05 27.91
KRPM10A 1993.08 29.64
KRPM10A 1993.13 28.78
KRPM10A 1993.18 28.48
KRPM10A 1993.23 27.99
KRPM10A 1993.27 26.82
KRPM10A 1993.32 26.74
KRPM10A 1993.37 26.61
KRPM10A 1993.42 26.07
KRPM10A 1993.46 25.61
KRPM10A 1993.51 25.38
KRPM10A 1993.56 25.59
KRPM10A 1993.61 26.29
KRPM10A 1993.65 25.41
KRPM10A 1993.70 24.45
KRPM10A 1993.75 23.23
KRPM10A 1993.86 23.29
KRPM10A 1993.97 25.15
KRPM10A 1994.08 27.10
KRPM10A 1994.14 26.94
KRPM10A 1994.20 26.12
KRPM10A 1994.27 26.17
KRPM10A 1994.33 25.99
KRPM10A 1994.39 25.58
KRPM10A 1994.45 25.31
KRPM10A 1994.51 25.05
KRPM10A 1994.57 25.42
KRPM10A 1994.63 25.18
KRPM10A 1994.69 24.26
KRPM10A 1994.75 23.99
KRPM10A 1994.82 24.90
KRPM10A 1994.88 25.58
KRPM10A 1994.95 27.56
219

KRPM10A 1995.02 29.05
KRPM10A 1995.08 29.36
KRPM10A 1995.14 28.95
KRPM10A 1995.19 28.24
KRPM10A 1995.25 26.90
KRPM10A 1995.31 26.77
KRPM10A 1995.36 25.58
KRPM10A 1995.42 24.59
KRPM10A 1995.47 23.70
KRPM10A 1995.53 23.54
KRPM10A 1995.58 22.80
KRPM10A 1995.64 22.10
KRPM10A 1995.69 21.41
KRPM10A 1995.75 21.35
KRPM10A 1995.81 22.84
KRPM10A 1995.86 25.08
KRPM10A 1995.92 26.92
KRPM10A 1995.97 26.55
KRPM10A 1996.03 26.88
KRPM10A 1996.08 27.18
KRPM10A 1996.14 26.78
KRPM10A 1996.20 25.66
KRPM10A 1996.27 25.00
KRPM10A 1996.33 25.68
KRPM10A 1996.39 25.14
KRPM10A 1996.45 24.66
KRPM10A 1996.51 25.11
KRPM10A 1996.57 25.59
KRPM10A 1996.63 24.98
KRPM10A 1996.69 22.68
KRPM10A 1996.75 21.80
KRPM10A 1996.78 22.79
KRPM10A 1996.81 22.84
KRPM10A 1996.84 22.86
KRPM10A 1996.87 22.94
KRPM10A 1996.90 22.82
KRPM10A 1996.93 24.14
KRPM10A 1996.96 27.24
KRPM10A 1996.99 27.45
KRPM10A 1997.02 27.41
KRPM10A 1997.05 28.52
KRPM10A 1997.08 28.88
KRPM10A 1997.12 28.80
KRPM10A 1997.16 28.62
KRPM10A 1997.19 28.74
KRPM10A 1997.23 28.30
KRPM10A 1997.27 27.85
KRPM10A 1997.31 28.59
220

KRPM10A 1997.34 28.46
KRPM10A 1997.38 26.99
KRPM10A 1997.42 25.19
KRPM10A 1997.45 24.65
KRPM10A 1997.49 25.50
KRPM10A 1997.53 26.42
KRPM10A 1997.56 26.82
KRPM10A 1997.60 26.86
KRPM10A 1997.64 26.43
KRPM10A 1997.68 24.90
KRPM10A 1997.71 24.19
KRPM10A 1997.75 24.00
KRPM10A 1997.81 24.57
KRPM10A 1997.86 24.80
KRPM10A 1997.92 25.67
KRPM10A 1997.97 26.15
KRPM10A 1998.03 26.72
KRPM10A 1998.08 27.79
KRPM10A 1998.13 27.22
KRPM10A 1998.17 26.86
KRPM10A 1998.22 26.62
KRPM10A 1998.26 25.54
KRPM10A 1998.31 25.81
KRPM10A 1998.35 26.64
KRPM10A 1998.39 26.13
KRPM10A 1998.44 24.89
KRPM10A 1998.48 24.24
KRPM10A 1998.53 24.36
KRPM10A 1998.57 24.28
KRPM10A 1998.62 23.81
KRPM10A 1998.66 22.86
KRPM10A 1998.71 21.87
KRPM10A 1998.75 21.26
KRPM10A 1998.83 22.94
KRPM10A 1998.92 24.07
KRPM10A 1999.00 26.11
KRPM10A 1999.08 28.77
KRPM10A 1999.17 28.72
KRPM10A 1999.25 27.53
KRPM10A 1999.33 26.66
KRPM10A 1999.42 26.17
KRPM10A 1999.50 26.20
KRPM10A 1999.58 25.66
KRPM10A 1999.67 24.11
KRPM10A 1999.75 24.02
KRPM10A 1999.77 24.90
KRPM10A 1999.78 26.06
KRPM10A 1999.80 26.92
221

KRPM10A 1999.82 26.25
KRPM10A 1999.83 26.03
KRPM10A 1999.85 26.14
KRPM10A 1999.87 26.29
KRPM10A 1999.88 26.63
KRPM10A 1999.90 27.22
KRPM10A 1999.92 25.64
KRPM10A 1999.93 24.85
KRPM10A 1999.95 25.85
KRPM10A 1999.97 26.09
KRPM10A 1999.98 25.17
KRPM10A 2000.00 24.37
KRPM10A 2000.02 24.00
KRPM10A 2000.03 22.82
KRPM10A 2000.05 22.42
KRPM10A 2000.07 25.27
KRPM10A 2000.08 25.43
KRPM10A 2000.12 25.42
KRPM10A 2000.15 25.83
KRPM10A 2000.19 26.20
KRPM10A 2000.22 26.32
KRPM10A 2000.26 25.61
KRPM10A 2000.29 25.16
KRPM10A 2000.33 25.45
KRPM10A 2000.36 25.91
KRPM10A 2000.40 25.70
KRPM10A 2000.43 25.63
KRPM10A 2000.47 25.71
KRPM10A 2000.50 26.35
KRPM10A 2000.54 26.99
KRPM10A 2000.57 26.30
KRPM10A 2000.61 25.17
KRPM10A 2000.64 25.29
KRPM10A 2000.68 25.89
KRPM10A 2000.71 25.76
KRPM10A 2000.75 24.17
KRPM10A 2000.86 24.53
KRPM10A 2000.97 26.58
KRPM10A 2001.08 27.02
KRPM10A 2001.13 26.66
KRPM10A 2001.19 26.42
KRPM10A 2001.24 26.42
KRPM10A 2001.29 26.65
KRPM10A 2001.34 26.78
KRPM10A 2001.39 27.13
KRPM10A 2001.44 26.98
KRPM10A 2001.49 25.98
KRPM10A 2001.54 26.32
222

KRPM10A 2001.60 26.60
KRPM10A 2001.65 25.86
KRPM10A 2001.70 23.19
KRPM10A 2001.75 23.08
KRPM10A 2001.83 24.33
KRPM10A 2001.92 26.10
KRPM10A 2002.00 27.32
KRPM10A 2002.08 28.00
KRPM10A 2002.12 27.56
KRPM10A 2002.16 27.37
KRPM10A 2002.19 27.31
KRPM10A 2002.23 27.18
KRPM10A 2002.27 26.65
KRPM10A 2002.31 26.50
KRPM10A 2002.34 28.15
KRPM10A 2002.38 27.43
KRPM10A 2002.42 27.98
KRPM10A 2002.45 27.37
KRPM10A 2002.49 26.77
KRPM10A 2002.53 25.70
KRPM10A 2002.56 25.31
KRPM10A 2002.60 25.06
KRPM10A 2002.64 25.44
KRPM10A 2002.68 24.65
KRPM10A 2002.71 24.26
KRPM10A 2002.75 24.18
KRPM10A 2002.78 24.43
KRPM10A 2002.80 25.23
KRPM10A 2002.83 25.76
KRPM10A 2002.85 25.25
KRPM10A 2002.88 25.41
KRPM10A 2002.90 26.19
KRPM10A 2002.93 26.91
KRPM10A 2002.96 26.99
KRPM10A 2002.98 27.06
KRPM10A 2003.01 27.13
KRPM10A 2003.03 27.27
KRPM10A 2003.06 27.22
KRPM10A 2003.08 27.84
KRPM10A 2003.17 27.36
KRPM10A 2003.25 26.11
KRPM10A 2003.33 24.73
KRPM10A 2003.42 23.73
KRPM10A 2003.50 23.96
KRPM10A 2003.58 24.37
KRPM10A 2003.67 24.88
KRPM10A 2003.75 22.99
KRPM10A 2003.78 25.37
223

KRPM10A 2003.81 25.72
KRPM10A 2003.84 25.04
KRPM10A 2003.87 24.77
KRPM10A 2003.90 23.86
KRPM10A 2003.93 23.31
KRPM10A 2003.96 23.12
KRPM10A 2003.99 24.59
KRPM10A 2004.02 26.47
KRPM10A 2004.05 27.97
KRPM10A 2004.08 28.75
KRPM10A 2004.14 28.73
KRPM10A 2004.20 28.11
KRPM10A 2004.27 27.43
KRPM10A 2004.33 27.66
KRPM10A 2004.39 27.22
KRPM10A 2004.45 26.02
KRPM10A 2004.51 25.03
KRPM10A 2004.57 25.52
KRPM10A 2004.63 26.95
KRPM10A 2004.69 26.01
KRPM10A 2004.75 24.04
KRPM10A 2004.78 24.25
KRPM10A 2004.82 25.08
KRPM10A 2004.85 26.04
KRPM10A 2004.88 26.18
KRPM10A 2004.92 26.03
KRPM10A 2004.95 24.34
KRPM10A 2004.98 25.39
KRPM10A 2005.02 26.15
KRPM10A 2005.05 27.59
KRPM10A 2005.08 28.15
KRPM10A 2005.22 27.18
KRPM10A 2005.35 26.46
KRPM10A 2005.48 25.01
KRPM10A 2005.62 24.76
KRPM10A 2005.75 23.99
KRPM10A 2005.86 25.59
KRPM10A 2005.97 25.46
KRPM10A 2006.08 26.37
KRPM15B 1867.08 27.18
KRPM15B 1867.16 26.88
KRPM15B 1867.23 26.13
KRPM15B 1867.31 26.06
KRPM15B 1867.38 25.93
KRPM15B 1867.45 26.09
KRPM15B 1867.53 26.26
KRPM15B 1867.60 25.47
224

KRPM15B 1867.68 24.54
KRPM15B 1867.75 23.70
KRPM15B 1867.77 24.32
KRPM15B 1867.80 24.15
KRPM15B 1867.82 24.84
KRPM15B 1867.85 24.88
KRPM15B 1867.87 24.26
KRPM15B 1867.89 23.96
KRPM15B 1867.92 24.02
KRPM15B 1867.94 24.76
KRPM15B 1867.96 25.88
KRPM15B 1867.99 26.58
KRPM15B 1868.01 28.17
KRPM15B 1868.04 28.97
KRPM15B 1868.06 29.39
KRPM15B 1868.08 29.59
KRPM15B 1868.12 29.14
KRPM15B 1868.15 27.59
KRPM15B 1868.18 26.89
KRPM15B 1868.22 26.21
KRPM15B 1868.25 25.67
KRPM15B 1868.28 25.57
KRPM15B 1868.32 26.06
KRPM15B 1868.35 26.42
KRPM15B 1868.38 26.75
KRPM15B 1868.42 26.46
KRPM15B 1868.45 25.88
KRPM15B 1868.48 25.45
KRPM15B 1868.52 25.36
KRPM15B 1868.55 25.40
KRPM15B 1868.58 25.04
KRPM15B 1868.62 24.69
KRPM15B 1868.65 24.28
KRPM15B 1868.68 23.64
KRPM15B 1868.72 22.71
KRPM15B 1868.75 22.48
KRPM15B 1868.79 22.56
KRPM15B 1868.82 22.62
KRPM15B 1868.86 23.81
KRPM15B 1868.90 24.69
KRPM15B 1868.94 24.78
KRPM15B 1868.97 26.67
KRPM15B 1869.01 28.05
KRPM15B 1869.05 28.51
KRPM15B 1869.08 28.82
KRPM15B 1869.13 28.02
KRPM15B 1869.18 25.09
KRPM15B 1869.23 24.82
225

KRPM15B 1869.27 24.78
KRPM15B 1869.32 24.33
KRPM15B 1869.37 23.82
KRPM15B 1869.42 23.71
KRPM15B 1869.46 23.69
KRPM15B 1869.51 23.46
KRPM15B 1869.56 23.15
KRPM15B 1869.61 22.90
KRPM15B 1869.65 22.70
KRPM15B 1869.70 22.49
KRPM15B 1869.75 22.04
KRPM15B 1869.81 22.27
KRPM15B 1869.86 22.87
KRPM15B 1869.92 24.72
KRPM15B 1869.97 25.33
KRPM15B 1870.03 26.35
KRPM15B 1870.08 27.06
KRPM15B 1870.13 25.35
KRPM15B 1870.18 24.08
KRPM15B 1870.23 24.38
KRPM15B 1870.27 24.11
KRPM15B 1870.32 24.19
KRPM15B 1870.37 24.03
KRPM15B 1870.42 24.28
KRPM15B 1870.46 23.76
KRPM15B 1870.51 23.94
KRPM15B 1870.56 23.47
KRPM15B 1870.61 23.79
KRPM15B 1870.65 23.47
KRPM15B 1870.70 22.40
KRPM15B 1870.75 21.54
KRPM15B 1870.78 21.72
KRPM15B 1870.81 22.61
KRPM15B 1870.83 23.18
KRPM15B 1870.86 23.94
KRPM15B 1870.89 23.96
KRPM15B 1870.92 23.54
KRPM15B 1870.94 23.96
KRPM15B 1870.97 24.61
KRPM15B 1871.00 25.68
KRPM15B 1871.03 27.03
KRPM15B 1871.06 27.49
KRPM15B 1871.08 28.70
KRPM15B 1871.15 24.81
KRPM15B 1871.22 24.78
KRPM15B 1871.28 24.81
KRPM15B 1871.35 25.04
KRPM15B 1871.42 25.29
226

KRPM15B 1871.48 24.64
KRPM15B 1871.55 23.78
KRPM15B 1871.62 23.33
KRPM15B 1871.68 23.22
KRPM15B 1871.75 23.09
KRPM15B 1871.79 23.27
KRPM15B 1871.82 23.24
KRPM15B 1871.86 23.26
KRPM15B 1871.90 24.84
KRPM15B 1871.94 27.07
KRPM15B 1871.97 27.66
KRPM15B 1872.01 27.94
KRPM15B 1872.05 28.53
KRPM15B 1872.08 29.36
KRPM15B 1872.13 29.15
KRPM15B 1872.17 28.65
KRPM15B 1872.21 27.26
KRPM15B 1872.25 25.04
KRPM15B 1872.29 24.44
KRPM15B 1872.33 23.77
KRPM15B 1872.38 24.01
KRPM15B 1872.42 24.62
KRPM15B 1872.46 24.43
KRPM15B 1872.50 24.32
KRPM15B 1872.54 24.18
KRPM15B 1872.58 23.61
KRPM15B 1872.63 22.61
KRPM15B 1872.67 21.92
KRPM15B 1872.71 21.38
KRPM15B 1872.75 20.82
KRPM15B 1872.78 21.68
KRPM15B 1872.81 22.76
KRPM15B 1872.83 23.54
KRPM15B 1872.86 24.02
KRPM15B 1872.89 24.62
KRPM15B 1872.92 24.93
KRPM15B 1872.94 25.18
KRPM15B 1872.97 25.87
KRPM15B 1873.00 26.41
KRPM15B 1873.03 27.15
KRPM15B 1873.06 28.06
KRPM15B 1873.08 28.60
KRPM15B 1873.13 28.59
KRPM15B 1873.17 27.97
KRPM15B 1873.21 26.43
KRPM15B 1873.25 25.66
KRPM15B 1873.29 25.65
KRPM15B 1873.33 26.15
227

KRPM15B 1873.38 26.24
KRPM15B 1873.42 26.36
KRPM15B 1873.46 27.04
KRPM15B 1873.50 26.85
KRPM15B 1873.54 25.88
KRPM15B 1873.58 24.76
KRPM15B 1873.63 24.84
KRPM15B 1873.67 25.59
KRPM15B 1873.71 25.23
KRPM15B 1873.75 23.28
KRPM15B 1873.82 23.31
KRPM15B 1873.88 24.40
KRPM15B 1873.95 24.96
KRPM15B 1874.02 26.81
KRPM15B 1874.08 28.01
KRPM15B 1874.17 25.40
KRPM15B 1874.25 24.95
KRPM15B 1874.33 24.48
KRPM15B 1874.42 23.82
KRPM15B 1874.50 23.28
KRPM15B 1874.58 23.06
KRPM15B 1874.67 23.02
KRPM15B 1874.75 22.82
KRPM15B 1874.80 23.24
KRPM15B 1874.85 23.44
KRPM15B 1874.89 24.34
KRPM15B 1874.94 25.56
KRPM15B 1874.99 26.08
KRPM15B 1875.04 27.14
KRPM15B 1875.08 27.73
KRPM15B 1875.15 25.17
KRPM15B 1875.22 24.90
KRPM15B 1875.28 24.76
KRPM15B 1875.35 24.31
KRPM15B 1875.42 24.02
KRPM15B 1875.48 23.86
KRPM15B 1875.55 23.92
KRPM15B 1875.62 24.08
KRPM15B 1875.68 24.01
KRPM15B 1875.75 23.85
KRPM15B 1875.78 24.16
KRPM15B 1875.81 23.94
KRPM15B 1875.83 23.95
KRPM15B 1875.86 23.97
KRPM15B 1875.89 24.35
KRPM15B 1875.92 24.23
KRPM15B 1875.94 24.88
KRPM15B 1875.97 24.34
228

KRPM15B 1876.00 24.75
KRPM15B 1876.03 26.02
KRPM15B 1876.06 26.95
KRPM15B 1876.08 28.15
KRPM15B 1876.15 26.81
KRPM15B 1876.22 26.38
KRPM15B 1876.28 26.41
KRPM15B 1876.35 25.75
KRPM15B 1876.42 25.27
KRPM15B 1876.48 25.09
KRPM15B 1876.55 25.38
KRPM15B 1876.62 25.02
KRPM15B 1876.68 24.01
KRPM15B 1876.75 23.75
KRPM15B 1876.78 23.77
KRPM15B 1876.82 24.23
KRPM15B 1876.85 24.49
KRPM15B 1876.88 25.01
KRPM15B 1876.92 25.26
KRPM15B 1876.95 25.64
KRPM15B 1876.98 26.11
KRPM15B 1877.02 27.03
KRPM15B 1877.05 28.07
KRPM15B 1877.08 28.19
KRPM15B 1877.22 25.26
KRPM15B 1877.35 25.14
KRPM15B 1877.48 24.45
KRPM15B 1877.62 23.97
KRPM15B 1877.75 23.88
KRPM15B 1877.79 24.34
KRPM15B 1877.83 24.40
KRPM15B 1877.88 24.47
KRPM15B 1877.92 24.50
KRPM15B 1877.96 24.96
KRPM15B 1878.00 25.33
KRPM15B 1878.04 26.42
KRPM15B 1878.08 27.94
KRPM15B 1878.19 23.48
KRPM15B 1878.31 23.59
KRPM15B 1878.42 23.87
KRPM15B 1878.53 23.78
KRPM15B 1878.64 23.57
KRPM15B 1878.75 22.75
KRPM15B 1878.79 23.39
KRPM15B 1878.82 22.99
KRPM15B 1878.86 22.79
KRPM15B 1878.90 23.81
KRPM15B 1878.94 25.07
229

KRPM15B 1878.97 25.72
KRPM15B 1879.01 26.60
KRPM15B 1879.05 27.58
KRPM15B 1879.08 28.23
KRPM15B 1879.12 27.83
KRPM15B 1879.16 26.68
KRPM15B 1879.20 25.79
KRPM15B 1879.24 25.78
KRPM15B 1879.28 25.91
KRPM15B 1879.32 25.55
KRPM15B 1879.36 24.69
KRPM15B 1879.40 24.61
KRPM15B 1879.44 24.81
KRPM15B 1879.48 25.15
KRPM15B 1879.51 25.19
KRPM15B 1879.55 24.57
KRPM15B 1879.59 24.18
KRPM15B 1879.63 23.73
KRPM15B 1879.67 23.72
KRPM15B 1879.71 23.78
KRPM15B 1879.75 22.84
KRPM15B 1879.78 23.18
KRPM15B 1879.81 23.48
KRPM15B 1879.83 24.28
KRPM15B 1879.86 25.29
KRPM15B 1879.89 25.85
KRPM15B 1879.92 26.16
KRPM15B 1879.94 26.21
KRPM15B 1879.97 25.26
KRPM15B 1880.00 24.89
KRPM15B 1880.03 25.13
KRPM15B 1880.06 25.71
KRPM15B 1880.08 26.23
KRPM15B 1880.22 26.21
KRPM15B 1880.35 25.43
KRPM15B 1880.48 24.46
KRPM15B 1880.62 23.81
KRPM15B 1880.75 23.63
KRPM15B 1880.81 23.68
KRPM15B 1880.86 24.67
KRPM15B 1880.92 25.52
KRPM15B 1880.97 26.16
KRPM15B 1881.03 26.80
KRPM15B 1881.08 27.55
KRPM15B 1881.22 27.22
KRPM15B 1881.35 25.37
KRPM15B 1881.48 23.60
KRPM15B 1881.62 22.42
230

KRPM15B 1881.75 22.13
KRPM15B 1881.78 22.53
KRPM15B 1881.82 22.83
KRPM15B 1881.85 23.27
KRPM15B 1881.88 23.10
KRPM15B 1881.92 23.12
KRPM15B 1881.95 23.64
KRPM15B 1881.98 24.83
KRPM15B 1882.02 25.71
KRPM15B 1882.05 26.81
KRPM15B 1882.08 26.91
KRPM15B 1882.15 26.63
KRPM15B 1882.22 25.38
KRPM15B 1882.28 24.22
KRPM15B 1882.35 24.00
KRPM15B 1882.42 23.57
KRPM15B 1882.48 23.64
KRPM15B 1882.55 23.09
KRPM15B 1882.62 22.46
KRPM15B 1882.68 21.83
KRPM15B 1882.75 21.34
KRPM15B 1882.80 21.72
KRPM15B 1882.85 22.72
KRPM15B 1882.89 23.59
KRPM15B 1882.94 24.13
KRPM15B 1882.99 25.07
KRPM15B 1883.04 25.90
KRPM15B 1883.08 26.91
KRPM15B 1883.15 25.21
KRPM15B 1883.22 25.71
KRPM15B 1883.28 25.57
KRPM15B 1883.35 24.30
KRPM15B 1883.42 24.83
KRPM15B 1883.48 25.07
KRPM15B 1883.55 25.56
KRPM15B 1883.62 25.23
KRPM15B 1883.68 24.10
KRPM15B 1883.75 23.66
KRPM15B 1883.82 24.16
KRPM15B 1883.88 24.77
KRPM15B 1883.95 25.83
KRPM15B 1884.02 26.91
KRPM15B 1884.08 27.96
KRPM15B 1884.14 27.76
KRPM15B 1884.20 25.95
KRPM15B 1884.27 25.68
KRPM15B 1884.33 25.53
KRPM15B 1884.39 25.68
231

KRPM15B 1884.45 25.65
KRPM15B 1884.51 25.01
KRPM15B 1884.57 24.82
KRPM15B 1884.63 24.32
KRPM15B 1884.69 23.95
KRPM15B 1884.75 23.76
KRPM15B 1884.82 24.09
KRPM15B 1884.88 24.79
KRPM15B 1884.95 25.84
KRPM15B 1885.02 27.51
KRPM15B 1885.08 28.27
KRPM15B 1885.14 27.83
KRPM15B 1885.20 26.87
KRPM15B 1885.27 25.38
KRPM15B 1885.33 26.09
KRPM15B 1885.39 26.57
KRPM15B 1885.45 26.54
KRPM15B 1885.51 25.84
KRPM15B 1885.57 24.54
KRPM15B 1885.63 23.76
KRPM15B 1885.69 22.95
KRPM15B 1885.75 22.90
KRPM15B 1885.81 23.22
KRPM15B 1885.86 23.79
KRPM15B 1885.92 24.49
KRPM15B 1885.97 25.57
KRPM15B 1886.03 26.51
KRPM15B 1886.08 27.86
KRPM15B 1886.15 27.86
KRPM15B 1886.22 26.32
KRPM15B 1886.28 25.36
KRPM15B 1886.35 25.12
KRPM15B 1886.42 20.66
KRPM15B 1886.48 19.65
KRPM15B 1886.55 19.64
KRPM15B 1886.62 19.64
KRPM15B 1886.68 18.99
KRPM15B 1886.75 18.51
KRPM15B 1886.78 19.28
KRPM15B 1886.81 21.04
KRPM15B 1886.84 22.35
KRPM15B 1886.87 23.29
KRPM15B 1886.90 24.06
KRPM15B 1886.93 24.97
KRPM15B 1886.96 26.02
KRPM15B 1886.99 26.85
KRPM15B 1887.02 27.30
KRPM15B 1887.05 27.57
232

KRPM15B 1887.08 28.11
KRPM15B 1887.13 27.32
KRPM15B 1887.19 26.15
KRPM15B 1887.24 24.75
KRPM15B 1887.29 24.65
KRPM15B 1887.34 24.41
KRPM15B 1887.39 24.20
KRPM15B 1887.44 24.12
KRPM15B 1887.49 24.50
KRPM15B 1887.54 25.13
KRPM15B 1887.60 24.84
KRPM15B 1887.65 23.63
KRPM15B 1887.70 23.18
KRPM15B 1887.75 22.76
KRPM15B 1887.78 22.78
KRPM15B 1887.81 24.18
KRPM15B 1887.83 24.76
KRPM15B 1887.86 24.15
KRPM15B 1887.89 23.39
KRPM15B 1887.92 23.62
KRPM15B 1887.94 24.93
KRPM15B 1887.97 25.47
KRPM15B 1888.00 25.96
KRPM15B 1888.03 26.62
KRPM15B 1888.06 27.31
KRPM15B 1888.08 28.03
KRPM15B 1888.19 27.96
KRPM15B 1888.31 27.04
KRPM15B 1888.42 26.15
KRPM15B 1888.53 25.76
KRPM15B 1888.64 25.18
KRPM15B 1888.75 24.67
KRPM15B 1888.77 24.69
KRPM15B 1888.80 24.92
KRPM15B 1888.82 25.08
KRPM15B 1888.85 25.50
KRPM15B 1888.87 25.88
KRPM15B 1888.89 26.51
KRPM15B 1888.92 26.07
KRPM15B 1888.94 26.15
KRPM15B 1888.96 27.15
KRPM15B 1888.99 27.66
KRPM15B 1889.01 27.77
KRPM15B 1889.04 27.49
KRPM15B 1889.06 27.94
KRPM15B 1889.08 28.26
KRPM15B 1889.13 27.59
KRPM15B 1889.19 26.30
233

KRPM15B 1889.24 24.27
KRPM15B 1889.29 24.63
KRPM15B 1889.34 24.96
KRPM15B 1889.39 25.85
KRPM15B 1889.44 25.94
KRPM15B 1889.49 25.02
KRPM15B 1889.54 24.15
KRPM15B 1889.60 22.95
KRPM15B 1889.65 22.83
KRPM15B 1889.70 22.66
KRPM15B 1889.75 22.48
KRPM15B 1889.77 22.61
KRPM15B 1889.79 22.72
KRPM15B 1889.82 23.04
KRPM15B 1889.84 23.23
KRPM15B 1889.86 23.73
KRPM15B 1889.88 24.13
KRPM15B 1889.91 24.89
KRPM15B 1889.93 25.74
KRPM15B 1889.95 26.53
KRPM15B 1889.97 26.54
KRPM15B 1889.99 26.80
KRPM15B 1890.02 27.39
KRPM15B 1890.04 27.97
KRPM15B 1890.06 27.99
KRPM15B 1890.08 28.21
KRPM15B 1890.12 28.21
KRPM15B 1890.16 28.07
KRPM15B 1890.19 26.96
KRPM15B 1890.23 25.96
KRPM15B 1890.27 25.60
KRPM15B 1890.31 25.43
KRPM15B 1890.34 25.70
KRPM15B 1890.38 26.82
KRPM15B 1890.42 26.57
KRPM15B 1890.45 26.41
KRPM15B 1890.49 26.47
KRPM15B 1890.53 26.07
KRPM15B 1890.56 25.77
KRPM15B 1890.60 25.42
KRPM15B 1890.64 25.29
KRPM15B 1890.68 24.25
KRPM15B 1890.71 24.33
KRPM15B 1890.75 23.40
KRPM15B 1890.82 23.57
KRPM15B 1890.88 24.69
KRPM15B 1890.95 25.50
KRPM15B 1891.02 26.89
234

KRPM15B 1891.08 27.42
KRPM15B 1891.31 27.05
KRPM15B 1891.53 26.84
KRPM15B 1891.75 25.18
KRPM15B 1891.79 26.44
KRPM15B 1891.83 26.31
KRPM15B 1891.88 26.07
KRPM15B 1891.92 25.80
KRPM15B 1891.96 26.49
KRPM15B 1892.00 26.87
KRPM15B 1892.04 27.82
KRPM15B 1892.08 28.50
KRPM15B 1892.13 26.15
KRPM15B 1892.18 25.48
KRPM15B 1892.23 25.15
KRPM15B 1892.27 24.85
KRPM15B 1892.32 25.46
KRPM15B 1892.37 24.61
KRPM15B 1892.42 25.50
KRPM15B 1892.46 25.23
KRPM15B 1892.51 25.23
KRPM15B 1892.56 24.77
KRPM15B 1892.61 24.90
KRPM15B 1892.65 24.22
KRPM15B 1892.70 22.62
KRPM15B 1892.75 22.30
KRPM15B 1892.79 22.55
KRPM15B 1892.83 23.32
KRPM15B 1892.88 23.96
KRPM15B 1892.92 24.24
KRPM15B 1892.96 24.70
KRPM15B 1893.00 24.78
KRPM15B 1893.04 25.58
KRPM15B 1893.08 27.48
KRPM15B 1893.16 26.77
KRPM15B 1893.23 25.15
KRPM15B 1893.31 25.89
KRPM15B 1893.38 25.41
KRPM15B 1893.45 24.96
KRPM15B 1893.53 24.69
KRPM15B 1893.60 25.01
KRPM15B 1893.68 24.16
KRPM15B 1893.75 23.89
KRPM15B 1893.81 25.11
KRPM15B 1893.86 26.42
KRPM15B 1893.92 27.11
KRPM15B 1893.97 27.65
KRPM15B 1894.03 28.16
235

KRPM15B 1894.08 28.25
KRPM15B 1894.18 27.49
KRPM15B 1894.27 26.25
KRPM15B 1894.37 26.37
KRPM15B 1894.46 25.41
KRPM15B 1894.56 24.87
KRPM15B 1894.65 23.74
KRPM15B 1894.75 23.88
KRPM15B 1894.79 23.86
KRPM15B 1894.83 23.88
KRPM15B 1894.88 24.14
KRPM15B 1894.92 24.64
KRPM15B 1894.96 25.92
KRPM15B 1895.00 27.08
KRPM15B 1895.04 28.05
KRPM15B 1895.08 28.43
KRPM15B 1895.31 25.63
KRPM15B 1895.53 24.51
KRPM15B 1895.75 25.14
KRPM15B 1895.81 25.05
KRPM15B 1895.86 24.64
KRPM15B 1895.92 24.96
KRPM15B 1895.97 25.71
KRPM15B 1896.03 26.86
KRPM15B 1896.08 27.81
KRPM15B 1896.18 27.57
KRPM15B 1896.27 26.50
KRPM15B 1896.37 26.26
KRPM15B 1896.46 26.34
KRPM15B 1896.56 26.07
KRPM15B 1896.65 25.33
KRPM15B 1896.75 24.70
KRPM15B 1896.83 25.12
KRPM15B 1896.92 25.53
KRPM15B 1897.00 26.59
KRPM15B 1897.08 28.87
KRPM15B 1897.17 28.58
KRPM15B 1897.25 26.00
KRPM15B 1897.33 25.26
KRPM15B 1897.42 25.56
KRPM15B 1897.50 25.61
KRPM15B 1897.58 24.88
KRPM15B 1897.67 24.15
KRPM15B 1897.75 22.71
KRPM15B 1897.78 23.31
KRPM15B 1897.82 23.35
KRPM15B 1897.85 23.42
KRPM15B 1897.88 24.08
236

KRPM15B 1897.92 24.56
KRPM15B 1897.95 25.78
KRPM15B 1897.98 25.89
KRPM15B 1898.02 26.47
KRPM15B 1898.05 27.30
KRPM15B 1898.08 27.64
KRPM15B 1898.31 26.61
KRPM15B 1898.53 26.04
KRPM15B 1898.75 25.06
KRPM15B 1898.78 22.49
KRPM15B 1898.82 23.34
KRPM15B 1898.85 24.18
KRPM15B 1898.88 24.43
KRPM15B 1898.92 24.61
KRPM15B 1898.95 25.60
KRPM15B 1898.98 27.02
KRPM15B 1899.02 27.41
KRPM15B 1899.05 28.16
KRPM15B 1899.08 28.46
KRPM15B 1899.16 28.12
KRPM15B 1899.23 27.59
KRPM15B 1899.31 27.36
KRPM15B 1899.38 25.93
KRPM15B 1899.45 24.49
KRPM15B 1899.53 24.57
KRPM15B 1899.60 25.43
KRPM15B 1899.68 24.72
KRPM15B 1899.75 25.03
KRPM15B 1899.83 26.73
KRPM15B 1899.92 27.34
KRPM15B 1900.00 27.41
KRPM15B 1900.08 28.20
KRPM15B 1900.31 24.71
KRPM15B 1900.53 24.94
KRPM15B 1900.75 24.59
KRPM15B 1900.82 24.64
KRPM15B 1900.88 25.21
KRPM15B 1900.95 25.62
KRPM15B 1901.02 27.90
KRPM15B 1901.08 28.27
KRPM15B 1901.18 25.98
KRPM15B 1901.27 26.68
KRPM15B 1901.37 27.76
KRPM15B 1901.46 26.28
KRPM15B 1901.56 24.85
KRPM15B 1901.65 23.64
KRPM15B 1901.75 23.80
KRPM15B 1901.78 23.87
237

KRPM15B 1901.82 23.16
KRPM15B 1901.85 23.98
KRPM15B 1901.88 24.54
KRPM15B 1901.92 24.61
KRPM15B 1901.95 25.21
KRPM15B 1901.98 26.37
KRPM15B 1902.02 27.14
KRPM15B 1902.05 27.73
KRPM15B 1902.08 28.52
KRPM15B 1902.15 28.90
KRPM15B 1902.22 28.00
KRPM15B 1902.28 27.44
KRPM15B 1902.35 27.62
KRPM15B 1902.42 29.16
KRPM15B 1902.48 28.54
KRPM15B 1902.55 28.09
KRPM15B 1902.62 26.97
KRPM15B 1902.68 23.69
KRPM15B 1902.75 25.27
KRPM15B 1902.79 25.51
KRPM15B 1902.83 25.66
KRPM15B 1902.88 26.13
KRPM15B 1902.92 26.73
KRPM15B 1902.96 27.12
KRPM15B 1903.00 27.21
KRPM15B 1903.04 27.65
KRPM15B 1903.08 27.43
KRPM15B 1903.42 27.29
KRPM15B 1903.75 23.37
KRPM15B 1903.81 23.32
KRPM15B 1903.86 24.59
KRPM15B 1903.92 25.19
KRPM15B 1903.97 25.51
KRPM15B 1904.03 26.38
KRPM15B 1904.08 27.43
KRPM15B 1904.17 25.28
KRPM15B 1904.25 26.85
KRPM15B 1904.33 26.03
KRPM15B 1904.42 25.69
KRPM15B 1904.50 24.60
KRPM15B 1904.58 23.89
KRPM15B 1904.67 23.62
KRPM15B 1904.75 23.41
KRPM15B 1904.80 23.58
KRPM15B 1904.85 24.06
KRPM15B 1904.89 25.18
KRPM15B 1904.94 26.32
KRPM15B 1904.99 27.20
238

KRPM15B 1905.04 27.51
KRPM15B 1905.08 27.55
KRPM15B 1905.22 26.76
KRPM15B 1905.35 26.53
KRPM15B 1905.48 25.55
KRPM15B 1905.62 24.23
KRPM15B 1905.75 24.78
KRPM15B 1905.86 25.17
KRPM15B 1905.97 26.66
KRPM15B 1906.08 26.90
KRPM15B 1906.22 26.94
KRPM15B 1906.35 27.05
KRPM15B 1906.48 25.93
KRPM15B 1906.62 24.60
KRPM15B 1906.75 25.01
KRPM15B 1906.81 25.63
KRPM15B 1906.86 25.69
KRPM15B 1906.92 25.30
KRPM15B 1906.97 27.06
KRPM15B 1907.03 28.10
KRPM15B 1907.08 28.81
KRPM15B 1907.22 27.32
KRPM15B 1907.35 26.67
KRPM15B 1907.48 26.85
KRPM15B 1907.62 26.18
KRPM15B 1907.75 25.13
KRPM15B 1907.79 24.68
KRPM15B 1907.83 25.35
KRPM15B 1907.88 25.64
KRPM15B 1907.92 25.54
KRPM15B 1907.96 25.96
KRPM15B 1908.00 26.97
KRPM15B 1908.04 27.32
KRPM15B 1908.08 28.87
KRPM15B 1908.19 28.13
KRPM15B 1908.31 26.36
KRPM15B 1908.42 24.91
KRPM15B 1908.53 24.80
KRPM15B 1908.64 24.05
KRPM15B 1908.75 23.69
KRPM15B 1908.78 24.35
KRPM15B 1908.82 25.71
KRPM15B 1908.85 26.29
KRPM15B 1908.88 26.17
KRPM15B 1908.92 27.01
KRPM15B 1908.95 28.05
KRPM15B 1908.98 28.75
KRPM15B 1909.02 28.62
239

KRPM15B 1909.05 29.18
KRPM15B 1909.08 28.84
KRPM15B 1909.12 28.47
KRPM15B 1909.16 27.73
KRPM15B 1909.20 26.81
KRPM15B 1909.24 26.38
KRPM15B 1909.28 26.11
KRPM15B 1909.32 25.78
KRPM15B 1909.36 25.46
KRPM15B 1909.40 25.49
KRPM15B 1909.44 25.81
KRPM15B 1909.48 25.65
KRPM15B 1909.51 24.56
KRPM15B 1909.55 25.20
KRPM15B 1909.59 25.46
KRPM15B 1909.63 25.74
KRPM15B 1909.67 24.19
KRPM15B 1909.71 24.15
KRPM15B 1909.75 23.84
KRPM15B 1909.79 24.62
KRPM15B 1909.82 26.05
KRPM15B 1909.86 26.83
KRPM15B 1909.90 27.40
KRPM15B 1909.94 27.54
KRPM15B 1909.97 27.47
KRPM15B 1910.01 27.94
KRPM15B 1910.05 28.32
KRPM15B 1910.08 28.35
KRPM15B 1910.14 28.29
KRPM15B 1910.19 27.88
KRPM15B 1910.25 26.72
KRPM15B 1910.31 27.59
KRPM15B 1910.36 27.47
KRPM15B 1910.42 27.11
KRPM15B 1910.47 24.96
KRPM15B 1910.53 24.35
KRPM15B 1910.58 24.07
KRPM15B 1910.64 23.84
KRPM15B 1910.69 23.82
KRPM15B 1910.75 22.77
KRPM15B 1910.80 23.19
KRPM15B 1910.85 23.61
KRPM15B 1910.89 24.43
KRPM15B 1910.94 25.23
KRPM15B 1910.99 25.47
KRPM15B 1911.04 26.51
KRPM15B 1911.08 28.10
KRPM15B 1911.31 28.01
240

KRPM15B 1911.53 25.47
KRPM15B 1911.75 25.57
KRPM15B 1911.86 26.21
KRPM15B 1911.97 27.00
KRPM15B 1912.08 28.25
KRPM15B 1912.75 25.52
KRPM15B 1912.86 26.02
KRPM15B 1912.97 26.17
KRPM15B 1913.08 27.47
KRPM15B 1913.42 27.01
KRPM15B 1913.75 24.63
KRPM15B 1913.82 25.54
KRPM15B 1913.88 26.49
KRPM15B 1913.95 27.94
KRPM15B 1914.02 28.63
KRPM15B 1914.08 28.99
KRPM15B 1914.25 26.03
KRPM15B 1914.42 26.02
KRPM15B 1914.58 25.96
KRPM15B 1914.75 24.33
KRPM15B 1914.81 25.74
KRPM15B 1914.86 26.25
KRPM15B 1914.92 26.86
KRPM15B 1914.97 28.08
KRPM15B 1915.03 28.59
KRPM15B 1915.08 29.76
KRPM15B 1915.19 28.65
KRPM15B 1915.31 25.67
KRPM15B 1915.42 26.48
KRPM15B 1915.53 26.62
KRPM15B 1915.64 26.31
KRPM15B 1915.75 23.14
KRPM15B 1915.80 22.90
KRPM15B 1915.85 24.15
KRPM15B 1915.89 23.94
KRPM15B 1915.94 24.41
KRPM15B 1915.99 25.97
KRPM15B 1916.04 27.40
KRPM15B 1916.08 28.87
KRPM15B 1916.13 27.50
KRPM15B 1916.17 26.70
KRPM15B 1916.21 25.84
KRPM15B 1916.25 25.72
KRPM15B 1916.29 25.39
KRPM15B 1916.33 25.40
KRPM15B 1916.38 24.96
KRPM15B 1916.42 24.35
KRPM15B 1916.46 23.96
241

KRPM15B 1916.50 23.70
KRPM15B 1916.54 23.86
KRPM15B 1916.58 23.68
KRPM15B 1916.63 23.28
KRPM15B 1916.67 22.97
KRPM15B 1916.71 23.00
KRPM15B 1916.75 22.84
KRPM15B 1916.82 23.58
KRPM15B 1916.88 24.71
KRPM15B 1916.95 25.67
KRPM15B 1917.02 26.13
KRPM15B 1917.08 26.55
KRPM15B 1917.14 25.86
KRPM15B 1917.19 25.87
KRPM15B 1917.25 25.20
KRPM15B 1917.31 24.10
KRPM15B 1917.36 23.79
KRPM15B 1917.42 23.13
KRPM15B 1917.47 22.75
KRPM15B 1917.53 21.71
KRPM15B 1917.58 21.32
KRPM15B 1917.64 21.06
KRPM15B 1917.69 21.32
KRPM15B 1917.75 20.95
KRPM15B 1917.82 21.75
KRPM15B 1917.88 23.52
KRPM15B 1917.95 24.53
KRPM15B 1918.02 25.61
KRPM15B 1918.08 25.86
KRPM15B 1918.16 25.72
KRPM15B 1918.23 25.39
KRPM15B 1918.31 25.58
KRPM15B 1918.38 25.17
KRPM15B 1918.45 25.04
KRPM15B 1918.53 25.17
KRPM15B 1918.60 25.80
KRPM15B 1918.68 24.89
KRPM15B 1918.75 24.72
KRPM15B 1918.81 24.85
KRPM15B 1918.86 24.87
KRPM15B 1918.92 25.64
KRPM15B 1918.97 25.89
KRPM15B 1919.03 26.47
KRPM15B 1919.08 27.70
KRPM15B 1919.18 25.60
KRPM15B 1919.27 26.08
KRPM15B 1919.37 26.17
KRPM15B 1919.46 25.53
242

KRPM15B 1919.56 24.86
KRPM15B 1919.65 23.92
KRPM15B 1919.75 23.67
KRPM15B 1919.81 24.07
KRPM15B 1919.86 24.22
KRPM15B 1919.92 25.47
KRPM15B 1919.97 26.61
KRPM15B 1920.03 26.85
KRPM15B 1920.08 27.75
KRPM15B 1920.19 27.10
KRPM15B 1920.31 26.87
KRPM15B 1920.42 26.43
KRPM15B 1920.53 25.51
KRPM15B 1920.64 24.67
KRPM15B 1920.75 23.20
KRPM15B 1920.81 23.57
KRPM15B 1920.86 24.39
KRPM15B 1920.92 24.77
KRPM15B 1920.97 25.15
KRPM15B 1921.03 26.80
KRPM15B 1921.08 27.65
KRPM15B 1921.14 24.89
KRPM15B 1921.20 24.77
KRPM15B 1921.27 24.70
KRPM15B 1921.33 24.93
KRPM15B 1921.39 25.35
KRPM15B 1921.45 25.11
KRPM15B 1921.51 25.14
KRPM15B 1921.57 24.77
KRPM15B 1921.63 24.26
KRPM15B 1921.69 23.99
KRPM15B 1921.75 23.60
KRPM15B 1921.82 23.90
KRPM15B 1921.88 24.46
KRPM15B 1921.95 25.52
KRPM15B 1922.02 26.85
KRPM15B 1922.08 27.20
KRPM15B 1922.16 26.54
KRPM15B 1922.23 25.99
KRPM15B 1922.31 26.22
KRPM15B 1922.38 26.16
KRPM15B 1922.45 26.12
KRPM15B 1922.53 25.01
KRPM15B 1922.60 22.97
KRPM15B 1922.68 22.14
KRPM15B 1922.75 21.49
KRPM15B 1922.81 21.77
KRPM15B 1922.86 22.04
243

KRPM15B 1922.92 23.18
KRPM15B 1922.97 24.00
KRPM15B 1923.03 24.95
KRPM15B 1923.08 25.68
KRPM15B 1923.16 25.24
KRPM15B 1923.23 25.06
KRPM15B 1923.31 24.81
KRPM15B 1923.38 24.76
KRPM15B 1923.45 24.87
KRPM15B 1923.53 25.61
KRPM15B 1923.60 24.63
KRPM15B 1923.68 23.26
KRPM15B 1923.75 23.20
KRPM15B 1923.82 24.26
KRPM15B 1923.88 24.48
KRPM15B 1923.95 25.38
KRPM15B 1924.02 26.22
KRPM15B 1924.08 26.60
KRPM15B 1924.22 24.58
KRPM15B 1924.35 24.06
KRPM15B 1924.48 24.06
KRPM15B 1924.62 23.28
KRPM15B 1924.75 22.57
KRPM15B 1924.80 22.69
KRPM15B 1924.85 22.69
KRPM15B 1924.89 23.20
KRPM15B 1924.94 25.15
KRPM15B 1924.99 26.75
KRPM15B 1925.04 26.69
KRPM15B 1925.08 27.98
KRPM15B 1925.19 25.40
KRPM15B 1925.31 25.74
KRPM15B 1925.42 25.27
KRPM15B 1925.53 25.14
KRPM15B 1925.64 25.20
KRPM15B 1925.75 24.55
KRPM15B 1925.81 24.69
KRPM15B 1925.86 25.42
KRPM15B 1925.92 26.87
KRPM15B 1925.97 27.02
KRPM15B 1926.03 27.30
KRPM15B 1926.08 28.89
KRPM15B 1926.18 28.23
KRPM15B 1926.27 25.78
KRPM15B 1926.37 25.37
KRPM15B 1926.46 24.77
KRPM15B 1926.56 23.75
KRPM15B 1926.65 22.98
244

KRPM15B 1926.75 22.35
KRPM15B 1926.79 22.98
KRPM15B 1926.82 24.01
KRPM15B 1926.86 23.98
KRPM15B 1926.90 23.36
KRPM15B 1926.94 23.74
KRPM15B 1926.97 25.62
KRPM15B 1927.01 26.76
KRPM15B 1927.05 27.60
KRPM15B 1927.08 27.86
KRPM15B 1927.16 27.32
KRPM15B 1927.23 26.48
KRPM15B 1927.31 26.29
KRPM15B 1927.38 26.55
KRPM15B 1927.45 26.06
KRPM15B 1927.53 25.60
KRPM15B 1927.60 24.76
KRPM15B 1927.68 24.08
KRPM15B 1927.75 23.95
KRPM15B 1927.82 24.57
KRPM15B 1927.88 25.17
KRPM15B 1927.95 25.43
KRPM15B 1928.02 26.07
KRPM15B 1928.08 26.81
KRPM15B 1928.17 26.75
KRPM15B 1928.25 26.69
KRPM15B 1928.33 25.67
KRPM15B 1928.42 25.92
KRPM15B 1928.50 25.52
KRPM15B 1928.58 25.01
KRPM15B 1928.67 24.04
KRPM15B 1928.75 23.84
KRPM15B 1928.83 24.55
KRPM15B 1928.92 25.64
KRPM15B 1929.00 27.20
KRPM15B 1929.08 28.66
KRPM15B 1929.15 27.73
KRPM15B 1929.22 25.85
KRPM15B 1929.28 25.94
KRPM15B 1929.35 25.86
KRPM15B 1929.42 26.22
KRPM15B 1929.48 25.90
KRPM15B 1929.55 25.26
KRPM15B 1929.62 24.50
KRPM15B 1929.68 24.03
KRPM15B 1929.75 23.06
KRPM15B 1929.82 24.29
KRPM15B 1929.88 25.27
245

KRPM15B 1929.95 26.19
KRPM15B 1930.02 26.88
KRPM15B 1930.08 27.59
KRPM15B 1930.17 26.84
KRPM15B 1930.25 26.14
KRPM15B 1930.33 25.99
KRPM15B 1930.42 25.91
KRPM15B 1930.50 26.33
KRPM15B 1930.58 25.69
KRPM15B 1930.67 24.53
KRPM15B 1930.75 23.59
KRPM15B 1930.79 23.98
KRPM15B 1930.83 24.54
KRPM15B 1930.88 24.77
KRPM15B 1930.92 25.09
KRPM15B 1930.96 25.13
KRPM15B 1931.00 25.89
KRPM15B 1931.04 26.21
KRPM15B 1931.08 26.80
KRPM15B 1931.17 26.44
KRPM15B 1931.25 25.22
KRPM15B 1931.33 24.88
KRPM15B 1931.42 24.78
KRPM15B 1931.50 24.85
KRPM15B 1931.58 24.23
KRPM15B 1931.67 22.32
KRPM15B 1931.75 21.52
KRPM15B 1931.82 22.22
KRPM15B 1931.88 23.67
KRPM15B 1931.95 25.42
KRPM15B 1932.02 25.68
KRPM15B 1932.08 27.13
KRPM15B 1932.22 24.81
KRPM15B 1932.35 23.39
KRPM15B 1932.48 22.41
KRPM15B 1932.62 22.60
KRPM15B 1932.75 22.37
KRPM15B 1932.82 22.99
KRPM15B 1932.88 24.61
KRPM15B 1932.95 25.64
KRPM15B 1933.02 26.73
KRPM15B 1933.08 26.95
KRPM15B 1933.16 26.94
KRPM15B 1933.23 25.46
KRPM15B 1933.31 25.55
KRPM15B 1933.38 25.53
KRPM15B 1933.45 25.40
KRPM15B 1933.53 24.15
246

KRPM15B 1933.60 23.31
KRPM15B 1933.68 22.77
KRPM15B 1933.75 22.59
KRPM15B 1933.86 23.69
KRPM15B 1933.97 25.31
KRPM15B 1934.08 26.59
KRPM15B 1934.16 25.47
KRPM15B 1934.23 25.26
KRPM15B 1934.31 25.09
KRPM15B 1934.38 25.02
KRPM15B 1934.45 25.00
KRPM15B 1934.53 25.00
KRPM15B 1934.60 25.06
KRPM15B 1934.68 25.03
KRPM15B 1934.75 24.76
KRPM15B 1934.86 25.12
KRPM15B 1934.97 25.78
KRPM15B 1935.08 27.28
KRPM15B 1935.19 27.10
KRPM15B 1935.31 26.92
KRPM15B 1935.42 25.94
KRPM15B 1935.53 24.83
KRPM15B 1935.64 24.07
KRPM15B 1935.75 23.46
KRPM15B 1935.80 24.20
KRPM15B 1935.85 24.66
KRPM15B 1935.89 24.15
KRPM15B 1935.94 23.57
KRPM15B 1935.99 23.73
KRPM15B 1936.04 25.26
KRPM15B 1936.08 26.27
KRPM15B 1936.16 26.02
KRPM15B 1936.23 25.68
KRPM15B 1936.31 25.47
KRPM15B 1936.38 25.99
KRPM15B 1936.45 26.32
KRPM15B 1936.53 26.18
KRPM15B 1936.60 26.29
KRPM15B 1936.68 25.08
KRPM15B 1936.75 24.74
KRPM15B 1936.86 26.17
KRPM15B 1936.97 27.00
KRPM15B 1937.08 27.60
KRPM15B 1937.31 26.80
KRPM15B 1937.53 23.48
KRPM15B 1937.75 22.95
KRPM15B 1937.82 23.38
KRPM15B 1937.88 24.01
247

KRPM15B 1937.95 24.99
KRPM15B 1938.02 25.95
KRPM15B 1938.08 26.51
KRPM15B 1938.19 25.52
KRPM15B 1938.31 26.00
KRPM15B 1938.42 25.39
KRPM15B 1938.53 24.60
KRPM15B 1938.64 24.01
KRPM15B 1938.75 23.64
KRPM15B 1938.81 24.15
KRPM15B 1938.86 25.41
KRPM15B 1938.92 26.27
KRPM15B 1938.97 27.66
KRPM15B 1939.03 27.62
KRPM15B 1939.08 27.69
KRPM15B 1939.16 27.47
KRPM15B 1939.23 27.46
KRPM15B 1939.31 27.58
KRPM15B 1939.38 26.52
KRPM15B 1939.45 24.93
KRPM15B 1939.53 24.07
KRPM15B 1939.60 23.44
KRPM15B 1939.68 23.57
KRPM15B 1939.75 23.32
KRPM15B 1939.83 23.55
KRPM15B 1939.92 23.89
KRPM15B 1940.00 25.77
KRPM15B 1940.08 27.48
KRPM15B 1940.19 26.32
KRPM15B 1940.31 25.30
KRPM15B 1940.42 26.11
KRPM15B 1940.53 26.08
KRPM15B 1940.64 25.44
KRPM15B 1940.75 24.86
KRPM15B 1940.82 25.38
KRPM15B 1940.88 25.32
KRPM15B 1940.95 25.94
KRPM15B 1941.02 26.39
KRPM15B 1941.08 27.61
KRPM15B 1941.17 26.52
KRPM15B 1941.25 27.12
KRPM15B 1941.33 27.17
KRPM15B 1941.42 26.24
KRPM15B 1941.50 25.67
KRPM15B 1941.58 24.76
KRPM15B 1941.67 23.76
KRPM15B 1941.75 22.89
KRPM15B 1941.82 23.87
248

KRPM15B 1941.88 24.41
KRPM15B 1941.95 25.06
KRPM15B 1942.02 26.38
KRPM15B 1942.08 28.30
KRPM15B 1942.12 28.05
KRPM15B 1942.16 26.96
KRPM15B 1942.20 24.56
KRPM15B 1942.24 24.73
KRPM15B 1942.28 25.23
KRPM15B 1942.32 24.93
KRPM15B 1942.36 24.95
KRPM15B 1942.40 25.84
KRPM15B 1942.44 25.30
KRPM15B 1942.48 24.61
KRPM15B 1942.51 23.91
KRPM15B 1942.55 24.26
KRPM15B 1942.59 24.34
KRPM15B 1942.63 24.37
KRPM15B 1942.67 23.90
KRPM15B 1942.71 23.45
KRPM15B 1942.75 23.44
KRPM15B 1942.79 24.19
KRPM15B 1942.82 24.46
KRPM15B 1942.86 24.87
KRPM15B 1942.90 25.24
KRPM15B 1942.94 26.29
KRPM15B 1942.97 27.26
KRPM15B 1943.01 27.11
KRPM15B 1943.05 27.59
KRPM15B 1943.08 27.77
KRPM15B 1943.17 26.90
KRPM15B 1943.25 24.93
KRPM15B 1943.33 23.95
KRPM15B 1943.42 24.46
KRPM15B 1943.50 25.01
KRPM15B 1943.58 24.94
KRPM15B 1943.67 23.93
KRPM15B 1943.75 23.63
KRPM15B 1943.83 24.79
KRPM15B 1943.92 26.26
KRPM15B 1944.00 27.03
KRPM15B 1944.08 27.43
KRPM15B 1944.18 26.10
KRPM15B 1944.27 25.38
KRPM15B 1944.37 25.41
KRPM15B 1944.46 25.00
KRPM15B 1944.56 24.38
KRPM15B 1944.65 23.80
249

KRPM15B 1944.75 23.50
KRPM15B 1944.80 24.16
KRPM15B 1944.85 24.08
KRPM15B 1944.89 24.57
KRPM15B 1944.94 25.15
KRPM15B 1944.99 26.03
KRPM15B 1945.04 26.60
KRPM15B 1945.08 26.75
KRPM15B 1945.13 25.61
KRPM15B 1945.18 25.76
KRPM15B 1945.23 25.81
KRPM15B 1945.27 26.09
KRPM15B 1945.32 25.88
KRPM15B 1945.37 25.68
KRPM15B 1945.42 25.11
KRPM15B 1945.46 24.75
KRPM15B 1945.51 24.18
KRPM15B 1945.56 24.47
KRPM15B 1945.61 25.38
KRPM15B 1945.65 26.07
KRPM15B 1945.70 24.67
KRPM15B 1945.75 24.43
KRPM15B 1946.08 27.21
KRPM15B 1946.18 26.29
KRPM15B 1946.27 25.45
KRPM15B 1946.37 24.88
KRPM15B 1946.46 25.03
KRPM15B 1946.56 24.82
KRPM15B 1946.65 24.19
KRPM15B 1946.75 22.92
KRPM15B 1946.81 23.42
KRPM15B 1946.86 24.23
KRPM15B 1946.92 24.47
KRPM15B 1946.97 25.25
KRPM15B 1947.03 26.10
KRPM15B 1947.08 27.00
KRPM15B 1947.25 26.24
KRPM15B 1947.42 24.79
KRPM15B 1947.58 23.27
KRPM15B 1947.75 22.72
KRPM15B 1947.82 23.51
KRPM15B 1947.88 24.88
KRPM15B 1947.95 25.60
KRPM15B 1948.02 26.26
KRPM15B 1948.08 27.45
KRPM15B 1948.18 26.62
KRPM15B 1948.27 25.03
KRPM15B 1948.37 24.96
250

KRPM15B 1948.46 25.54
KRPM15B 1948.56 25.27
KRPM15B 1948.65 24.50
KRPM15B 1948.75 23.10
KRPM15B 1948.82 23.81
KRPM15B 1948.88 24.17
KRPM15B 1948.95 25.99
KRPM15B 1949.02 26.25
KRPM15B 1949.08 27.33
KRPM15B 1949.18 25.31
KRPM15B 1949.27 25.02
KRPM15B 1949.37 24.40
KRPM15B 1949.46 23.77
KRPM15B 1949.56 23.60
KRPM15B 1949.65 23.09
KRPM15B 1949.75 22.74
KRPM15B 1949.83 24.19
KRPM15B 1949.92 25.66
KRPM15B 1950.00 26.96
KRPM15B 1950.08 27.39
KRPM15B 1950.14 26.17
KRPM15B 1950.20 26.19
KRPM15B 1950.27 26.02
KRPM15B 1950.33 25.45
KRPM15B 1950.39 24.54
KRPM15B 1950.45 24.00
KRPM15B 1950.51 24.24
KRPM15B 1950.57 24.54
KRPM15B 1950.63 24.64
KRPM15B 1950.69 23.55
KRPM15B 1950.75 23.54
KRPM15B 1950.83 24.50
KRPM15B 1950.92 25.74
KRPM15B 1951.00 26.89
KRPM15B 1951.08 27.92
KRPM15B 1951.14 26.37
KRPM15B 1951.20 26.34
KRPM15B 1951.27 25.25
KRPM15B 1951.33 24.06
KRPM15B 1951.39 24.66
KRPM15B 1951.45 25.71
KRPM15B 1951.51 26.26
KRPM15B 1951.57 25.92
KRPM15B 1951.63 24.61
KRPM15B 1951.69 23.38
KRPM15B 1951.75 22.41
KRPM15B 1951.78 23.11
KRPM15B 1951.82 23.24
251

KRPM15B 1951.85 23.58
KRPM15B 1951.88 23.26
KRPM15B 1951.92 23.33
KRPM15B 1951.95 24.02
KRPM15B 1951.98 25.33
KRPM15B 1952.02 26.39
KRPM15B 1952.05 26.90
KRPM15B 1952.08 27.50
KRPM15B 1952.14 27.01
KRPM15B 1952.19 26.20
KRPM15B 1952.25 26.56
KRPM15B 1952.31 26.34
KRPM15B 1952.36 25.93
KRPM15B 1952.42 25.71
KRPM15B 1952.47 25.40
KRPM15B 1952.53 25.45
KRPM15B 1952.58 25.30
KRPM15B 1952.64 25.94
KRPM15B 1952.69 23.25
KRPM15B 1952.75 22.67
KRPM15B 1952.83 23.63
KRPM15B 1952.92 25.08
KRPM15B 1953.00 26.36
KRPM15B 1953.08 26.98
KRPM15B 1953.17 26.11
KRPM15B 1953.25 25.04
KRPM15B 1953.33 25.56
KRPM15B 1953.42 25.92
KRPM15B 1953.50 24.96
KRPM15B 1953.58 24.12
KRPM15B 1953.67 23.93
KRPM15B 1953.75 23.76
KRPM15B 1953.92 24.68
KRPM15B 1954.08 25.70
KRPM15B 1954.17 24.01
KRPM15B 1954.25 23.55
KRPM15B 1954.33 24.23
KRPM15B 1954.42 25.15
KRPM15B 1954.50 25.31
KRPM15B 1954.58 24.14
KRPM15B 1954.67 23.20
KRPM15B 1954.75 22.62
KRPM15B 1954.92 24.57
KRPM15B 1955.08 26.48
KRPM15B 1955.19 26.10
KRPM15B 1955.31 25.72
KRPM15B 1955.42 24.93
KRPM15B 1955.53 24.77
252

KRPM15B 1955.64 24.00
KRPM15B 1955.75 22.83
KRPM15B 1955.82 23.10
KRPM15B 1955.88 24.52
KRPM15B 1955.95 25.29
KRPM15B 1956.02 25.50
KRPM15B 1956.08 25.60
KRPM15B 1956.25 25.26
KRPM15B 1956.42 25.09
KRPM15B 1956.58 23.57
KRPM15B 1956.75 22.45
KRPM15B 1956.86 23.51
KRPM15B 1956.97 24.86
KRPM15B 1957.08 26.41
KRPM15B 1957.16 26.11
KRPM15B 1957.23 24.58
KRPM15B 1957.31 23.83
KRPM15B 1957.38 23.82
KRPM15B 1957.45 23.93
KRPM15B 1957.53 23.68
KRPM15B 1957.60 23.74
KRPM15B 1957.68 24.09
KRPM15B 1957.75 22.83
KRPM15B 1957.86 23.44
KRPM15B 1957.97 24.84
KRPM15B 1958.08 26.03
KRPM15B 1958.22 23.72
KRPM15B 1958.35 22.91
KRPM15B 1958.48 24.99
KRPM15B 1958.62 24.59
KRPM15B 1958.75 22.69
KRPM15B 1958.92 23.79
KRPM15B 1959.08 25.73
KRPM15B 1959.25 24.13
KRPM15B 1959.42 24.53
KRPM15B 1959.58 24.31
KRPM15B 1959.75 23.23
KRPM15B 1959.83 23.66
KRPM15B 1959.92 24.95
KRPM15B 1960.00 26.03
KRPM15B 1960.08 26.69
KRPM15B 1960.16 26.41
KRPM15B 1960.23 24.02
KRPM15B 1960.31 24.00
KRPM15B 1960.38 24.60
KRPM15B 1960.45 25.43
KRPM15B 1960.53 26.20
KRPM15B 1960.60 25.90
253

KRPM15B 1960.68 24.88
KRPM15B 1960.75 23.13
KRPM15B 1960.81 23.35
KRPM15B 1960.86 24.16
KRPM15B 1960.92 24.67
KRPM15B 1960.97 24.29
KRPM15B 1961.03 24.67
KRPM15B 1961.08 26.18
KRPM15B 1961.15 25.91
KRPM15B 1961.22 25.90
KRPM15B 1961.28 25.25
KRPM15B 1961.35 24.89
KRPM15B 1961.42 24.62
KRPM15B 1961.48 24.62
KRPM15B 1961.55 25.70
KRPM15B 1961.62 24.47
KRPM15B 1961.68 23.69
KRPM15B 1961.75 22.99
KRPM15B 1961.83 23.76
KRPM15B 1961.92 24.57
KRPM15B 1962.00 25.75
KRPM15B 1962.08 26.36
KRPM15B 1962.17 26.12
KRPM15B 1962.25 25.35
KRPM15B 1962.33 24.51
KRPM15B 1962.42 23.52
KRPM15B 1962.50 22.56
KRPM15B 1962.58 22.87
KRPM15B 1962.67 23.03
KRPM15B 1962.75 22.11
KRPM15B 1962.83 24.26
KRPM15B 1962.92 26.08
KRPM15B 1963.00 27.11
KRPM15B 1963.08 28.35
KRPM15B 1963.25 26.98
KRPM15B 1963.42 25.54
KRPM15B 1963.58 24.20
KRPM15B 1963.75 23.75
KRPM15B 1963.83 24.27
KRPM15B 1963.92 25.05
KRPM15B 1964.00 25.44
KRPM15B 1964.08 27.08
KRPM15B 1964.19 25.82
KRPM15B 1964.31 24.53
KRPM15B 1964.42 24.13
KRPM15B 1964.53 23.57
KRPM15B 1964.64 23.48
KRPM15B 1964.75 23.09
254

KRPM15B 1964.83 23.63
KRPM15B 1964.92 25.79
KRPM15B 1965.00 26.58
KRPM15B 1965.08 26.65
KRPM15B 1965.22 24.69
KRPM15B 1965.35 24.72
KRPM15B 1965.48 24.49
KRPM15B 1965.62 23.36
KRPM15B 1965.75 22.40
KRPM15B 1965.92 23.48
KRPM15B 1966.08 25.52
KRPM15B 1966.18 25.19
KRPM15B 1966.27 25.00
KRPM15B 1966.37 25.41
KRPM15B 1966.46 24.41
KRPM15B 1966.56 24.49
KRPM15B 1966.65 23.92
KRPM15B 1966.75 23.48
KRPM15B 1966.80 24.59
KRPM15B 1966.85 25.29
KRPM15B 1966.89 24.85
KRPM15B 1966.94 24.61
KRPM15B 1966.99 24.84
KRPM15B 1967.04 25.66
KRPM15B 1967.08 26.44
KRPM15B 1967.42 25.55
KRPM15B 1967.75 23.52
KRPM15B 1967.82 23.87
KRPM15B 1967.88 25.27
KRPM15B 1967.95 26.00
KRPM15B 1968.02 26.35
KRPM15B 1968.08 27.34
KRPM15B 1968.18 26.45
KRPM15B 1968.27 25.14
KRPM15B 1968.37 25.41
KRPM15B 1968.46 26.32
KRPM15B 1968.56 25.76
KRPM15B 1968.65 23.63
KRPM15B 1968.75 23.50
KRPM15B 1968.80 23.54
KRPM15B 1968.85 24.63
KRPM15B 1968.89 25.80
KRPM15B 1968.94 26.70
KRPM15B 1968.99 27.17
KRPM15B 1969.04 27.57
KRPM15B 1969.08 28.19
KRPM15B 1969.18 27.93
KRPM15B 1969.27 25.72
255

KRPM15B 1969.37 23.16
KRPM15B 1969.46 22.49
KRPM15B 1969.56 23.50
KRPM15B 1969.65 23.33
KRPM15B 1969.75 22.45
KRPM15B 1969.80 22.84
KRPM15B 1969.85 23.39
KRPM15B 1969.89 24.18
KRPM15B 1969.94 25.09
KRPM15B 1969.99 26.04
KRPM15B 1970.04 26.39
KRPM15B 1970.08 26.82
KRPM15B 1970.15 26.47
KRPM15B 1970.22 25.95
KRPM15B 1970.28 25.37
KRPM15B 1970.35 24.46
KRPM15B 1970.42 24.91
KRPM15B 1970.48 25.00
KRPM15B 1970.55 24.54
KRPM15B 1970.62 23.56
KRPM15B 1970.68 22.81
KRPM15B 1970.75 22.47
KRPM15B 1970.79 22.56
KRPM15B 1970.82 22.67
KRPM15B 1970.86 23.21
KRPM15B 1970.90 23.75
KRPM15B 1970.94 24.07
KRPM15B 1970.97 25.41
KRPM15B 1971.01 27.12
KRPM15B 1971.05 27.30
KRPM15B 1971.08 27.62
KRPM15B 1971.16 26.90
KRPM15B 1971.23 26.94
KRPM15B 1971.31 26.27
KRPM15B 1971.38 24.64
KRPM15B 1971.45 24.39
KRPM15B 1971.53 24.85
KRPM15B 1971.60 23.81
KRPM15B 1971.68 23.15
KRPM15B 1971.75 22.59
KRPM15B 1971.81 23.28
KRPM15B 1971.86 24.92
KRPM15B 1971.92 25.50
KRPM15B 1971.97 25.97
KRPM15B 1972.03 27.31
KRPM15B 1972.08 27.44
KRPM15B 1972.15 27.02
KRPM15B 1972.22 26.47
256

KRPM15B 1972.28 26.08
KRPM15B 1972.35 25.97
KRPM15B 1972.42 26.20
KRPM15B 1972.48 26.15
KRPM15B 1972.55 26.67
KRPM15B 1972.62 26.59
KRPM15B 1972.68 24.98
KRPM15B 1972.75 23.95
KRPM15B 1972.80 24.17
KRPM15B 1972.85 24.58
KRPM15B 1972.89 25.18
KRPM15B 1972.94 24.28
KRPM15B 1972.99 24.69
KRPM15B 1973.04 26.37
KRPM15B 1973.08 27.40
KRPM15B 1973.19 26.36
KRPM15B 1973.31 25.32
KRPM15B 1973.42 25.47
KRPM15B 1973.53 24.41
KRPM15B 1973.64 22.83
KRPM15B 1973.75 21.71
KRPM15B 1973.78 22.13
KRPM15B 1973.82 23.22
KRPM15B 1973.85 24.03
KRPM15B 1973.88 25.42
KRPM15B 1973.92 26.40
KRPM15B 1973.95 26.15
KRPM15B 1973.98 25.42
KRPM15B 1974.02 24.79
KRPM15B 1974.05 25.78
KRPM15B 1974.08 26.77
KRPM15B 1974.31 25.99
KRPM15B 1974.53 23.28
KRPM15B 1974.75 21.96
KRPM15B 1974.82 22.18
KRPM15B 1974.88 22.87
KRPM15B 1974.95 24.35
KRPM15B 1975.02 26.03
KRPM15B 1975.08 26.21
KRPM15B 1975.22 25.93
KRPM15B 1975.35 25.65
KRPM15B 1975.48 25.05
KRPM15B 1975.62 24.60
KRPM15B 1975.75 22.44
KRPM15B 1975.83 22.53
KRPM15B 1975.92 26.22
KRPM15B 1976.00 26.78
KRPM15B 1976.08 27.07
257

KRPM15B 1976.19 26.78
KRPM15B 1976.31 26.23
KRPM15B 1976.42 25.21
KRPM15B 1976.53 24.88
KRPM15B 1976.64 24.84
KRPM15B 1976.75 24.50
KRPM15B 1976.92 26.24
KRPM15B 1977.08 26.78
KRPM15B 1977.42 26.61
KRPM15B 1977.75 26.34
KRPM15B 1977.83 26.51
KRPM15B 1977.92 26.74
KRPM15B 1978.00 27.64
KRPM15B 1978.08 27.67
KRPM15B 1978.18 27.42
KRPM15B 1978.27 26.03
KRPM15B 1978.37 25.30
KRPM15B 1978.46 24.77
KRPM15B 1978.56 24.71
KRPM15B 1978.65 24.72
KRPM15B 1978.75 24.61
KRPM15B 1978.82 25.24
KRPM15B 1978.88 25.29
KRPM15B 1978.95 26.96
KRPM15B 1979.02 27.03
KRPM15B 1979.08 27.11
KRPM15B 1979.31 26.34
KRPM15B 1979.53 25.78
KRPM15B 1979.75 24.82
KRPM15B 1979.83 24.94
KRPM15B 1979.92 25.97
KRPM15B 1980.00 26.33
KRPM15B 1980.08 27.36
KRPM15B 1980.18 26.45
KRPM15B 1980.27 25.82
KRPM15B 1980.37 25.35
KRPM15B 1980.46 26.21
KRPM15B 1980.56 25.84
KRPM15B 1980.65 25.14
KRPM15B 1980.75 24.23
KRPM15B 1980.86 24.55
KRPM15B 1980.97 26.12
KRPM15B 1981.08 27.71
KRPM15B 1981.19 25.82
KRPM15B 1981.31 25.27
KRPM15B 1981.42 25.39
KRPM15B 1981.53 24.83
KRPM15B 1981.64 24.15
258

KRPM15B 1981.75 23.97
KRPM15B 1981.86 24.66
KRPM15B 1981.97 26.52
KRPM15B 1982.08 27.51
KRPM15B 1982.17 26.30
KRPM15B 1982.25 26.04
KRPM15B 1982.33 25.91
KRPM15B 1982.42 26.21
KRPM15B 1982.50 26.15
KRPM15B 1982.58 25.95
KRPM15B 1982.67 25.77
KRPM15B 1982.75 25.58
KRPM15B 1982.86 25.76
KRPM15B 1982.97 26.94
KRPM15B 1983.08 28.65
KRPM15B 1983.31 26.89
KRPM15B 1983.53 23.97
KRPM15B 1983.75 23.49
KRPM15B 1983.82 23.60
KRPM15B 1983.88 24.13
KRPM15B 1983.95 25.60
KRPM15B 1984.02 26.99
KRPM15B 1984.08 27.09
KRPM15B 1984.19 27.08
KRPM15B 1984.31 26.80
KRPM15B 1984.42 26.58
KRPM15B 1984.53 25.75
KRPM15B 1984.64 24.50
KRPM15B 1984.75 23.95
KRPM15B 1984.82 24.62
KRPM15B 1984.88 25.63
KRPM15B 1984.95 26.57
KRPM15B 1985.02 27.41
KRPM15B 1985.08 28.04
KRPM15B 1985.22 27.26
KRPM15B 1985.35 26.37
KRPM15B 1985.48 24.89
KRPM15B 1985.62 23.45
KRPM15B 1985.75 22.74
KRPM15B 1985.80 23.36
KRPM15B 1985.85 23.79
KRPM15B 1985.89 24.30
KRPM15B 1985.94 24.66
KRPM15B 1985.99 25.33
KRPM15B 1986.04 26.68
KRPM15B 1986.08 27.46
KRPM15B 1986.22 26.53
KRPM15B 1986.35 25.61
259

KRPM15B 1986.48 24.07
KRPM15B 1986.62 23.09
KRPM15B 1986.75 22.64
KRPM15B 1986.78 22.81
KRPM15B 1986.81 22.91
KRPM15B 1986.84 23.44
KRPM15B 1986.87 24.29
KRPM15B 1986.90 24.56
KRPM15B 1986.93 24.96
KRPM15B 1986.96 25.47
KRPM15B 1986.99 25.92
KRPM15B 1987.02 26.56
KRPM15B 1987.05 27.53
KRPM15B 1987.08 28.18
KRPM15B 1987.25 27.55
KRPM15B 1987.42 26.26
KRPM15B 1987.58 24.38
KRPM15B 1987.75 24.20
KRPM15B 1987.81 24.50
KRPM15B 1987.86 24.47
KRPM15B 1987.92 24.82
KRPM15B 1987.97 25.58
KRPM15B 1988.03 26.87
KRPM15B 1988.08 27.22
KRPM15B 1988.17 26.36
KRPM15B 1988.25 25.11
KRPM15B 1988.33 25.29
KRPM15B 1988.42 25.10
KRPM15B 1988.50 24.98
KRPM15B 1988.58 24.28
KRPM15B 1988.67 23.49
KRPM15B 1988.75 22.17
KRPM15B 1988.80 23.02
KRPM15B 1988.85 23.84
KRPM15B 1988.89 24.37
KRPM15B 1988.94 25.22
KRPM15B 1988.99 26.50
KRPM15B 1989.04 27.45
KRPM15B 1989.08 27.45
KRPM15B 1989.16 26.27
KRPM15B 1989.23 25.98
KRPM15B 1989.31 26.66
KRPM15B 1989.38 26.56
KRPM15B 1989.45 26.14
KRPM15B 1989.53 25.92
KRPM15B 1989.60 25.86
KRPM15B 1989.68 24.84
KRPM15B 1989.75 24.42
260

KRPM15B 1989.82 24.55
KRPM15B 1989.88 25.50
KRPM15B 1989.95 26.35
KRPM15B 1990.02 27.73
KRPM15B 1990.08 28.48
KRPM15B 1990.42 28.02
KRPM15B 1990.75 25.46
KRPM15B 1990.82 25.48
KRPM15B 1990.88 25.72
KRPM15B 1990.95 26.54
KRPM15B 1991.02 27.15
KRPM15B 1991.08 27.60
KRPM15B 1991.19 26.84
KRPM15B 1991.31 25.06
KRPM15B 1991.42 24.18
KRPM15B 1991.53 24.18
KRPM15B 1991.64 23.86
KRPM15B 1991.75 23.48
KRPM15B 1991.81 23.77
KRPM15B 1991.86 24.06
KRPM15B 1991.92 24.77
KRPM15B 1991.97 26.07
KRPM15B 1992.03 27.31
KRPM15B 1992.08 27.68
KRPM15B 1992.31 26.88
KRPM15B 1992.53 25.22
KRPM15B 1992.75 25.01
KRPM15B 1992.81 25.56
KRPM15B 1992.86 26.04
KRPM15B 1992.92 26.41
KRPM15B 1992.97 27.08
KRPM15B 1993.03 27.38
KRPM15B 1993.08 27.61
KRPM15B 1993.16 27.38
KRPM15B 1993.23 26.17
KRPM15B 1993.31 25.70
KRPM15B 1993.38 25.32
KRPM15B 1993.45 24.06
KRPM15B 1993.53 23.50
KRPM15B 1993.60 22.99
KRPM15B 1993.68 22.53
KRPM15B 1993.75 22.34
KRPM15B 1993.82 23.39
KRPM15B 1993.88 24.49
KRPM15B 1993.95 25.30
KRPM15B 1994.02 25.48
KRPM15B 1994.08 26.50
KRPM15B 1994.19 25.79
261

KRPM15B 1994.31 25.22
KRPM15B 1994.42 24.70
KRPM15B 1994.53 24.36
KRPM15B 1994.64 24.41
KRPM15B 1994.75 24.27
KRPM15B 1994.82 24.62
KRPM15B 1994.88 25.15
KRPM15B 1994.95 26.19
KRPM15B 1995.02 27.31
KRPM15B 1995.08 27.76
KRPM15B 1995.25 27.57
KRPM15B 1995.42 24.89
KRPM15B 1995.58 22.34
KRPM15B 1995.75 21.61
KRPM15B 1995.82 21.84
KRPM15B 1995.88 22.16
KRPM15B 1995.95 24.16
KRPM15B 1996.02 25.05
KRPM15B 1996.08 25.46
KRPM15B 1996.25 25.35
KRPM15B 1996.42 24.40
KRPM15B 1996.58 23.18
KRPM15B 1996.75 22.51
KRPM15B 1996.80 22.71
KRPM15B 1996.85 23.07
KRPM15B 1996.89 23.54
KRPM15B 1996.94 24.53
KRPM15B 1996.99 26.38
KRPM15B 1997.04 27.35
KRPM15B 1997.08 28.51
KRPM15B 1997.25 26.41
KRPM15B 1997.42 25.00
KRPM15B 1997.58 25.08
KRPM15B 1997.75 24.96
KRPM15B 1998.08 26.29
KRPM15B 1998.25 25.24
KRPM15B 1998.42 22.51
KRPM15B 1998.58 22.99
KRPM15B 1998.75 22.40
KRPM15B 1998.79 23.47
KRPM15B 1998.82 24.26
KRPM15B 1998.86 24.75
KRPM15B 1998.90 25.77
KRPM15B 1998.94 25.31
KRPM15B 1998.97 24.62
KRPM15B 1999.01 25.17
KRPM15B 1999.05 25.98
KRPM15B 1999.08 26.23
262

KRPM15B 1999.17 25.86
KRPM15B 1999.25 26.09
KRPM15B 1999.33 25.57
KRPM15B 1999.42 25.36
KRPM15B 1999.50 24.28
KRPM15B 1999.58 22.32
KRPM15B 1999.67 20.85
KRPM15B 1999.75 20.20
KRPM15B 1999.77 21.09
KRPM15B 1999.80 21.99
KRPM15B 1999.82 23.51
KRPM15B 1999.85 24.33
KRPM15B 1999.87 24.95
KRPM15B 1999.89 25.83
KRPM15B 1999.92 26.00
KRPM15B 1999.94 26.16
KRPM15B 1999.96 25.10
KRPM15B 1999.99 25.11
KRPM15B 2000.01 25.68
KRPM15B 2000.04 25.39
KRPM15B 2000.06 25.96
KRPM15B 2000.08 26.87
KRPM15B 2000.18 26.32
KRPM15B 2000.27 25.52
KRPM15B 2000.37 25.59
KRPM15B 2000.46 25.15
KRPM15B 2000.56 24.68
KRPM15B 2000.65 24.01
KRPM15B 2000.75 23.81
KRPM15B 2000.80 24.23
KRPM15B 2000.85 25.27
KRPM15B 2000.89 25.72
KRPM15B 2000.94 25.88
KRPM15B 2000.99 26.98
KRPM15B 2001.04 26.52
KRPM15B 2001.08 27.04
KRPM15B 2001.19 26.50
KRPM15B 2001.31 25.56
KRPM15B 2001.42 25.64
KRPM15B 2001.53 24.56
KRPM15B 2001.64 23.41
KRPM15B 2001.75 22.93
KRPM15B 2001.82 23.68
KRPM15B 2001.88 24.33
KRPM15B 2001.95 25.12
KRPM15B 2002.02 25.52
KRPM15B 2002.08 25.93
KRPM15B 2002.31 25.53
263

KRPM15B 2002.53 25.18
KRPM15B 2002.75 25.01
KRPM15B 2002.86 25.08
KRPM15B 2002.97 25.62
KRPM15B 2003.08 26.38
KRPM15B 2003.19 26.16
KRPM15B 2003.31 26.11
KRPM15B 2003.42 25.46
KRPM15B 2003.53 24.52
KRPM15B 2003.64 23.70
KRPM15B 2003.75 23.58
KRPM15B 2003.82 24.33
KRPM15B 2003.88 24.92
KRPM15B 2003.95 25.93
KRPM15B 2004.02 26.63
KRPM15B 2004.08 27.21
KRPM15B 2004.75 25.97
KRPM15B 2004.82 26.19
KRPM15B 2004.88 26.92
KRPM15B 2004.95 26.94
KRPM15B 2005.02 27.25
KRPM15B 2005.08 27.51
KRPM15B 2005.25 25.44
KRPM15B 2005.42 24.90
KRPM15B 2005.58 24.54
KRPM15B 2005.75 24.41
KRPM15B 2005.83 24.73
KRPM15B 2005.92 24.69
KRPM15B 2006.00 25.84
KRPM15B 2006.08 26.38
KRPM15B 2006.19 24.80
KRPM15B 2006.31 25.20
KRPM15B 2006.42 25.70
KRPM15B 2006.53 25.49
KRPM15B 2006.64 25.28
KRPM15B 2006.75 24.58
KRPM15B 2006.92 24.74
KRPM15B 2007.08 26.05

264

Appendix D. KRPM monthly interpolated cellulose δ
18
O values

Year Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec
1867 27.18 26.79 26.11 26.01 26.01 26.20 25.67 24.66 23.70 24.86 24.02 27.37
1868 29.59 27.24 25.67 26.24 26.46 25.40 25.04 23.96 22.48 22.92 24.74 27.71
1869 28.82 25.82 24.80 24.20 23.71 23.52 23.02 22.65 22.94 23.74 26.20 27.44
1870 28.63 27.12 26.86 25.97 25.20 24.55 23.97 23.65 22.71 24.14 25.02 26.59
1871 28.54 26.00 25.41 24.91 24.47 23.93 23.39 23.13 22.95 23.46 25.54 27.39
1872 28.45 27.60 25.30 24.17 24.10 23.82 23.33 22.36 21.68 24.14 25.88 27.52
1873 29.20 27.87 25.69 25.51 25.19 25.28 24.07 24.48 23.33 23.79 25.23 27.02
1874 28.37 26.50 25.71 24.90 24.01 23.43 23.01 22.69 22.28 23.07 24.76 25.93
1875 26.73 25.35 25.14 24.87 24.61 24.41 24.35 24.24 24.03 24.84 25.74 25.90
1876 27.50 26.53 26.13 25.65 25.08 24.78 24.55 23.83 23.33 23.74 24.75 26.04
1877 27.22 26.13 25.39 25.18 24.83 24.45 24.12 23.87 23.67 24.25 24.86 26.02
1878 28.20 26.06 25.06 24.65 24.28 24.12 23.93 23.64 23.21 23.77 24.99 26.35
1879 27.66 26.73 26.24 25.29 24.38 24.65 24.24 23.97 23.54 24.49 25.82 25.69
1880 26.59 26.33 26.00 25.57 25.12 24.75 24.43 24.18 23.96 24.97 25.91 26.66
1881 27.46 27.08 26.51 25.65 24.82 24.11 23.56 23.17 22.90 23.72 24.11 25.55
1882 26.72 26.28 25.37 24.85 24.46 24.18 23.56 22.91 22.34 23.40 24.60 25.81
1883 27.13 26.15 26.11 25.40 25.31 25.39 25.40 24.79 24.33 24.89 25.62 26.53
1884 27.42 26.88 26.12 25.92 25.88 25.49 25.20 24.80 24.53 24.84 25.42 27.25
1885 28.29 27.23 25.87 25.61 25.34 25.09 24.52 24.11 23.95 24.51 25.41 26.72
1886 28.35 27.44 26.11 25.11 22.82 22.30 22.11 21.76 21.36 23.07 24.49 26.15
1887 27.69 26.83 25.86 25.40 24.96 24.88 24.77 24.06 23.61 25.13 24.95 25.71
1888 27.56 27.36 27.02 26.61 26.21 25.93 25.62 25.30 25.00 25.57 26.26 27.23
1889 27.73 26.56 25.08 24.68 24.61 24.02 23.31 23.04 22.84 23.41 24.91 26.27
1890 27.37 27.01 26.13 25.70 25.64 25.27 24.70 24.11 23.51 24.13 25.21 26.42
1891 27.26 27.06 26.86 26.66 26.49 26.21 25.81 25.35 24.89 25.80 26.11 27.42
1892 29.31 28.05 27.53 27.20 26.67 26.02 25.29 24.34 23.22 24.10 24.83 25.47
1893 27.07 26.46 25.76 25.39 24.72 24.62 24.70 24.35 24.10 25.12 26.16 27.06
1894 27.71 26.97 26.21 25.84 25.41 24.89 24.33 23.74 23.49 23.89 25.10 27.13
1895 28.19 27.01 25.83 24.91 24.52 24.43 24.50 24.55 24.39 25.09 26.11 27.06
1896 28.07 27.19 26.74 26.49 26.43 26.36 26.14 25.78 25.47 25.69 25.90 27.09
1897 28.89 28.23 26.43 25.55 25.19 25.02 24.46 23.89 22.97 23.63 24.55 25.68
1898 26.74 26.38 26.02 25.69 25.42 25.22 24.98 24.71 24.43 24.19 25.02 26.72
1899 27.75 27.39 26.98 26.47 25.51 25.02 25.20 24.85 24.81 25.97 26.58 27.21
1900 28.20 27.34 26.49 25.87 25.71 25.64 25.49 25.30 25.12 25.56 26.22 27.53
1901 28.34 27.13 27.04 27.26 26.88 26.02 25.22 24.56 24.42 24.40 25.01 26.95
1902 28.68 28.48 27.72 27.36 27.87 27.35 26.75 25.08 25.31 25.81 26.65 27.19
265

1903 27.61 27.39 27.17 26.95 26.73 26.04 25.35 24.66 23.97 24.35 25.05 26.14
1904 27.60 26.37 26.99 26.42 26.09 25.32 24.75 24.39 24.07 24.75 26.08 27.26
1905 27.82 27.31 26.87 26.53 26.00 25.58 25.07 24.91 24.98 25.51 26.31 27.09
1906 27.56 27.44 27.33 27.23 26.82 26.32 25.77 25.54 25.54 25.97 25.90 27.67
1907 28.93 28.13 27.43 26.90 26.57 26.53 26.27 25.94 25.57 25.84 26.09 26.96
1908 28.07 27.65 26.98 26.22 25.54 25.40 25.10 24.77 24.54 25.94 26.70 27.78
1909 28.10 27.30 26.45 25.94 25.74 25.20 25.23 24.53 24.07 25.31 26.00 27.03
1910 27.77 27.58 26.84 26.92 26.39 24.74 24.03 23.75 23.06 23.97 25.19 26.15
1911 27.68 27.55 27.42 27.13 26.54 25.95 25.69 25.60 25.50 26.09 27.12 28.23
1912 29.04 28.83 28.62 28.41 27.63 26.85 26.62 26.04 25.21 25.96 27.04 28.02
1913 29.08 28.29 27.29 27.13 27.10 26.70 26.20 25.29 24.63 25.88 27.31 28.32
1914 28.55 27.72 26.89 26.54 26.17 25.79 25.51 25.03 24.54 26.20 27.05 28.14
1915 29.35 28.27 26.88 26.05 25.80 25.12 24.60 24.16 23.25 23.97 24.87 26.82
1916 28.73 27.50 26.10 25.00 24.36 23.75 23.50 23.10 22.91 24.32 25.39 26.23
1917 27.08 26.56 25.72 24.58 23.74 22.87 22.23 21.96 21.63 22.75 24.15 25.41
1918 26.59 25.98 25.57 25.49 25.49 25.11 25.13 25.13 24.48 25.66 26.17 27.05
1919 28.44 26.94 26.40 25.90 25.17 24.86 24.52 24.13 24.00 24.36 26.11 27.34
1920 27.97 27.29 26.71 26.53 26.30 25.70 25.12 24.56 23.84 24.38 25.13 26.29
1921 28.46 26.59 26.05 25.71 25.37 25.11 24.66 24.18 23.73 23.96 24.72 26.51
1922 27.44 26.80 26.30 26.20 25.99 25.29 23.96 22.90 22.09 22.41 23.17 24.36
1923 25.50 25.12 24.87 24.62 24.48 24.60 24.22 23.36 23.10 24.03 24.84 26.04
1924 27.20 26.00 24.98 24.35 24.10 23.83 23.51 23.27 23.04 23.36 24.75 26.72
1925 27.75 26.52 26.02 25.84 25.60 25.48 25.33 25.09 24.68 25.13 27.10 27.60
1926 28.72 27.82 26.25 25.21 24.37 23.83 23.21 22.69 22.21 23.77 24.17 26.29
1927 27.86 27.45 26.96 26.69 26.10 25.28 24.67 24.24 24.10 24.83 25.56 26.35
1928 27.31 27.26 27.21 26.56 26.29 25.70 25.18 24.49 24.19 24.83 25.65 27.02
1929 28.32 27.46 26.61 26.35 26.27 25.79 25.12 24.58 23.86 25.01 26.11 27.12
1930 28.02 27.52 27.03 26.82 26.65 26.64 26.10 25.30 24.61 25.14 25.47 25.92
1931 26.43 25.71 24.56 23.85 23.26 23.29 22.98 22.03 21.63 23.01 24.89 26.24
1932 27.58 26.26 25.04 24.11 23.52 23.02 22.92 22.80 22.62 23.30 25.00 26.46
1933 26.99 26.64 25.74 25.52 25.22 24.54 23.74 23.14 22.76 23.46 24.71 26.09
1934 27.16 26.29 25.87 25.49 25.16 25.12 25.12 25.09 24.93 25.36 26.11 27.04
1935 27.99 27.82 27.31 26.21 25.63 25.12 24.40 23.95 23.69 24.54 24.50 25.00
1936 26.44 26.09 25.71 25.52 25.56 25.46 25.35 24.70 24.32 25.40 26.80 27.34
1937 28.10 27.54 26.98 26.26 25.23 24.40 23.91 23.60 23.30 24.11 25.28 26.57
1938 27.49 26.68 26.24 25.85 25.18 24.72 24.30 23.94 23.63 24.32 25.19 26.75
1939 27.63 27.51 27.51 27.28 26.34 25.47 24.69 24.21 23.64 24.10 24.62 25.90
1940 27.73 27.65 27.10 26.73 26.66 26.28 25.89 25.51 25.15 25.76 26.18 27.32
1941 28.43 27.41 27.40 27.36 26.61 25.96 25.00 24.11 23.34 24.39 25.23 26.25
1942 28.29 27.45 26.23 25.79 25.57 24.49 24.43 24.14 23.71 24.40 25.28 26.65
266

1943 27.85 27.36 25.81 24.64 24.47 24.90 25.02 24.53 24.11 25.00 26.26 27.12
1944 27.47 26.82 26.39 26.00 25.58 25.09 24.56 24.28 24.11 24.54 25.04 26.08
1945 26.75 26.19 26.32 25.77 25.01 24.61 25.01 25.24 24.56 25.28 26.00 26.85
1946 27.70 27.15 26.46 25.60 25.24 25.02 24.69 24.15 23.35 24.36 25.31 26.33
1947 27.33 26.93 26.53 25.96 25.39 24.75 24.12 23.72 23.32 23.96 26.08 26.41
1948 27.54 26.88 25.94 25.43 25.26 25.24 24.94 24.44 23.71 24.43 26.23 27.44
1949 28.79 27.11 26.08 25.17 24.46 23.83 23.53 23.28 23.08 24.24 26.24 27.57
1950 28.06 27.17 26.50 25.38 24.12 23.97 24.28 24.04 23.50 24.65 26.40 27.81
1951 28.47 27.21 26.32 25.39 25.68 25.75 25.03 23.64 22.40 23.42 23.42 25.85
1952 27.57 27.01 26.86 26.13 25.39 25.18 25.04 24.41 23.16 24.27 25.49 26.46
1953 26.87 26.36 25.71 25.82 25.68 24.89 24.41 24.24 24.06 24.58 25.09 25.55
1954 26.00 24.78 24.17 24.23 24.42 24.60 24.11 23.37 22.80 23.47 24.95 26.35
1955 27.22 26.97 26.01 25.30 24.84 24.67 24.20 23.44 22.99 23.41 24.72 25.87
1956 26.11 25.75 25.44 25.24 25.05 24.52 23.97 23.28 22.43 23.65 24.76 26.19
1957 27.39 26.91 25.62 24.78 24.45 24.17 24.08 24.16 23.26 23.94 25.08 26.16
1958 26.86 25.98 25.29 24.73 24.88 25.06 24.62 24.33 22.69 23.24 23.79 24.76
1959 25.73 24.93 24.13 24.33 24.53 24.42 24.31 23.77 23.23 23.66 24.95 26.03
1960 26.74 26.28 25.06 24.99 25.21 25.49 25.35 24.69 23.58 23.66 24.70 25.43
1961 26.79 26.63 26.43 26.00 25.47 25.26 25.11 24.32 23.67 24.21 24.78 25.67
1962 26.28 26.02 25.49 24.92 24.28 23.63 23.60 23.50 22.86 24.36 25.69 26.81
1963 28.03 27.10 26.18 25.44 25.12 24.82 24.47 24.31 24.16 24.68 25.54 26.24
1964 27.42 26.59 25.75 25.02 24.52 24.27 24.14 24.03 23.85 24.59 26.14 26.67
1965 26.83 26.07 25.56 25.41 25.21 24.91 24.40 23.91 23.45 23.76 24.08 25.05
1966 26.02 25.83 25.70 25.76 25.54 25.19 25.03 24.68 24.37 25.28 25.18 25.31
1967 25.97 25.68 25.38 25.45 25.53 25.25 24.97 24.70 24.43 25.17 26.27 26.81
1968 27.92 27.16 26.29 25.94 25.93 25.79 25.21 24.39 24.07 25.16 27.18 27.97
1969 28.29 27.61 26.52 25.35 24.32 23.79 23.48 23.16 22.74 23.76 25.02 26.32
1970 26.85 26.14 25.44 24.78 24.69 24.61 23.96 23.19 22.82 23.41 24.50 26.41
1971 27.10 26.59 26.27 25.66 24.98 24.62 24.02 23.61 23.26 24.19 25.64 26.77
1972 27.51 26.70 26.08 26.15 26.11 25.72 25.40 24.69 23.99 24.66 25.29 25.70
1973 26.96 26.22 25.65 25.41 25.15 24.55 23.80 22.81 21.78 23.22 24.92 25.12
1974 26.04 25.60 25.23 24.93 24.73 24.34 23.73 23.00 22.20 23.33 24.40 25.43
1975 25.94 25.78 25.45 25.07 24.74 24.42 23.78 22.75 21.88 23.66 26.14 26.07
1976 26.92 26.56 26.28 26.14 25.70 25.42 25.21 24.88 24.42 25.27 25.57 27.25
1977 27.85 27.51 27.04 26.77 26.42 26.13 26.14 26.05 25.84 25.94 26.38 27.23
1978 27.82 27.36 26.65 26.02 25.47 25.15 24.93 24.76 24.64 25.06 25.39 26.32
1979 28.09 27.48 26.93 26.04 25.73 25.62 26.07 24.94 24.70 25.04 25.84 26.30
1980 27.09 25.98 25.27 25.29 25.49 25.62 25.63 24.69 23.83 24.92 25.68 26.30
1981 26.96 26.26 25.90 25.46 25.19 24.90 24.58 24.26 24.06 24.47 25.55 26.73
1982 27.39 26.61 26.31 26.07 26.05 25.98 25.85 25.72 25.59 25.79 26.17 26.70
267

1983 27.40 27.01 26.61 26.14 25.53 24.82 24.41 24.16 23.91 24.63 25.03 26.56
1984 27.31 27.02 26.68 26.30 25.94 25.49 24.93 24.41 24.06 24.84 25.77 26.64
1985 27.37 26.93 26.85 26.59 25.92 25.42 24.85 23.60 22.80 23.85 24.48 25.67
1986 27.46 26.88 26.30 25.73 24.84 23.95 23.34 22.92 22.64 23.31 24.76 26.08
1987 27.72 27.53 26.50 25.80 25.48 25.03 24.42 24.11 24.04 24.48 25.19 25.88
1988 26.56 25.99 25.28 24.96 24.86 24.80 24.34 23.19 21.55 23.49 25.36 26.53
1989 27.21 26.12 25.52 26.21 25.91 25.55 25.58 24.76 24.08 25.27 26.13 27.01
1990 27.94 27.62 27.50 27.32 27.19 26.76 26.13 25.37 24.83 25.10 25.76 26.62
1991 27.33 26.84 26.13 25.14 24.59 24.67 24.48 24.11 23.62 23.96 25.29 27.60
1992 28.20 27.75 27.20 26.81 26.84 26.09 25.48 25.03 24.80 25.81 26.01 26.57
1993 28.62 27.89 26.73 26.13 25.38 24.57 24.53 23.88 22.78 23.47 24.56 25.54
1994 26.80 26.30 25.83 25.51 25.07 24.77 24.87 24.49 24.13 24.91 26.12 27.85
1995 28.56 28.13 27.24 26.20 24.74 23.62 22.57 21.86 21.48 22.94 25.04 25.77
1996 26.32 25.88 25.26 25.24 24.65 24.42 24.31 23.19 22.15 22.92 23.76 27.03
1997 28.70 28.05 27.24 27.10 25.09 25.39 25.96 25.15 24.48 24.99 25.65 26.20
1998 27.04 26.34 25.52 25.10 24.01 23.52 23.58 22.72 21.83 23.66 24.81 25.57
1999 27.50 27.29 26.81 26.11 25.76 25.24 23.99 22.48 22.11 24.97 25.82 24.88
2000 26.15 26.18 25.75 25.54 25.52 25.62 25.27 24.83 23.99 24.72 25.68 26.78
2001 27.03 26.57 26.26 26.17 26.35 25.42 25.26 24.07 23.01 24.09 25.41 26.37
2002 26.96 26.57 26.27 26.61 26.67 25.86 25.16 24.96 24.59 25.35 25.95 26.46
2003 27.11 26.79 26.12 25.34 24.59 24.36 24.24 24.28 23.29 24.85 24.51 25.76
2004 27.98 27.78 27.25 27.18 26.60 25.79 26.08 26.24 25.01 25.97 26.48 26.47
2005 27.83 27.01 26.22 25.86 25.32 24.85 24.68 24.47 24.20 24.96 25.11 25.77
2006 26.38 25.20 25.00 25.33 25.70 25.54 25.38 25.10 24.58 24.66 24.74 N/A

268

Appendix E. TDB and XDC annual cellulose δ
18
O values

Core Year δ
18
O(‰)
TDB05A 2002 31.73
TDB05A 2001 30.60
TDB05A 2000 30.77
TDB05A 1999 30.39
TDB05A 1998 31.51
TDB05A 1997 29.34
TDB05A 1996 28.38
TDB05A 1995 31.74
TDB05A 1994 31.88
TDB05A 1993 30.36
TDB05A 1992 30.15
TDB05A 1991 31.49
TDB05A 1990 30.63
TDB05A 1989 29.41
TDB05A 1988 31.28
TDB05A 1987 30.69
TDB05A 1986 30.50
TDB05A 1985 31.06
TDB05A 1984 29.33
TDB05A 1983 29.27
TDB05A 1982 29.12
TDB05A 1981 32.13
TDB05A 1980 31.79
TDB05A 1979 32.30
TDB05A 1978 31.08
TDB05A 1977 29.82
TDB05A 1976 29.95
TDB05A 1975 30.36
TDB05A 1974 30.46
TDB05A 1966 31.82
TDB05A 1965 29.75
TDB05A 1964 29.80
TDB05A 1963 31.76
TDB05A 1962 29.41
TDB05A 1961 29.95
269

TDB05A 1960 32.68
TDB05A 1959 30.35
TDB05A 1958 31.58
TDB05A 1957 30.36
TDB05A 1956 31.25
TDB05A 1955 29.73
TDB05A 1954 30.34
TDB05A 1953 31.01
TDB05A 1952 29.89
TDB05A 1951 29.25
TDB05A 1950 31.25
TDB05A 1949 28.88
TDB05A 1948 29.47
TDB05A 1947 29.97
TDB05A 1946 30.01
TDB05A 1945 31.80
TDB05A 1944 30.32
TDB05A 1943 28.07
TDB05A 1942 30.67
TDB05A 1941 31.22
TDB05A 1940 30.06
TDB05A 1933 30.51
TDB05A 1932 29.67
TDB05A 1931 30.67
TDB05A 1930 29.89
TDB05A 1929 30.58
TDB05A 1928 29.65
TDB05A 1927 29.51
TDB05A 1926 31.15
TDB05A 1925 30.42
TDB05A 1924 31.09
TDB05A 1923 29.94
TDB05A 1922 30.32
TDB05A 1921 29.50
TDB05A 1920 28.81
TDB05A 1919 30.18
TDB05A 1918 30.31
TDB05A 1917 27.31
TDB05A 1916 29.06
TDB05A 1915 28.70
270

TDB05A 1914 27.46
TDB05A 1913 28.08
TDB05A 1912 28.96
TDB05A 1911 29.89
TDB05A 1910 28.16
TDB05A 1909 29.33
TDB05A 1908 29.14
TDB05A 1907 27.75
TDB05A 1906 26.67
TDB05A 1905 27.89
TDB05A 1904 25.18
TDB05A 1903 27.24
TDB05A 1902 30.34
TDB05A 1901 29.77
TDB05A 1900 28.48
TDB05A 1899 28.88
TDB05A 1898 32.29
TDB05A 1897 29.78
TDB05A 1896 31.33
TDB05A 1895 29.45
TDB05A 1894 29.68
TDB05A 1893 28.08
TDB05A 1892 29.92
TDB05A 1891 29.06
TDB05A 1890 27.80
TDB05A 1889 29.31
TDB05A 1888 26.81
TDB05A 1887 28.46
TDB05A 1886 27.46
TDB05A 1885 27.85
TDB05A 1884 29.21
TDB05A 1883 29.52
TDB05A 1882 29.53
TDB05A 1881 29.19
TDB05A 1880 29.74
TDB05A 1879 31.20
TDB05A 1878 29.83
TDB05A 1877 28.14
TDB05A 1876 28.48
TDB05A 1875 28.48
271

TDB05A 1874 27.87
TDB05A 1873 28.77
TDB05A 1872 28.57
TDB05A 1871 27.82
TDB05A 1870 28.19
TDB05A 1869 27.31
TDB05A 1868 26.86
TDB05A 1867 26.76
TDB05A 1866 28.94
TDB05A 1865 27.35
TDB05A 1864 28.06
TDB05A 1863 29.14
TDB05A 1862 29.70
TDB05A 1861 30.62
TDB05A 1860 30.47
TDB05A 1859 30.33
TDB05A 1858 28.29
TDB05A 1857 29.20
TDB05A 1856 28.32
TDB05A 1855 27.60
TDB05A 1854 29.10
TDB05A 1853 30.45
TDB05A 1852 29.71
TDB05A 1851 28.10
TDB05A 1850 28.73
TDB05A 1849 28.12
TDB05A 1848 27.06
TDB05A 1847 30.62
TDB05A 1846 30.93
TDB05A 1845 30.63
TDB05A 1844 30.19
TDB05A 1843 29.44
TDB05A 1842 30.04
TDB05A 1841 28.31
TDB05A 1840 29.74
TDB05A 1839 29.91
TDB05A 1838 29.56
TDB05A 1837 30.15
TDB05A 1836 30.13
TDB05A 1835 28.24
272

TDB05A 1834 31.01
TDB05A 1833 31.16
TDB05A 1832 28.16
TDB05A 1831 30.87
TDB05A 1830 28.30
TDB05A 1829 30.45
TDB05A 1828 28.86
TDB05A 1827 27.42
TDB05A 1826 29.83
TDB05A 1825 29.18
TDB05A 1824 30.31
TDB05A 1823 29.99
TDB05A 1822 30.89
TDB05A 1821 30.00
TDB27A 2002 30.34
TDB27A 2001 31.11
TDB27A 2000 29.26
TDB27A 1999 27.55
TDB27A 1998 29.36
TDB27A 1997 28.26
TDB27A 1996 27.62
TDB27A 1995 30.67
TDB27A 1994 32.02
TDB27A 1993 28.95
TDB27A 1992 30.02
TDB27A 1991 30.08
TDB27A 1990 29.62
TDB27A 1989 26.88
TDB27A 1988 30.01
TDB27A 1987 29.00
TDB27A 1986 28.18
TDB27A 1985 30.12
TDB27A 1984 27.71
TDB27A 1983 28.26
TDB27A 1982 27.45
TDB27A 1981 27.77
TDB27A 1980 28.57
TDB27A 1979 28.43
TDB27A 1978 27.26
TDB27A 1977 27.26
273

TDB27A 1976 27.00
TDB27A 1975 27.31
TDB27A 1974 27.82
TDB27A 1973 29.42
TDB27A 1972 25.54
TDB27A 1971 28.17
TDB27A 1970 27.82
TDB27A 1969 28.15
TDB27A 1968 27.28
TDB27A 1967 25.22
TDB27A 1966 27.31
TDB27A 1965 29.25
TDB27A 1964 26.94
TDB27A 1963 28.39
TDB27A 1962 27.61
TDB27A 1961 27.86
TDB27A 1960 28.92
TDB27A 1959 28.52
TDB27A 1958 29.27
TDB27A 1957 29.58
TDB27A 1956 29.53
TDB27A 1955 27.07
TDB27A 1954 26.39
TDB27A 1953 29.72
TDB27A 1952 27.73
TDB27A 1951 27.19
TDB27A 1950 29.13
TDB27A 1949 27.81
TDB27A 1948 27.51
TDB27A 1947 27.15
TDB27A 1946 28.59
TDB27A 1945 31.09
TDB27A 1944 30.85
TDB27A 1943 27.84
TDB27A 1942 31.30
TDB27A 1941 28.66
TDB27A 1940 30.34
TDB27A 1939 28.33
TDB27A 1938 28.37
TDB27A 1937 27.91
274

TDB27A 1936 27.36
TDB27A 1935 26.66
TDB27A 1934 29.87
TDB27A 1933 29.29
TDB27A 1932 30.33
TDB27A 1931 29.90
TDB27A 1930 29.73
TDB27A 1929 30.43
TDB27A 1928 29.35
TDB27A 1927 28.75
TDB27A 1926 32.10
TDB27A 1925 30.34
TDB27A 1924 30.02
TDB27A 1923 28.65
TDB27A 1922 30.07
TDB27A 1921 29.16
TDB27A 1920 28.96
TDB27A 1919 29.87
TDB27A 1918 29.50
TDB27A 1917 27.20
TDB27A 1916 30.08
TDB27A 1915 28.54
TDB27A 1914 25.09
TDB27A 1913 26.04
TDB27A 1912 27.82
TDB27A 1911 27.48
TDB27A 1910 26.57
TDB27A 1909 27.57
TDB27A 1908 27.71
TDB27A 1907 26.64
TDB27A 1906 26.82
TDB27A 1905 27.54
TDB27A 1904 25.12
TDB27A 1903 24.67
TDB27A 1902 28.11
TDB27A 1901 28.72
TDB27A 1900 28.79
TDB27A 1899 27.84
TDB27A 1898 29.03
TDB27A 1897 28.99
275

TDB27A 1896 30.18
TDB27A 1895 28.69
TDB27A 1894 29.80
TDB27A 1893 26.92
TDB27A 1892 28.81
TDB27A 1891 29.06
TDB27A 1890 27.53
TDB27A 1889 26.88
TDB27A 1888 26.84
TDB27A 1887 28.05
TDB27A 1886 27.26
TDB27A 1885 26.81
TDB27A 1884 27.89
TDB27A 1883 30.10
TDB27A 1882 29.43
TDB27A 1881 29.86
TDB27A 1880 30.37
TDB27A 1879 29.99
TDB27A 1878 30.73
TDB27A 1877 27.84
TDB27A 1876 28.27
TDB27A 1875 26.02
TDB27A 1874 27.85
TDB27A 1873 28.45
TDB27A 1872 28.58
TDB27A 1871 27.81
TDB27A 1870 27.20
TDB27A 1869 26.52
TDB27A 1868 24.21
TDB27A 1867 26.54
TDB27A 1866 26.81
TDB27A 1865 26.93
TDB27A 1864 28.52
TDB27A 1863 27.82
TDB27A 1862 30.00
TDB27A 1861 31.23
TDB27A 1860 30.36
TDB27A 1859 29.15
TDB27A 1858 28.31
TDB27A 1857 28.58
276

TDB27A 1856 27.15
TDB27A 1855 26.31
TDB27A 1854 28.32
TDB27A 1853 29.04
TDB27A 1852 29.37
TDB27A 1851 27.16
TDB27A 1850 26.59
TDB27A 1849 26.39
TDB27A 1848 26.37
TDB27A 1847 28.13
TDB27A 1846 30.18
TDB27A 1845 29.53
TDB27A 1844 28.93
TDB27A 1843 29.42
TDB27A 1842 29.21
TDB27A 1841 27.90
TDB27A 1840 27.78
TDB27A 1839 28.22
TDB27A 1838 28.31
TDB27A 1837 27.38
TDB27A 1836 29.89
TDB27A 1835 26.77
TDB27A 1834 29.37
TDB27A 1833 29.66
TDB27A 1832 28.41
TDB27A 1831 30.44
TDB27A 1830 27.46
TDB27A 1829 29.38
TDB27A 1828 27.79
TDB27A 1827 25.95
TDB27A 1826 28.12
TDB27A 1825 27.17
TDB27A 1824 32.59
TDB27A 1823 28.82
TDB27A 1822 30.79
TDB27A 1821 28.95
TDB27A 1820 26.59
TDB27A 1819 27.96
TDB27A 1818 29.72
TDB27A 1817 27.32
277

TDB27A 1816 28.33
TDB27A 1815 27.98
TDB27A 1814 25.23
TDB27A 1813 28.35
TDB27A 1812 27.88
TDB27A 1811 28.43
TDB27A 1810 30.00
TDB27A 1809 29.51
TDB27A 1808 27.33
TDB27A 1807 27.87
TDB27A 1806 26.22
TDB27A 1805 27.18
TDB27A 1804 27.26
TDB27A 1803 24.87
TDB27A 1802 24.42
TDB27A 1801 27.70
TDB27A 1800 28.44
TDB28A 2002 30.34
TDB28A 2001 31.11
TDB28A 2000 29.26
TDB28A 1999 27.55
TDB28A 1998 29.36
TDB28A 1997 28.26
TDB28A 1996 27.62
TDB28A 1995 30.67
TDB28A 1994 32.02
TDB28A 1993 28.95
TDB28A 1992 30.02
TDB28A 1991 30.08
TDB28A 1990 29.62
TDB28A 1989 26.88
TDB28A 1988 30.01
TDB28A 1987 29.00
TDB28A 1986 28.18
TDB28A 1985 30.12
TDB28A 1984 27.71
TDB28A 1983 28.26
TDB28A 1982 27.45
TDB28A 1981 27.77
TDB28A 1980 28.57
278

TDB28A 1979 28.43
TDB28A 1978 27.26
TDB28A 1977 27.26
TDB28A 1976 27.00
TDB28A 1975 27.31
TDB28A 1974 27.82
TDB28A 1973 29.42
TDB28A 1972 25.54
TDB28A 1971 28.17
TDB28A 1970 27.82
TDB28A 1969 28.15
TDB28A 1968 27.28
TDB28A 1967 25.22
TDB28A 1966 27.31
TDB28A 1965 29.25
TDB28A 1964 26.94
TDB28A 1963 28.39
TDB28A 1962 27.61
TDB28A 1961 27.86
TDB28A 1960 28.92
TDB28A 1959 28.52
TDB28A 1958 29.27
TDB28A 1957 29.58
TDB28A 1956 29.53
TDB28A 1955 27.07
TDB28A 1954 26.39
TDB28A 1953 29.72
TDB28A 1952 27.73
TDB28A 1951 27.19
TDB28A 1950 29.13
TDB28A 1949 27.81
TDB28A 1948 27.51
TDB28A 1947 27.15
TDB28A 1946 28.59
TDB28A 1945 31.09
TDB28A 1944 30.85
TDB28A 1943 27.84
TDB28A 1942 31.30
TDB28A 1941 28.66
TDB28A 1940 30.34
279

TDB28A 1939 28.33
TDB28A 1938 28.37
TDB28A 1937 27.91
TDB28A 1936 27.36
TDB28A 1935 26.66
TDB28A 1934 29.87
TDB28A 1933 29.29
TDB28A 1932 30.33
TDB28A 1931 29.90
TDB28A 1930 29.73
TDB28A 1929 30.43
TDB28A 1928 29.35
TDB28A 1927 28.75
TDB28A 1926 32.10
TDB28A 1925 30.34
TDB28A 1924 30.02
TDB28A 1923 28.65
TDB28A 1922 30.07
TDB28A 1921 29.16
TDB28A 1920 28.96
TDB28A 1919 29.87
TDB28A 1918 29.50
TDB28A 1917 27.20
TDB28A 1916 30.08
TDB28A 1915 28.54
TDB28A 1914 25.09
TDB28A 1913 26.04
TDB28A 1912 27.82
TDB28A 1911 27.48
TDB28A 1910 26.57
TDB28A 1909 27.57
TDB28A 1908 27.71
TDB28A 1907 26.64
TDB28A 1906 26.82
TDB28A 1905 27.54
TDB28A 1904 25.12
TDB28A 1903 24.67
TDB28A 1902 28.11
TDB28A 1901 28.72
TDB28A 1900 28.79
280

TDB28A 1899 27.84
TDB28A 1898 29.03
TDB28A 1897 28.99
TDB28A 1896 30.18
TDB28A 1895 28.69
TDB28A 1894 29.80
TDB28A 1893 26.92
TDB28A 1892 28.81
TDB28A 1891 29.06
TDB28A 1890 27.53
TDB28A 1889 26.88
TDB28A 1888 26.84
TDB28A 1887 28.05
TDB28A 1886 27.26
TDB28A 1885 26.81
TDB28A 1884 27.89
TDB28A 1883 30.10
TDB28A 1882 29.43
TDB28A 1881 29.86
TDB28A 1880 30.37
TDB28A 1879 29.99
TDB28A 1878 30.73
TDB28A 1877 27.84
TDB28A 1876 28.27
TDB28A 1875 26.02
TDB28A 1874 27.85
TDB28A 1873 28.45
TDB28A 1872 28.58
TDB28A 1871 27.81
TDB28A 1870 27.20
TDB28A 1869 26.52
TDB28A 1868 24.21
TDB28A 1867 26.54
TDB28A 1866 26.81
TDB28A 1865 26.93
TDB28A 1864 28.52
TDB28A 1863 27.82
TDB28A 1862 30.00
TDB28A 1861 31.23
TDB28A 1860 30.36
281

TDB28A 1859 29.15
TDB28A 1858 28.31
TDB28A 1857 28.58
TDB28A 1856 27.15
TDB28A 1855 26.31
TDB28A 1854 28.32
TDB28A 1853 29.04
TDB28A 1852 29.37
TDB28A 1851 27.16
TDB28A 1850 26.59
TDB28A 1849 26.39
TDB28A 1848 26.37
TDB28A 1847 28.13
TDB28A 1846 30.18
TDB28A 1845 29.53
TDB28A 1844 28.93
TDB28A 1843 29.42
TDB28A 1842 29.21
TDB28A 1841 27.90
TDB28A 1840 27.78
TDB28A 1839 28.22
TDB28A 1838 28.31
TDB28A 1837 27.38
TDB28A 1836 29.89
TDB28A 1835 26.77
TDB28A 1834 29.37
TDB28A 1833 29.66
TDB28A 1832 28.41
TDB28A 1831 30.44
TDB28A 1830 27.46
TDB28A 1829 29.38
TDB28A 1828 27.79
TDB28A 1827 25.95
TDB28A 1826 28.12
TDB28A 1825 27.17
TDB28A 1824 32.59
TDB28A 1823 28.82
TDB28A 1822 30.79
TDB28A 1821 28.95
TDB28A 1820 26.59
282

TDB28A 1819 27.96
TDB28A 1818 29.72
TDB28A 1817 27.32
TDB28A 1816 28.33
TDB28A 1815 27.98
TDB28A 1814 25.23
TDB28A 1813 28.35
TDB28A 1812 27.88
TDB28A 1811 28.43
TDB28A 1810 30.00
TDB28A 1809 29.51
TDB28A 1808 27.33
TDB28A 1807 27.87
TDB28A 1806 26.22
TDB28A 1805 27.18
TDB28A 1804 27.26
TDB28A 1803 24.87
TDB28A 1802 24.42
TDB28A 1801 27.70
TDB28A 1800 28.44
TDB99A 2002 30.34
TDB99A 2001 31.11
TDB99A 2000 29.26
TDB99A 1999 27.55
TDB99A 1998 29.36
TDB99A 1997 28.26
TDB99A 1996 27.62
TDB99A 1995 30.67
TDB99A 1994 32.02
TDB99A 1993 28.95
TDB99A 1992 30.02
TDB99A 1991 30.08
TDB99A 1990 29.62
TDB99A 1989 26.88
TDB99A 1988 30.01
TDB99A 1987 29.00
TDB99A 1986 28.18
TDB99A 1985 30.12
TDB99A 1984 27.71
TDB99A 1983 28.26
283

TDB99A 1982 27.45
TDB99A 1981 27.77
TDB99A 1980 28.57
TDB99A 1979 28.43
TDB99A 1978 27.26
TDB99A 1977 27.26
TDB99A 1976 27.00
TDB99A 1975 27.31
TDB99A 1974 27.82
TDB99A 1973 29.42
TDB99A 1972 25.54
TDB99A 1971 28.17
TDB99A 1970 27.82
TDB99A 1969 28.15
TDB99A 1968 27.28
TDB99A 1967 25.22
TDB99A 1966 27.31
TDB99A 1965 29.25
TDB99A 1964 26.94
TDB99A 1963 28.39
TDB99A 1962 27.61
TDB99A 1961 27.86
TDB99A 1960 28.92
TDB99A 1959 28.52
TDB99A 1958 29.27
TDB99A 1957 29.58
TDB99A 1956 29.53
TDB99A 1955 27.07
TDB99A 1954 26.39
TDB99A 1953 29.72
TDB99A 1952 27.73
TDB99A 1951 27.19
TDB99A 1950 29.13
TDB99A 1949 27.81
TDB99A 1948 27.51
TDB99A 1947 27.15
TDB99A 1946 28.59
TDB99A 1945 31.09
TDB99A 1944 30.85
TDB99A 1943 27.84
284

TDB99A 1942 31.30
TDB99A 1941 28.66
TDB99A 1940 30.34
TDB99A 1939 28.33
TDB99A 1938 28.37
TDB99A 1937 27.91
TDB99A 1936 27.36
TDB99A 1935 26.66
TDB99A 1934 29.87
TDB99A 1933 29.29
TDB99A 1932 30.33
TDB99A 1931 29.90
TDB99A 1930 29.73
TDB99A 1929 30.43
TDB99A 1928 29.35
TDB99A 1927 28.75
TDB99A 1926 32.10
TDB99A 1925 30.34
TDB99A 1924 30.02
TDB99A 1923 28.65
TDB99A 1922 30.07
TDB99A 1921 29.16
TDB99A 1920 28.96
TDB99A 1919 29.87
TDB99A 1918 29.50
TDB99A 1917 27.20
TDB99A 1916 30.08
TDB99A 1915 28.54
TDB99A 1914 25.09
TDB99A 1913 26.04
TDB99A 1912 27.82
TDB99A 1911 27.48
TDB99A 1910 26.57
TDB99A 1909 27.57
TDB99A 1908 27.71
TDB99A 1907 26.64
TDB99A 1906 26.82
TDB99A 1905 27.54
TDB99A 1904 25.12
TDB99A 1903 24.67
285

TDB99A 1902 28.11
TDB99A 1901 28.72
TDB99A 1900 28.79
TDB99A 1899 27.84
TDB99A 1898 29.03
TDB99A 1897 28.99
TDB99A 1896 30.18
TDB99A 1895 28.69
TDB99A 1894 29.80
TDB99A 1893 26.92
TDB99A 1892 28.81
TDB99A 1891 29.06
TDB99A 1890 27.53
TDB99A 1889 26.88
TDB99A 1888 26.84
TDB99A 1887 28.05
TDB99A 1886 27.26
TDB99A 1885 26.81
TDB99A 1884 27.89
TDB99A 1883 30.10
TDB99A 1882 29.43
TDB99A 1881 29.86
TDB99A 1880 30.37
TDB99A 1879 29.99
TDB99A 1878 30.73
TDB99A 1877 27.84
TDB99A 1876 28.27
TDB99A 1875 26.02
TDB99A 1874 27.85
TDB99A 1873 28.45
TDB99A 1872 28.58
TDB99A 1871 27.81
TDB99A 1870 27.20
TDB99A 1869 26.52
TDB99A 1868 24.21
TDB99A 1867 26.54
TDB99A 1866 26.81
TDB99A 1865 26.93
TDB99A 1864 28.52
TDB99A 1863 27.82
286

TDB99A 1862 30.00
TDB99A 1861 31.23
TDB99A 1860 30.36
TDB99A 1859 29.15
TDB99A 1858 28.31
TDB99A 1857 28.58
TDB99A 1856 27.15
TDB99A 1855 26.31
TDB99A 1854 28.32
TDB99A 1853 29.04
TDB99A 1852 29.37
TDB99A 1851 27.16
TDB99A 1850 26.59
TDB99A 1849 26.39
TDB99A 1848 26.37
TDB99A 1847 28.13
TDB99A 1846 30.18
TDB99A 1845 29.53
TDB99A 1844 28.93
TDB99A 1843 29.42
TDB99A 1842 29.21
TDB99A 1841 27.90
TDB99A 1840 27.78
TDB99A 1839 28.22
TDB99A 1838 28.31
TDB99A 1837 27.38
TDB99A 1836 29.89
TDB99A 1835 26.77
TDB99A 1834 29.37
TDB99A 1833 29.66
TDB99A 1832 28.41
TDB99A 1831 30.44
TDB99A 1830 27.46
TDB99A 1829 29.38
TDB99A 1828 27.79
TDB99A 1827 25.95
TDB99A 1826 28.12
TDB99A 1825 27.17
TDB99A 1824 32.59
TDB99A 1823 28.82
287

TDB99A 1822 30.79
TDB99A 1821 28.95
TDB99A 1820 26.59
TDB99A 1819 27.96
TDB99A 1818 29.72
TDB99A 1817 27.32
TDB99A 1816 28.33
TDB99A 1815 27.98
TDB99A 1814 25.23
TDB99A 1813 28.35
TDB99A 1812 27.88
TDB99A 1811 28.43
TDB99A 1810 30.00
TDB99A 1809 29.51
TDB99A 1808 27.33
TDB99A 1807 27.87
TDB99A 1806 26.22
TDB99A 1805 27.18
TDB99A 1804 27.26
TDB99A 1803 24.87
TDB99A 1802 24.42
TDB99A 1801 27.70
TDB99A 1800 28.44
XDC0132A 2008 33.43
XDC0132A 2007 32.39
XDC0132A 2006 31.23
XDC0132A 2005 29.68
XDC0132A 2004 30.30
XDC0132A 2003 30.64
XDC0132A 2002 30.53
XDC0132A 2001 30.45
XDC0132A 2000 30.51
XDC0132A 1999 30.37
XDC0132A 1998 29.42
XDC0132A 1997 30.27
XDC0132A 1996 29.97
XDC0132A 1995 30.00
XDC0132A 1994 31.10
XDC0132A 1993 30.50
XDC0132A 1992 30.75
288

XDC0132A 1991 31.54
XDC0132A 1990 31.76
XDC0132A 1989 29.95
XDC0132A 1988 31.56
XDC0132A 1987 31.19
XDC0132A 1986 31.27
XDC0132A 1985 31.88
XDC0132A 1984 31.28
XDC0132A 1983 30.63
XDC0132A 1982 31.37
XDC0132A 1981 30.84
XDC0132A 1980 31.02
XDC0132A 1979 31.06
XDC0132A 1978 32.50
XDC0132A 1977 30.61
XDC0132A 1976 30.15
XDC0132A 1975 30.55
XDC0132A 1974 31.43
XDC0132A 1973 30.89
XDC0132A 1972 29.62
XDC0132A 1971 31.17
XDC0132A 1970 30.15
XDC0132A 1969 30.17
XDC0132A 1968 30.02
XDC0132A 1967 29.99
XDC0132A 1966 29.82
XDC0132A 1965 30.40
XDC0132A 1964 30.23
XDC0132A 1963 29.64
XDC0132A 1962 30.26
XDC0132A 1961 30.48
XDC0132A 1960 30.85
XDC0132A 1959 28.50
XDC0132A 1958 28.74
XDC0132A 1957 29.00
XDC0132A 1956 30.54
XDC0132A 1955 29.74
XDC0132A 1954 29.60
XDC0132A 1953 29.99
XDC0132A 1952 29.28
289

XDC0132A 1951 30.05
XDC0132A 1950 30.18
XDC0132A 1949 30.06
XDC0132A 1948 29.95
XDC0132A 1947 31.09
XDC0132A 1946 29.45
XDC0132A 1945 31.63
XDC0132A 1944 30.41
XDC0132A 1943 27.72
XDC0132A 1942 29.58
XDC0132A 1941 31.41
XDC0132A 1940 30.59
XDC0132A 1939 30.18
XDC0132A 1938 29.72
XDC0132A 1937 29.41
XDC0132A 1936 29.06
XDC0132A 1935 29.24
XDC0132A 1934 29.09
XDC0132A 1933 29.53
XDC0132A 1932 30.16
XDC0132A 1931 30.18
XDC0132A 1930 30.48
XDC0132A 1929 29.34
XDC0132A 1928 30.85
XDC0132A 1927 30.90
XDC0132A 1926 31.82
XDC0132A 1925 30.81
XDC0132A 1924 29.64
XDC0132A 1923 29.23
XDC0132A 1922 28.67
XDC0132A 1921 30.40
XDC0132A 1920 27.69
XDC0132A 1919 30.86
XDC0132A 1918 31.25
XDC0132A 1917 30.03
XDC0132A 1916 30.63
XDC0132A 1915 29.52
XDC0132A 1914 NaN
XDC0132A 1913 28.88
XDC0132A 1912 27.95
290

XDC0132A 1911 29.80
XDC0132A 1910 29.63
XDC0132A 1909 30.10
XDC0132A 1908 30.21
XDC0132A 1907 29.97
XDC0132A 1906 28.94
XDC0132A 1905 28.20
XDC0132A 1904 26.97
XDC0132A 1903 27.71
XDC0132A 1902 28.11
XDC0132A 1901 28.26
XDC0132A 1900 28.70
XDC0132A 1899 28.38
XDC0132A 1898 29.06
XDC0132A 1897 29.16
XDC0132A 1896 29.61
XDC0132A 1895 29.93
XDC0132A 1894 28.24
XDC0132A 1893 27.39
XDC0132A 1892 28.42
XDC0132A 1891 28.63
XDC0132A 1890 28.39
XDC0132A 1889 29.13
XDC0132A 1888 29.00
XDC0132A 1887 29.03
XDC0132A 1886 27.94
XDC0132A 1885 28.61
XDC0132A 1884 29.82
XDC0132A 1883 29.20
XDC0132A 1882 30.53
XDC0132A 1881 29.88
XDC0132A 1880 29.25
XDC0132A 1879 30.13
XDC0132A 1878 28.48
XDC0132A 1877 29.55
XDC0132A 1876 29.61
XDC0132A 1875 29.17
XDC0132A 1874 28.84
XDC0132A 1873 28.44
XDC0132A 1872 28.47
291

XDC0132A 1871 28.85
XDC0132A 1870 29.02
XDC0132A 1869 28.78
XDC0132A 1868 29.25
XDC0132A 1867 29.50
XDC0132A 1866 29.68
XDC0132A 1865 29.51
XDC0132A 1864 29.04
XDC0132A 1863 28.55
XDC0132A 1862 29.02
XDC0132A 1861 29.76
XDC0132A 1860 29.77
XDC0132A 1859 29.19
XDC0132A 1858 29.18
XDC0132A 1857 29.27
XDC0132A 1856 28.96
XDC0132A 1855 28.42
XDC0132A 1854 28.52
XDC0132A 1853 28.92
XDC0132A 1852 28.31
XDC0132A 1851 28.89
XDC0132A 1850 26.74
XDC0132A 1849 27.44
XDC0132A 1848 28.06
XDC0132A 1847 28.80
XDC0132A 1846 29.62
XDC0132A 1845 29.58
XDC0132A 1844 29.62
XDC0132A 1843 28.88
XDC0132A 1842 28.73
XDC0132A 1841 28.31
XDC0132A 1840 28.74
XDC0132A 1839 28.32
XDC0132A 1838 28.84
XDC0132A 1837 29.44
XDC0132A 1836 30.62
XDC0132A 1835 29.49
XDC0132A 1834 29.10
XDC0132A 1833 29.51
XDC0132A 1832 29.48
292

XDC0132A 1831 29.83
XDC0132A 1830 29.56
XDC0132A 1829 30.11
XDC0132A 1828 29.73
XDC0132A 1827 29.17
XDC0132A 1826 29.17
XDC0132A 1825 29.70
XDC0132A 1824 29.80
XDC0132A 1823 29.90
XDC0132A 1822 29.91
XDC0132A 1821 30.04
XDC0132A 1820 30.57
XDC0132A 1819 30.15
XDC0132A 1818 29.06
XDC0132A 1817 28.98
XDC0132A 1816 28.98
XDC0132A 1815 29.39
XDC0132A 1814 29.48
XDC0132A NaN NaN
XDC0132A 1783 30.80
XDC0132A 1782 30.63
XDC0132A 1781 29.22
XDC0132A 1780 29.09
XDC0132A 1779 28.55
XDC0132A 1778 28.60
XDC0132A 1777 30.36
XDC0132A 1776 31.23
XDC0132A 1775 30.33
XDC0132A 1774 28.25
XDC0132A 1773 29.01
XDC0132A 1772 29.08
XDC0132A 1771 29.87
XDC0132A 1770 30.97
XDC0132A 1769 28.98
XDC0132A 1768 28.76
XDC0132A 1767 29.06
XDC0132A 1766 29.26
XDC0132A 1765 29.40
XDC0132A 1764 30.87
XDC0132A 1763 31.54
293

XDC0132A 1762 29.65
XDC0132A 1761 29.70
XDC0132A 1760 29.38
XDC0132A 1759 29.14
XDC0132A 1758 28.85
XDC0132A 1757 28.36
XDC0132A 1756 28.25
XDC0132A 1755 27.44
XDC0132A 1754 28.45
XDC0132A 1753 27.62
XDC0132A 1752 28.87
XDC0132A 1751 29.73
XDC0132A 1750 31.75
XDC0132A 1749 32.08
XDC0132A 1748 30.84
XDC0132A 1747 29.69
XDC0132A 1746 29.24
XDC0142A 2008 33.77
XDC0142A 2007 31.79
XDC0142A 2006 31.42
XDC0142A 2005 30.50
XDC0142A 2004 31.42
XDC0142A 2003 31.88
XDC0142A 2002 30.97
XDC0142A 2001 33.28
XDC0142A 2000 31.66
XDC0142A 1999 30.63
XDC0142A 1998 31.36
XDC0142A 1997 30.74
XDC0142A 1996 30.58
XDC0142A 1995 32.81
XDC0142A 1994 33.04
XDC0142A 1993 31.01
XDC0142A 1992 31.79
XDC0142A 1991 31.82
XDC0142A 1990 31.69
XDC0142A 1989 29.71
XDC0142A 1988 31.45
XDC0142A 1987 30.54
XDC0142A 1986 31.44
294

XDC0142A 1985 32.44
XDC0142A 1984 30.98
XDC0142A 1983 30.80
XDC0142A 1982 32.65
XDC0142A 1981 31.81
XDC0142A 1980 31.03
XDC0142A 1979 32.18
XDC0142A 1978 32.71
XDC0142A 1977 31.15
XDC0142A 1976 31.25
XDC0142A 1975 31.66
XDC0142A 1974 32.77
XDC0142A 1973 31.25
XDC0142A 1972 30.47
XDC0142A 1971 31.96
XDC0142A 1970 31.36
XDC0142A 1969 31.76
XDC0142A 1968 31.09
XDC0142A 1967 30.47
XDC0142A 1966 31.14
XDC0142A 1965 31.87
XDC0142A 1964 31.13
XDC0142A 1963 31.83
XDC0142A 1962 31.51
XDC0142A 1961 31.84
XDC0142A 1960 31.75
XDC0142A 1959 29.65
XDC0142A 1958 30.69
XDC0142A 1957 31.35
XDC0142A 1956 32.14
XDC0142A 1955 30.42
XDC0142A 1954 30.05
XDC0142A 1953 31.33
XDC0142A 1952 30.37
XDC0142A 1951 30.46
XDC0142A 1950 31.67
XDC0142A 1949 29.98
XDC0142A 1948 30.86
XDC0142A 1947 32.16
XDC0142A 1946 30.95
295

XDC0142A 1945 32.58
XDC0142A 1944 31.22
XDC0142A 1943 29.64
XDC0142A 1942 30.48
XDC0142A 1941 33.11
XDC0142A 1940 31.28
XDC0142A 1939 31.57
XDC0142A 1938 31.14
XDC0142A 1937 30.78
XDC0142A 1936 30.94
XDC0142A 1935 31.17
XDC0142A 1934 30.82
XDC0142A 1933 31.90
XDC0142A 1932 32.79
XDC0142A 1931 32.32
XDC0142A 1930 32.30
XDC0142A 1929 31.41
XDC0142A 1928 32.56
XDC0142A 1927 32.05
XDC0142A 1926 32.70
XDC0142A 1925 31.68
XDC0142A 1924 30.27
XDC0142A 1923 29.69
XDC0142A 1922 29.88
XDC0142A 1921 28.94
XDC0142A 1920 28.80
XDC0142A 1919 31.90
XDC0142A 1918 30.71
XDC0142A 1917 30.75
XDC0142A 1916 31.04
XDC0142A 1915 29.29
XDC0142A 1914 29.33
XDC0142A 1913 29.68
XDC0142A 1912 29.31
XDC0142A 1911 29.92
XDC0142A 1910 31.49
XDC0142A 1909 30.85
XDC0142A 1908 31.26
XDC0142A 1907 31.06
XDC0142A 1906 29.84
296

XDC0142A 1905 29.21
XDC0142A 1904 28.25
XDC0142A 1903 27.45
XDC0142A 1902 28.48
XDC0142A 1901 28.05
XDC0142A 1900 29.55
XDC0142A 1899 28.82
XDC0142A 1898 28.41
XDC0142A 1897 29.22
XDC0142A 1896 29.78
XDC0142A 1895 30.40
XDC0142A 1894 30.12
XDC0142A 1893 28.17
XDC0142A 1892 28.45
XDC0142A 1891 29.93
XDC0142A 1890 29.25
XDC0142A 1889 30.26
XDC0142A 1888 29.88
XDC0142A 1887 29.49
XDC0142A 1886 28.73
XDC0142A 1885 29.08
XDC0142A 1884 30.90
XDC0142A 1883 30.44
XDC0142A 1882 29.93
XDC0142A 1881 30.84
XDC0142A 1880 30.55
XDC0142A 1879 31.21
XDC0142A 1878 29.78
XDC0142A 1877 29.47
XDC0142A 1876 30.24
XDC0142A 1875 31.46
XDC0142A 1874 30.33
XDC0142A 1873 30.00
XDC0142A 1872 30.54
XDC0142A 1871 28.92
XDC0142A 1870 29.22
XDC0142A 1869 28.91
XDC0142A 1868 29.79
XDC0142A 1867 30.77
XDC0142A 1866 30.14
297

XDC0142A 1865 30.23
XDC0142A 1864 29.77
XDC0142A 1863 29.05
XDC0142A 1862 29.42
XDC0142A 1861 31.05
XDC0142A 1860 30.82
XDC0142A 1859 30.27
XDC0142A 1858 29.70
XDC0142A 1857 29.18
XDC0142A 1856 29.79
XDC0142A 1855 28.90
XDC0142A 1854 28.93
XDC0142A 1853 30.40
XDC0142A 1852 30.54
XDC0142A 1851 29.17
XDC0142A 1850 29.40
XDC0142A 1849 28.96
XDC0142A 1848 28.31
XDC0142A 1847 28.87
XDC0142A 1846 30.69
XDC0142A 1845 30.94
XDC0142A 1844 31.65
XDC0142A 1843 31.43
XDC0142A 1842 30.39
XDC0142A 1841 29.69
XDC0142A 1840 30.54
XDC0142A 1839 29.47
XDC0142A 1838 29.30
XDC0142A 1837 30.56
XDC0142A 1836 30.98
XDC0142A 1835 30.26
XDC0142A 1834 30.36
XDC0142A 1833 30.40
XDC0142A 1832 28.66
XDC0142A 1831 32.46
XDC0142A 1830 30.20
XDC0142A 1829 32.06
XDC0142A 1828 30.63
XDC0142A 1827 30.02
XDC0142A 1826 30.02
298

XDC0142A 1825 30.94
XDC0142A 1824 32.10
XDC0142A 1823 30.89
XDC0142A 1822 30.83
XDC0142A 1821 30.98
XDC0142A 1820 30.09
XDC0142A 1819 30.16
XDC0142A 1818 29.55
XDC0142A 1817 29.14
XDC0142A 1816 29.39
XDC0142A 1815 29.61
XDC0142A 1814 29.72
XDC0142A 1813 29.38
XDC0142A 1812 30.51
XDC0142A 1811 31.58
XDC0142A 1810 31.78
XDC0142A 1809 31.00
XDC0142A 1808 30.51
XDC0142A 1807 29.78
XDC0142A 1806 29.12
XDC0142A 1805 30.56
XDC0142A 1804 29.52
XDC0142A 1803 28.67
XDC0142A 1802 28.99
XDC0142A 1801 30.18
XDC0142A 1800 31.18
XDC0142A 1799 30.40
XDC0142A 1798 29.29
XDC0142A 1797 31.76
XDC0142A 1796 32.14
XDC0142A 1795 30.43
XDC0142A 1794 30.17
XDC0142A 1793 29.89
XDC0142A 1792 30.75
XDC0142A 1791 28.91
XDC0142A 1790 29.34
XDC0142A 1789 31.44
XDC0142A 1788 30.50
XDC0142A 1787 31.49
XDC0142A 1786 30.53
299

XDC0142A 1785 30.65
XDC0142A 1784 31.28
XDC0142A 1783 30.88
XDC0142A 1782 30.52
XDC0142A 1781 28.85
XDC0142A 1780 28.95
XDC0142A 1779 28.93
XDC0142A 1778 28.85
XDC0142A 1777 29.75
XDC0142A 1776 31.52
XDC0142A 1775 30.14
XDC0142A 1774 29.17
XDC0142A 1773 27.64
XDC0142A 1772 29.88
XDC0142A 1771 29.68
XDC0142A 1770 31.53
XDC0142A 1769 29.67
XDC0142A 1768 29.34
XDC0142A 1767 29.22
XDC0142A 1766 30.82
XDC0142A 1765 30.22
XDC0142A 1764 31.35
XDC0142A 1763 32.08
XDC0142A 1762 30.49
XDC0142A 1761 29.69
XDC0142A 1760 30.23
XDC0142A 1759 29.38
XDC0142A 1758 29.56
XDC0142A 1757 28.48
XDC0142A 1756 28.63
XDC0142A 1755 28.39
XDC0142A 1754 29.83
XDC0142A 1753 29.54
XDC0142A 1752 29.58
XDC0142A 1751 29.33
XDC0142A 1750 30.34
XDC0142A 1749 31.96
XDC0142A 1748 30.92
XDC0142A 1747 29.69
XDC0142A 1746 31.42
300

XDC0142A 1745 30.64
XDC0142A 1744 30.00
XDC0142A 1743 30.87
XDC0142A 1742 30.30
XDC0142A 1741 30.11
XDC0142A 1740 30.97
XDC0142A 1739 29.93
XDC0142A 1738 29.29
XDC0142A 1737 30.03
XDC0142A 1736 29.42
XDC0142A 1735 29.63
XDC0142A 1734 30.26
XDC0142A 1733 29.50
XDC0142A 1732 28.60
XDC0142A 1731 28.97
XDC0142A 1730 30.55
XDC0142A 1729 31.90
XDC0142A 1728 30.99
XDC0142A 1727 30.04
XDC0142A 1720 31.17
XDC0142A 1719 31.62
XDC0142A 1718 30.20
XDC0142A 1717 30.04
XDC0142A 1716 30.12
XDC0142A 1715 30.50
XDC0142A 1714 31.73
XDC0142A 1713 31.20
XDC0142A 1712 30.13
XDC0142A 1711 30.81
XDC0142A 1710 30.17
XDC0142A 1709 31.01
XDC0142A 1708 31.26
XDC0142A 1707 30.90
XDC0142A 1706 29.98
XDC0142A 1705 27.90
XDC0142A 1704 29.55
XDC0142A 1703 29.70
XDC0142A 1702 28.91
XDC0142A 1701 28.56
XDC0142A 1700 29.41
301

XDC0142A 1699 29.71
XDC0142A 1698 29.02
XDC0142A 1697 29.57
XDC0142A 1696 30.08
XDC0142A 1695 29.46
XDC0142A 1694 29.94
XDC0142A 1693 30.57
XDC0142A 1692 30.76
XDC0142A 1691 30.40
XDC0142A 1690 31.77
XDC0142A 1689 31.99
XDC0142A 1688 30.67
XDC0142A 1687 29.69
XDC0142A 1686 28.84
XDC0142A 1685 28.65
XDC0142A 1684 29.90
XDC0142A 1683 30.64
XDC0142A 1682 30.71
XDC0142A 1681 30.10
XDC0142A 1680 29.13
XDC0142A 1679 29.21
XDC0142A 1678 30.45
XDC0142A 1677 30.20
XDC0142A 1676 31.93
XDC0142A 1675 30.33
XDC0142A 1674 29.86
XDC0142A 1673 29.86
XDC0142A 1672 29.86
XDC0142A 1671 29.03
XDC0142A 1670 29.80
XDC0142A 1669 30.11
XDC0142A 1668 31.35
XDC0142A 1667 32.06
XDC0142A 1666 31.49
XDC0142A 1665 30.71
XDC0142A 1664 30.27
XDC0142A 1663 30.07
XDC0142A 1662 28.11
XDC0142A 1661 27.69
XDC0142A 1660 29.37
302

XDC0142A 1659 29.22
XDC0142A 1658 29.47
XDC0142A 1657 31.05
XDC0142A 1656 29.88
XDC0142A 1655 28.52
XDC0142A 1654 29.56
XDC0142A 1653 30.02
XDC0142A 1652 31.22
XDC0142A 1651 29.28
XDC0142A 1650 29.09
XDC0142A 1649 31.41
XDC0142A 1648 30.31
XDC0142A 1647 28.99
XDC0142A 1646 28.95
XDC0142A 1645 29.74
XDC0142A 1644 30.36
XDC0142A 1643 31.38
XDC0142A 1642 29.18
XDC0142A 1641 29.13
XDC0142A 1640 31.56
XDC0142A 1639 31.37
XDC0142A 1638 29.45
XDC0142A 1637 29.92
XDC0142A 1636 30.16
XDC0142A 1635 30.21
XDC0142A 1634 30.52
XDC0142A 1633 30.90
XDC0142A 1632 30.77
XDC0142A 1631 30.34
XDC0142A 1630 29.91
XDC0142A 1629 27.89
XDC0142A 1628 30.88
XDC0142A 1627 31.71
XDC0142A 1626 29.30
XDC0142A 1625 27.75
XDC0142A 1624 26.18
XDC0142A 1623 26.20
XDC0142A 1622 26.53
XDC0142A 1621 26.42
XDC0142A 1620 27.99
303

XDC0142A 1619 30.03
XDC0142A 1618 30.54
XDC0142A 1617 27.64
XDC0142A 1616 26.71
XDC0142A 1615 27.69
XDC0142A 1614 28.46
XDC0142A 1613 29.38
XDC0142A 1612 28.09
XDC0142A 1611 27.68
XDC0142A 1610 28.68
XDC0142A 1609 29.73
XDC0142A 1608 29.54
XDC0142A 1607 28.64
XDC0142A 1606 27.78
XDC0142A 1605 27.68
XDC0142A 1604 28.77
XDC0142A 1603 28.78
XDC0142A 1602 29.55
XDC0142A 1601 28.54
XDC0142A 1600 28.68
XDC0142A 1599 27.65
XDC0142A 1598 27.58
XDC0142A 1574 29.25
XDC0142A 1573 29.18
XDC0142A 1572 29.71
XDC0142A 1571 29.26
XDC0142A 1570 30.26
XDC0142A 1569 28.04
XDC0142A 1568 28.82
XDC0142A 1567 30.73
XDC0142A 1566 28.92
XDC0142A 1565 29.62
XDC0142A 1564 30.89
XDC0142A 1563 31.63
XDC0142A 1562 29.98
XDC0142A 1561 28.93
XDC0142A 1560 27.98
XDC0142A 1559 29.76
XDC0142A 1558 29.66
XDC0142A 1557 29.92
304

XDC0142A 1556 28.99
XDC0142A 1555 29.93
XDC0142A 1554 29.95
XDC0142A 1553 31.11
XDC0142A 1552 29.79
XDC0142A 1551 29.75
XDC0142A 1551 29.88
XDC0142A 1550 30.31
XDC0142A 1549 30.09
XDC0142A 1548 31.73
XDC0142A 1547 29.75
XDC0142A 1546 29.64
XDC0142A 1545 29.59
XDC0142A 1544 29.57
XDC0142A 1543 27.77
XDC0142A 1542 28.67
XDC0142A 1541 30.27
XDC0142A 1540 29.56
XDC0142A 1539 31.88
XDC0142A 1538 31.76
XDC0142A 1537 29.89
XDC0142A 1536 29.47
XDC0142A 1535 29.71
XDC0142A 1534 29.64
XDC0142A 1533 30.48
XDC0142A 1532 31.17
XDC0142A 1531 31.18
XDC0142A 1530 29.04
XDC0142A 1529 30.72
XDC0142A 1528 30.83
XDC0142A 1527 30.50
XDC0142A 1526 30.31
XDC0142A 1525 28.43
XDC0142A 1524 29.09
XDC0142A 1523 30.14
XDC0142A 1522 29.20
XDC0142A 1521 30.17
XDC0142A 1520 31.12
XDC0142A 1519 30.73
XDC0142A 1518 29.34
305

XDC0142A 1517 29.12
XDC0142A 1516 30.04
XDC0142A 1515 31.16
XDC0142A 1514 31.81
XDC0142A 1513 30.11
XDC0142A 1512 31.67
XDC0142A 1511 30.94
XDC0142A 1510 29.26
XDC0142A 1509 29.04
XDC0142A 1508 30.06
XDC0142A 1507 31.70
XDC0144A 2008 33.77
XDC0144A 2007 31.79
XDC0144A 2006 31.42
XDC0144A 2005 30.50
XDC0144A 2004 31.42
XDC0144A 2003 31.88
XDC0144A 2002 30.97
XDC0144A 2001 33.28
XDC0144A 2000 31.66
XDC0144A 1999 30.63
XDC0144A 1998 31.36
XDC0144A 1997 30.74
XDC0144A 1996 30.58
XDC0144A 1995 32.81
XDC0144A 1994 33.04
XDC0144A 1993 31.01
XDC0144A 1992 31.79
XDC0144A 1991 31.82
XDC0144A 1990 31.69
XDC0144A 1989 29.71
XDC0144A 1988 31.45
XDC0144A 1987 30.54
XDC0144A 1986 31.44
XDC0144A 1985 32.44
XDC0144A 1984 30.98
XDC0144A 1983 30.80
XDC0144A 1982 32.65
XDC0144A 1981 31.81
XDC0144A 1980 31.03
306

XDC0144A 1979 32.18
XDC0144A 1978 32.71
XDC0144A 1977 31.15
XDC0144A 1976 31.25
XDC0144A 1975 31.66
XDC0144A 1974 32.77
XDC0144A 1973 31.25
XDC0144A 1972 30.47
XDC0144A 1971 31.96
XDC0144A 1970 31.36
XDC0144A 1969 31.76
XDC0144A 1968 31.09
XDC0144A 1967 30.47
XDC0144A 1966 31.14
XDC0144A 1965 31.87
XDC0144A 1964 31.13
XDC0144A 1963 31.83
XDC0144A 1962 31.51
XDC0144A 1961 31.84
XDC0144A 1960 31.75
XDC0144A 1959 29.65
XDC0144A 1958 30.69
XDC0144A 1957 31.35
XDC0144A 1956 32.14
XDC0144A 1955 30.42
XDC0144A 1954 30.05
XDC0144A 1953 31.33
XDC0144A 1952 30.37
XDC0144A 1951 30.46
XDC0144A 1950 31.67
XDC0144A 1949 29.98
XDC0144A 1948 30.86
XDC0144A 1947 32.16
XDC0144A 1946 30.95
XDC0144A 1945 32.58
XDC0144A 1944 31.22
XDC0144A 1943 29.64
XDC0144A 1942 30.48
XDC0144A 1941 33.11
XDC0144A 1940 31.28
307

XDC0144A 1939 31.57
XDC0144A 1938 31.14
XDC0144A 1937 30.78
XDC0144A 1936 30.94
XDC0144A 1935 31.17
XDC0144A 1934 30.82
XDC0144A 1933 31.90
XDC0144A 1932 32.79
XDC0144A 1931 32.32
XDC0144A 1930 32.30
XDC0144A 1929 31.41
XDC0144A 1928 32.56
XDC0144A 1927 32.05
XDC0144A 1926 32.70
XDC0144A 1925 31.68
XDC0144A 1924 30.27
XDC0144A 1923 29.69
XDC0144A 1922 29.88
XDC0144A 1921 28.94
XDC0144A 1920 28.80
XDC0144A 1919 31.90
XDC0144A 1918 30.71
XDC0144A 1917 30.75
XDC0144A 1916 31.04
XDC0144A 1915 29.29
XDC0144A 1914 29.33
XDC0144A 1913 29.68
XDC0144A 1912 29.31
XDC0144A 1911 29.92
XDC0144A 1910 31.49
XDC0144A 1909 30.85
XDC0144A 1908 31.26
XDC0144A 1907 31.06
XDC0144A 1906 29.84
XDC0144A 1905 29.21
XDC0144A 1904 28.25
XDC0144A 1903 27.45
XDC0144A 1902 28.48
XDC0144A 1901 28.05
XDC0144A 1900 29.55
308

XDC0144A 1899 28.82
XDC0144A 1898 28.41
XDC0144A 1897 29.22
XDC0144A 1896 29.78
XDC0144A 1895 30.40
XDC0144A 1894 30.12
XDC0144A 1893 28.17
XDC0144A 1892 28.45
XDC0144A 1891 29.93
XDC0144A 1890 29.25
XDC0144A 1889 30.26
XDC0144A 1888 29.88
XDC0144A 1887 29.49
XDC0144A 1886 28.73
XDC0144A 1885 29.08
XDC0144A 1884 30.90
XDC0144A 1883 30.44
XDC0144A 1882 29.93
XDC0144A 1881 30.84
XDC0144A 1880 30.55
XDC0144A 1879 31.21
XDC0144A 1878 29.78
XDC0144A 1877 29.47
XDC0144A 1876 30.24
XDC0144A 1875 31.46
XDC0144A 1874 30.33
XDC0144A 1873 30.00
XDC0144A 1872 30.54
XDC0144A 1871 28.92
XDC0144A 1870 29.22
XDC0144A 1869 28.91
XDC0144A 1868 29.79
XDC0144A 1867 30.77
XDC0144A 1866 30.14
XDC0144A 1865 30.23
XDC0144A 1864 29.77
XDC0144A 1863 29.05
XDC0144A 1862 29.42
XDC0144A 1861 31.05
XDC0144A 1860 30.82
309

XDC0144A 1859 30.27
XDC0144A 1858 29.70
XDC0144A 1857 29.18
XDC0144A 1856 29.79
XDC0144A 1855 28.90
XDC0144A 1854 28.93
XDC0144A 1853 30.40
XDC0144A 1852 30.54
XDC0144A 1851 29.17
XDC0144A 1850 29.40
XDC0144A 1849 28.96
XDC0144A 1848 28.31
XDC0144A 1847 28.87
XDC0144A 1846 30.69
XDC0144A 1845 30.94
XDC0144A 1844 31.65
XDC0144A 1843 31.43
XDC0144A 1842 30.39
XDC0144A 1841 29.69
XDC0144A 1840 30.54
XDC0144A 1839 29.47
XDC0144A 1838 29.30
XDC0144A 1837 30.56
XDC0144A 1836 30.98
XDC0144A 1835 30.26
XDC0144A 1834 30.36
XDC0144A 1833 30.40
XDC0144A 1832 28.66
XDC0144A 1831 32.46
XDC0144A 1830 30.20
XDC0144A 1829 32.06
XDC0144A 1828 30.63
XDC0144A 1827 30.02
XDC0144A 1826 30.02
XDC0144A 1825 30.94
XDC0144A 1824 32.10
XDC0144A 1823 30.89
XDC0144A 1822 30.83
XDC0144A 1821 30.98
XDC0144A 1820 30.09
310

XDC0144A 1819 30.16
XDC0144A 1818 29.55
XDC0144A 1817 29.14
XDC0144A 1816 29.39
XDC0144A 1815 29.61
XDC0144A 1814 29.72
XDC0144A 1813 29.38
XDC0144A 1812 30.51
XDC0144A 1811 31.58
XDC0144A 1810 31.78
XDC0144A 1809 31.00
XDC0144A 1808 30.51
XDC0144A 1807 29.78
XDC0144A 1806 29.12
XDC0144A 1805 30.56
XDC0144A 1804 29.52
XDC0144A 1803 28.67
XDC0144A 1802 28.99
XDC0144A 1801 30.18
XDC0144A 1800 31.18
XDC0144A 1799 30.40
XDC0144A 1798 29.29
XDC0144A 1797 31.76
XDC0144A 1796 32.14
XDC0144A 1795 30.43
XDC0144A 1794 30.17
XDC0144A 1793 29.89
XDC0144A 1792 30.75
XDC0144A 1791 28.91
XDC0144A 1790 29.34
XDC0144A 1789 31.44
XDC0144A 1788 30.50
XDC0144A 1787 31.49
XDC0144A 1786 30.53
XDC0144A 1785 30.65
XDC0144A 1784 31.28
XDC0144A 1783 30.88
XDC0144A 1782 30.52
XDC0144A 1781 28.85
XDC0144A 1780 28.95
311

XDC0144A 1779 28.93
XDC0144A 1778 28.85
XDC0144A 1777 29.75
XDC0144A 1776 31.52
XDC0144A 1775 30.14
XDC0144A 1774 29.17
XDC0144A 1773 27.64
XDC0144A 1772 29.88
XDC0144A 1771 29.68
XDC0144A 1770 31.53
XDC0144A 1769 29.67
XDC0144A 1768 29.34
XDC0144A 1767 29.22
XDC0144A 1766 30.82
XDC0144A 1765 30.22
XDC0144A 1764 31.35
XDC0144A 1763 32.08
XDC0144A 1762 30.49
XDC0144A 1761 29.69
XDC0144A 1760 30.23
XDC0144A 1759 29.38
XDC0144A 1758 29.56
XDC0144A 1757 28.48
XDC0144A 1756 28.63
XDC0144A 1755 28.39
XDC0144A 1754 29.83
XDC0144A 1753 29.54
XDC0144A 1752 29.58
XDC0144A 1751 29.33
XDC0144A 1750 30.34
XDC0144A 1749 31.96
XDC0144A 1748 30.92
XDC0144A 1747 29.69
XDC0144A 1746 31.42
XDC0144A 1745 30.64
XDC0144A 1744 30.00
XDC0144A 1743 30.87
XDC0144A 1742 30.30
XDC0144A 1741 30.11
XDC0144A 1740 30.97
312

XDC0144A 1739 29.93
XDC0144A 1738 29.29
XDC0144A 1737 30.03
XDC0144A 1736 29.42
XDC0144A 1735 29.63
XDC0144A 1734 30.26
XDC0144A 1733 29.50
XDC0144A 1732 28.60
XDC0144A 1731 28.97
XDC0144A 1730 30.55
XDC0144A 1729 31.90
XDC0144A 1728 30.99
XDC0144A 1727 30.04
XDC0144A 1720 31.17
XDC0144A 1719 31.62
XDC0144A 1718 30.20
XDC0144A 1717 30.04
XDC0144A 1716 30.12
XDC0144A 1715 30.50
XDC0144A 1714 31.73
XDC0144A 1713 31.20
XDC0144A 1712 30.13
XDC0144A 1711 30.81
XDC0144A 1710 30.17
XDC0144A 1709 31.01
XDC0144A 1708 31.26
XDC0144A 1707 30.90
XDC0144A 1706 29.98
XDC0144A 1705 27.90
XDC0144A 1704 29.55
XDC0144A 1703 29.70
XDC0144A 1702 28.91
XDC0144A 1701 28.56
XDC0144A 1700 29.41
XDC0144A 1699 29.71
XDC0144A 1698 29.02
XDC0144A 1697 29.57
XDC0144A 1696 30.08
XDC0144A 1695 29.46
XDC0144A 1694 29.94
313

XDC0144A 1693 30.57
XDC0144A 1692 30.76
XDC0144A 1691 30.40
XDC0144A 1690 31.77
XDC0144A 1689 31.99
XDC0144A 1688 30.67
XDC0144A 1687 29.69
XDC0144A 1686 28.84
XDC0144A 1685 28.65
XDC0144A 1684 29.90
XDC0144A 1683 30.64
XDC0144A 1682 30.71
XDC0144A 1681 30.10
XDC0144A 1680 29.13
XDC0144A 1679 29.21
XDC0144A 1678 30.45
XDC0144A 1677 30.20
XDC0144A 1676 31.93
XDC0144A 1675 30.33
XDC0144A 1674 29.86
XDC0144A 1673 29.86
XDC0144A 1672 29.86
XDC0144A 1671 29.03
XDC0144A 1670 29.80
XDC0144A 1669 30.11
XDC0144A 1668 31.35
XDC0144A 1667 32.06
XDC0144A 1666 31.49
XDC0144A 1665 30.71
XDC0144A 1664 30.27
XDC0144A 1663 30.07
XDC0144A 1662 28.11
XDC0144A 1661 27.69
XDC0144A 1660 29.37
XDC0144A 1659 29.22
XDC0144A 1658 29.47
XDC0144A 1657 31.05
XDC0144A 1656 29.88
XDC0144A 1655 28.52
XDC0144A 1654 29.56
314

XDC0144A 1653 30.02
XDC0144A 1652 31.22
XDC0144A 1651 29.28
XDC0144A 1650 29.09
XDC0144A 1649 31.41
XDC0144A 1648 30.31
XDC0144A 1647 28.99
XDC0144A 1646 28.95
XDC0144A 1645 29.74
XDC0144A 1644 30.36
XDC0144A 1643 31.38
XDC0144A 1642 29.18
XDC0144A 1641 29.13
XDC0144A 1640 31.56
XDC0144A 1639 31.37
XDC0144A 1638 29.45
XDC0144A 1637 29.92
XDC0144A 1636 30.16
XDC0144A 1635 30.21
XDC0144A 1634 30.52
XDC0144A 1633 30.90
XDC0144A 1632 30.77
XDC0144A 1631 30.34
XDC0144A 1630 29.91
XDC0144A 1629 27.89
XDC0144A 1628 30.88
XDC0144A 1627 31.71
XDC0144A 1626 29.30
XDC0144A 1625 27.75
XDC0144A 1624 26.18
XDC0144A 1623 26.20
XDC0144A 1622 26.53
XDC0144A 1621 26.42
XDC0144A 1620 27.99
XDC0144A 1619 30.03
XDC0144A 1618 30.54
XDC0144A 1617 27.64
XDC0144A 1616 26.71
XDC0144A 1615 27.69
XDC0144A 1614 28.46
315

XDC0144A 1613 29.38
XDC0144A 1612 28.09
XDC0144A 1611 27.68
XDC0144A 1610 28.68
XDC0144A 1609 29.73
XDC0144A 1608 29.54
XDC0144A 1607 28.64
XDC0144A 1606 27.78
XDC0144A 1605 27.68
XDC0144A 1604 28.77
XDC0144A 1603 28.78
XDC0144A 1602 29.55
XDC0144A 1601 28.54
XDC0144A 1600 28.68
XDC0144A 1599 27.65
XDC0144A 1598 27.58
XDC0144A 1574 29.25
XDC0144A 1573 29.18
XDC0144A 1572 29.71
XDC0144A 1571 29.26
XDC0144A 1570 30.26
XDC0144A 1569 28.04
XDC0144A 1568 28.82
XDC0144A 1567 30.73
XDC0144A 1566 28.92
XDC0144A 1565 29.62
XDC0144A 1564 30.89
XDC0144A 1563 31.63
XDC0144A 1562 29.98
XDC0144A 1561 28.93
XDC0144A 1560 27.98
XDC0144A 1559 29.76
XDC0144A 1558 29.66
XDC0144A 1557 29.92
XDC0144A 1556 28.99
XDC0144A 1555 29.93
XDC0144A 1554 29.95
XDC0144A 1553 31.11
XDC0144A 1552 29.79
XDC0144A 1551 29.75
316

XDC0144A 1551 29.88
XDC0144A 1550 30.31
XDC0144A 1549 30.09
XDC0144A 1548 31.73
XDC0144A 1547 29.75
XDC0144A 1546 29.64
XDC0144A 1545 29.59
XDC0144A 1544 29.57
XDC0144A 1543 27.77
XDC0144A 1542 28.67
XDC0144A 1541 30.27
XDC0144A 1540 29.56
XDC0144A 1539 31.88
XDC0144A 1538 31.76
XDC0144A 1537 29.89
XDC0144A 1536 29.47
XDC0144A 1535 29.71
XDC0144A 1534 29.64
XDC0144A 1533 30.48
XDC0144A 1532 31.17
XDC0144A 1531 31.18
XDC0144A 1530 29.04
XDC0144A 1529 30.72
XDC0144A 1528 30.83
XDC0144A 1527 30.50
XDC0144A 1526 30.31
XDC0144A 1525 28.43
XDC0144A 1524 29.09
XDC0144A 1523 30.14
XDC0144A 1522 29.20
XDC0144A 1521 30.17
XDC0144A 1520 31.12
XDC0144A 1519 30.73
XDC0144A 1518 29.34
XDC0144A 1517 29.12
XDC0144A 1516 30.04
XDC0144A 1515 31.16
XDC0144A 1514 31.81
XDC0144A 1513 30.11
XDC0144A 1512 31.67
317

XDC0144A 1511 30.94
XDC0144A 1510 29.26
XDC0144A 1509 29.04
XDC0144A 1508 30.06
XDC0144A 1507 31.70
XDC0147A 1708 31.06
XDC0147A 1709 30.10
XDC0147A 1710 31.27
XDC0147A 1711 30.90
XDC0147A 1712 30.81
XDC0147A 1713 31.52
XDC0147A 1714 30.67
XDC0147A 1715 29.98
XDC0147A 1716 30.29
XDC0147A 1717 30.83
XDC0147A 1718 31.52
XDC0147A 1719 32.10
XDC0147A 1720 31.63
XDC0147A 1721 32.58
XDC0147A 1722 31.43
XDC0147A 1723 31.49
XDC0147A 1724 30.45
XDC0147A 1725 31.50
XDC0147A 1726 29.12
XDC0147A 1727 31.69
XDC0147A 1728 31.99
XDC0147A 1729 32.32
XDC0147A 1730 31.51
XDC0147A 1731 30.30
XDC0147A 1732 29.67
XDC0147A 1733 31.11
XDC0147A 1734 30.23
XDC0147A 1735 30.31
XDC0147A 1736 30.09
XDC0147A 1737 29.96
XDC0147A 1738 29.97
XDC0147A 1739 30.69
XDC0147A 1740 30.96
XDC0147A 1741 30.41
XDC0147A 1742 30.33
318

XDC0147A 1743 31.21
XDC0147A 1744 30.74
XDC0147A 1745 30.58
XDC0147A 1746 30.62
XDC0147A 1747 31.58
XDC0147A 1748 33.14
XDC0147A 1749 33.14
XDC0147A 1750 30.87
XDC0147A 1751 31.31
XDC0147A 1752 29.80
XDC0147A 1753 31.06
XDC0147A 1754 29.84
XDC0147A 1755 28.39
XDC0147A 1756 28.76
XDC0147A 1757 29.20
XDC0147A 1758 29.87
XDC0147A 1759 29.55
XDC0147A 1760 30.38
XDC0147A 1761 30.07
XDC0147A 1762 31.25
XDC0147A 1763 32.37
XDC0147A 1764 30.68
XDC0147A 1765 30.73
XDC0147A 1766 31.66
XDC0147A 1767 29.69
XDC0147A 1768 30.24
XDC0147A 1769 31.44
XDC0147A 1770 32.31
XDC0147A 1771 30.10
XDC0147A 1772 30.77
XDC0147A 1773 28.44
XDC0147A 1774 30.14
XDC0147A 1775 31.11
XDC0147A 1776 32.53
XDC0147A 1777 30.64
XDC0147A 1778 30.04
XDC0147A 1779 30.18
XDC0147A 1780 29.47
XDC0147A 1781 30.47
XDC0147A 1782 30.98
319

XDC0147A 1783 32.22
XDC0147A 1784 32.08
XDC0147A 1785 31.20
XDC0147A 1786 30.84
XDC0147A 1787 30.95
XDC0147A 1788 30.94
XDC0147A 1789 30.05
XDC0147A 1790 29.54
XDC0147A 1791 30.56
XDC0147A 1792 31.37
XDC0147A 1793 30.71
XDC0147A 1794 31.12
XDC0147A 1795 31.72
XDC0147A 1796 33.17
XDC0147A 1797 31.73
XDC0147A 1798 29.61
XDC0147A 1799 32.16
XDC0147A 1800 32.25
XDC0147A 1801 29.90
XDC0147A 1802 29.31
XDC0147A 1803 29.98
XDC0147A 1804 31.37
XDC0147A 1805 31.14
XDC0147A 1806 30.16
XDC0147A 1807 30.96
XDC0147A 1808 30.88
XDC0147A 1809 31.64
XDC0147A 1810 32.88
XDC0147A 1811 30.91
XDC0147A 1812 30.89
XDC0147A 1813 31.08
XDC0147A 1814 30.42
XDC0147A 1815 30.86
XDC0147A 1816 31.77
XDC0147A 1817 30.54
XDC0147A 1818 31.46
XDC0147A 1819 31.11
XDC0147A 1820 31.40
XDC0147A 1821 31.59
XDC0147A 1822 31.68
320

XDC0147A 1823 30.88
XDC0147A 1824 32.35
XDC0147A 1825 31.33
XDC0147A 1826 29.95
XDC0147A 1827 31.29
XDC0147A 1828 31.61
XDC0147A 1829 31.34
XDC0147A 1830 30.68
XDC0147A 1831 31.68
XDC0147A 1832 29.98
XDC0147A 1833 30.48
XDC0147A 1834 30.36
XDC0147A 1835 30.15
XDC0147A 1836 31.24
XDC0147A 1837 29.22
XDC0147A 1838 30.01
XDC0147A 1839 29.18
XDC0147A 1840 30.09
XDC0147A 1841 29.04
XDC0147A 1842 29.98
XDC0147A 1843 31.17
XDC0147A 1844 30.59
XDC0147A 1845 30.17
XDC0147A 1846 29.64
XDC0147A 1847 28.29
XDC0147A 1848 29.21
XDC0147A 1849 29.77
XDC0147A 1850 29.85
XDC0147A 1851 29.44
XDC0147A 1852 31.08
XDC0147A 1853 30.46
XDC0147A 1854 29.86
XDC0147A 1855 30.57
XDC0147A 1856 30.35
XDC0147A 1857 30.02
XDC0147A 1858 30.30
XDC0147A 1859 30.44
XDC0147A 1860 31.75
XDC0147A 1861 30.58
XDC0147A 1862 30.19
321

XDC0147A 1863 30.38
XDC0147A 1864 30.98
XDC0147A 1865 30.90
XDC0147A 1866 30.41
XDC0147A 1867 31.09
XDC0147A 1868 29.05
XDC0147A 1869 30.75
XDC0147A 1870 29.64
XDC0147A 1871 30.54
XDC0147A 1872 31.10
XDC0147A 1873 29.76
XDC0147A 1874 30.51
XDC0147A 1875 30.25
XDC0147A 1876 30.00
XDC0147A 1877 28.75
XDC0147A 1878 30.46
XDC0147A 1879 30.88
XDC0147A 1880 30.00
XDC0147A 1881 30.49
XDC0147A 1882 29.86
XDC0147A 1883 31.22
XDC0147A 1884 30.95
XDC0147A 1885 29.41
XDC0147A 1886 29.57
XDC0147A 1887 30.11
XDC0147A 1888 30.14
XDC0147A 1889 29.70
XDC0147A 1890 29.27
XDC0147A 1891 30.20
XDC0147A 1892 28.48
XDC0147A 1893 29.40
XDC0147A 1894 30.53
XDC0147A 1895 29.56
XDC0147A 1896 29.68
XDC0147A 1897 29.49
XDC0147A 1898 29.24
XDC0147A 1899 29.52
XDC0147A 1900 30.30
XDC0147A 1901 28.75
XDC0147A 1902 27.55
322

XDC0147A 1903 29.27
XDC0147A 1904 29.06
XDC0147A 1905 29.15
XDC0147A 1906 29.44
XDC0147A 1907 29.51
XDC0147A 1908 30.02
XDC0147A 1909 30.04
XDC0147A 1910 30.21
XDC0147A 1911 29.85
XDC0147A 1912 29.43
XDC0147A 1913 29.03
XDC0147A 1914 29.59
XDC0147A 1915 30.38
XDC0147A 1916 30.85
XDC0147A 1917 29.65
XDC0147A 1918 31.01
XDC0147A 1919 31.13
XDC0147A 1920 28.35
XDC0147A 1921 29.39
XDC0147A 1922 29.21
XDC0147A 1923 29.92
XDC0147A 1924 30.12
XDC0147A 1926 31.67
XDC0147A 1927 30.62
XDC0147A 1928 33.20
XDC0147A 1929 31.89
XDC0147A 1930 31.93
XDC0147A 1931 32.19
XDC0147A 1932 32.60
XDC0147A 1933 32.08
XDC0147A 1934 31.38
XDC0147A 1935 30.99
XDC0147A 1936 30.20
XDC0147A 1937 30.45
XDC0147A 1938 30.46
XDC0147A 1939 30.59
XDC0147A 1940 31.40
XDC0147A 1941 31.73
XDC0147A 1942 31.08
XDC0147A 1943 30.38
323

XDC0147A 1944 30.63
XDC0147A 1945 31.96
XDC0147A 1946 31.25
XDC0147A 1947 31.93
XDC0147A 1948 31.10
XDC0147A 1949 30.56
XDC0147A 1950 31.32
XDC0147A 1951 31.02
XDC0147A 1952 30.70
XDC0147A 1953 31.44
XDC0147A 1954 30.34
XDC0147A 1955 30.67
XDC0147A 1956 31.93
XDC0147A 1957 30.95
XDC0147A 1958 30.38
XDC0147A 1959 30.36
XDC0147A 1960 31.77
XDC0147A 1961 31.27
XDC0147A 1962 30.64
XDC0147A 1963 30.68
XDC0147A 1964 30.55
XDC0147A 1965 30.99
XDC0147A 1966 30.62
XDC0147A 1967 30.81
XDC0147A 1968 30.96
XDC0147A 1969 31.75
XDC0147A 1970 31.21
XDC0147A 1971 30.87
XDC0147A 1972 29.14
XDC0147A 1973 31.59
XDC0147A 1974 31.83
XDC0147A 1975 31.77
XDC0147A 1976 31.10
XDC0147A 1977 31.39
XDC0147A 1978 32.72
XDC0147A 1979 32.87
XDC0147A 1980 31.22
XDC0147A 1981 32.10
XDC0147A 1982 32.77
XDC0147A 1983 31.22
324

XDC0147A 1984 31.01
XDC0147A 1985 32.67
XDC0147A 1986 32.07
XDC0147A 1987 31.32
XDC0147A 1988 31.78
XDC0147A 1989 29.38
XDC0147A 1990 31.85
XDC0147A 1991 32.21
XDC0147A 1992 31.41
XDC0147A 1993 30.35
XDC0147A 1994 31.95
XDC0147A 1995 32.45
XDC0147A 1996 30.70
XDC0147A 1997 30.65
XDC0147A 1998 31.52
XDC0147A 1999 29.73
XDC0147A 2000 31.05
XDC0147A 2001 32.63
XDC0147A 2002 31.07
XDC0147A 2003 31.06
XDC0147A 2004 31.25
XDC0147A 2005 30.30
XDC0147A 2006 30.69
XDC0147A 2007 31.05
XDC0147A 2008 32.26

Abstract (if available)

Abstract This dissertation investigates hydrological variability within tropical Asia over the past several few centuries as reflected in the stable oxygen isotope composition of atmospheric moisture. The stable isotopes of water in the climate system are unique tracers of moisture transport and tropical rainfall variability. The isotopic signal of atmospheric moisture within the tropics is transferred to cellulose of tropical trees during photosynthesis. Thus, the isotopic composition of tree cellulose can provide an archive of past hydrologic variability through isotopic reconstructions of the cellulose extracted from annual rings of long lived trees. The tropical atmospheric variability reflected in tropical trees can include variations in the Indian Monsoon and changes in moisture availability over Asia in response to the El Niño-Southern Oscillation (ENSO). Here an attempt has been made to better understand how the atmospheric dynamics associated within these climate phenomena influence the isotopic composition of tree cellulose and how these climate signatures have changed through time. High-resolution water isotope records are developed from trees collected from northern Thailand, southern Cambodia, and eastern part of the Tibetan Plateau. These records are examined to assess whether and how the 20th century is unique in terms of the hydrological conditions in tropical Asia under the influences of both monsoon and ENSO with the observed temperature changes. ❧ In northern Thailand, the oxygen isotopic composition (δ¹⁸O) of tree cellulose samples of Pinus kesiya from a montane forest has been analyzed in subannual resolution for the past 80 years. The cellulose δ¹⁸O values exhibit a distinctive annual cycle with an amplitude of up to 12‰, which is interpreted to reflect primarily the seasonal cycle of precipitation δ¹⁸O. The cellulose δ¹⁸O annual mean values correlate significantly with the amount of summer monsoon precipitation over the India subcontinent, corroborating recent studies that suggest the so-called “isotope amount effect” in the tropical precipitation δ¹⁸O reflects the hydrological processes of the upstream or the moisture source regions instead of the rainfall amount at the local site. No obvious trend in the summer monsoon precipitation is detected from the cellulose δ¹⁸O record. However, the record does suggest a temporal weakening relationship between the Indian Monsoon and ENSO over the 20th century. The annual maxima in the cellulose δ¹⁸O values are representative of the moisture balance during the winter dry season, and possibly document a decreasing trend in the isotopically-distinct fog water input during the dry season because of the warming in the 20th century. ❧ Isotope chronologies of Pinus merkusii from a coastal lowland forest in Cambodia have been generated to investigate hydrological variability over the Indo-Pacific Warm Pool (IPWP), based on the aforementioned observation that the δ¹⁸O in precipitation reflects the hydroclimate of the moisture source region. The IPWP is a major source of heat and moisture to the atmosphere and thus strongly influences the global climate. Recognizing its past variability is crucial for understanding large scale climate dynamics such as ENSO. The subannual cellulose δ¹⁸O has been replicated with multiple tree cores which span the past 140 years. The analysis of model outputs from a water isotope-enabled atmospheric model is used in conjunction with isotopic data from tree cellulose and precipitation to investigate moisture sources and how these sources of moisture vary on different timescales. The cellulose δ¹⁸O exhibits strong correlations with convection intensity and precipitation amount over the IPWP. Spectral analysis of the cellulose δ¹⁸O reveals significant peaks at 2-7 years corresponding to ENSO frequencies. This cellulose δ¹⁸O record exhibits no clear overall trend, but the period of 1880s through 1910s is characterized by relatively enriched cellulose δ¹⁸O values, which possibly indicates a background condition in the tropical Pacific Ocean that was more El Niño-like. ❧ Stable isotope dendrochronologies have been developed for sites across the eastern Tibetan Plateau. The plateau plays a pivotal role in creating the land-sea thermal contrast that is theorized to drive the summer monsoon circulation. Today, precipitation across the southern Tibetan Plateau is dominated by moisture carried by the summer monsoon winds. The isotopic composition of this moisture varies with the precipitation amount. Over the northern Tibetan Plateau, atmospheric moisture that falls as precipitation is from westerly air masses that carry a large fraction of recycled moisture across the continent. The isotopic composition of this moisture source is distinct from monsoon moisture over the southern Plateau. In addition, there is an important temperature effect that affects the isotopic fractionation of oxygen isotopes in precipitation over the northern and central Plateau. An inter-comparison of annually resolved tree cellulose δ¹⁸O values from two sites on the Tibetan Plateau forming a latitudinal transect, together with data from a former study are used here to investigate the interplay of these different moisture sources and temperature influence over time. The data from the northerly site indicate the late 20th century was the warmest and/or driest period of the past 500 years in the northeastern Tibetan Plateau, whereas evidence from the southerly site suggests there has been an increase in the strength of the summer monsoon circulation since the 1940s compared to the past two centuries. ❧ These studies have demonstrated that tree cellulose δ¹⁸O is a robust high-resolution proxy for hydroclimate in the past. In tropical Southeast Asia, tree cellulose δ¹⁸O could shed light on surface hydrology of the IPWP that is closely related to ENSO. Observations from tree cellulose δ¹⁸O in my studies have suggested no overall trend in the frequency or magnitude of ENSO variability through the 20th century, but a possible El Niño-like condition from the 1880s to the 1910s. Tree cellulose δ¹⁸O in northern Thailand indicates no overall trend in the monsoon precipitation in South and Southeast Asia. However, the new isotopic data presented here suggest monsoon circulation has intensified in the late 20th century across the eastern Tibetan Plateau.

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Asset Metadata

Creator Zhu, Mengfan (author)

Core Title Recent variability in the hyrdological cycle of tropical Asia from oxygen isotopes of tree celulose

School College of Letters, Arts and Sciences

Degree Doctor of Philosophy

Degree Program Geological Sciences

Publication Date 07/25/2012

Defense Date 05/22/2012

Publisher University of Southern California (original), University of Southern California. Libraries (digital)

Tag ENSO,monsoon,OAI-PMH Harvest,tree cellulose,δ18O

Language English

Contributor Electronically uploaded by the author (provenance)

Advisor Stott, Lowell (committee chair), Emile-Geay, Julien (committee member), Feakins, Sarah J. (committee member), Wilson, John P. (committee member)

Creator Email mengfan.zhu@gmail.com,mengfanz@usc.edu

Permanent Link (DOI) https://doi.org/10.25549/usctheses-c3-65436

Unique identifier UC11289834

Identifier usctheses-c3-65436 (legacy record id)

Legacy Identifier etd-ZhuMengfan-991.pdf

Dmrecord 65436

Document Type Dissertation

Rights Zhu, Mengfan

Type texts

Source University of Southern California (contributing entity), University of Southern California Dissertations and Theses (collection)

Access Conditions The author retains rights to his/her dissertation, thesis or other graduate work according to U.S. copyright law. Electronic access is being provided by the USC Libraries in agreement with the a...

Repository Name University of Southern California Digital Library

Repository Location USC Digital Library, University of Southern California, University Park Campus MC 2810, 3434 South Grand Avenue, 2nd Floor, Los Angeles, California 90089-2810, USA